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Conference Academic Partners

and by alphabetical order:

3

General Schedule ..........................................................page 4

Index by session ............................................................page 7

Index by author ..............................................................page 8

Keynote Lectures ........................................................page 26

Oral communinations ..............................................page 29

Poster communications ...................................... page 197

TABLE OF CONTENT

4

GENERAL SCHEDULEMonday July 9Room II

10:15-10:45 Opening plenary session

Session 02 : physical measurement S02-o-01 10:45-11:00 MEIJER Harro A. J. et al.S02-o-02 11:00-11:15 MÜLLER Arnold et al.S02-o-03 11:15-11:30 VON REDEN Karl F. et al.S02-o-04 11:30-11:45 VOGEL John et al.S02-o-05 11:45-12:00 KLEIN Matthias et al.S02-o-06 12:00-12:15 SYNAL Hans-Arno et al.S02-o-07 12:15-12:30 SALAZAR Gary et al.

Lunch Break and Poster Session A

Room IISession 03 - pretreatment protocolsS03-o-01 14:15-14:30 STEIER Peter et al.S03-o-02 14:30-14:45 BROCK Fiona et al.S03-o-03 14:45-15:00 BOUDIN Mathieu et al.S03-o-04 15:00-15:15 LEVCHENKO Vladimir et al.S03-o-05 15:15-15:30 SANTOS Guaciara Macedo et al.S03-o-06 15:30-15:45 WANG Hong S03-o-07 15:45-16:00 GÜTTLER Dominik et al.

Coffee Break and Poster Session AKEYNoTE-01 17:45-18:45 MAZZOTTI Davide et al.

Tuesday July 10Room II Room IVSession 03 - pretreatment protocols Session 13 - continental waterS03-o-08 08:15-08:30 MARZAIOLI Fabio et al. S13-o-01 08:15-08:30 CARMI Israel S03-o-09 08:30-08:45 LEROY Stéphanie et al. S13-o-02 08:30-08:45 GILLON Marina et al.S03-o-10 08:45-09:00 GENBERG Johan et al. S13-o-03 08:45-09:00 DULINSKI Marek et al.S03-o-11 09:00-09:15 MEIJER Harro A. J. et al. S13-o-04 09:00-09:15 POVINEC Pavel et al.S03-o-12 09:15-09:30 ROSENHEIM Brad et al. S13-o-05 09:15-09:30 GENTY Dominique et al.S03-o-13 09:30-09:45 WANG Shing-lin et al. S13-o-06 09:30-09:45 ROTHACKER Leo et al.S03-o-14 09:45-10:00 WILD Eva Maria et al. S13-o-07 09:45-10:00 TOUSSAINT Flora et al.

Coffee Break and Poster Session A

Session 03 - pretreatment protocols Session 13 - continental waterS03-o-15 10:30-10:45 BECK Lucile et al. S13-o-08 11:15-11:15 KEAVENEY Evelyn M et al.S03-o-16 10:45-11:00 CULLETON Brendan J. et al. S13-o-09 12:15-11:15 BLAIR Neal et al.S03-o-17 11:00-11:15 STARKOVICH Britt et al. S13-o-10 13:15-11:15 ROSENHEIM Brad et al.

Session 20 - modelling Session 17 - tracer of lifeS20-INV-01 11:15-11:45 BUTZIN Martin et al. S17-o-01 11:15-11:30 SALEHPOUR Mehran et al.S20-o-02 11:45-12:00 MILLER John et al. S17-o-02 11:30-11:45 GEORGIADOU Elisavet et al.S20-o-03 12:00-12:15 SIERRA Carlos A et al. S17-o-03 11:45-12:00 TANDOH Joseph Bremang et al.

Lunch Break and Poster Session A

Session 02 - physical measurement Session 16 - atmospheric impactS02-o-08 14:15-14:30 QUILES Anita et al. S16-o-01 14:15-14:30 GRAVEN Heather et al.S02-o-09 14:30-14:45 ZHAO Xiaolei S16-o-02 14:30-14:45 AULAGNIER Céline et al.S02-o-10 14:45-15:00 ZOPPI Ugo et al. S16-o-03 14:45-15:00 PAZDUR Anna et al.

Session 04 - specific compounds S16-o-04 15:00-15:15 PARK Junghun et al.

S04-o-01 15:00-15:15 WACKER Lukas et al. S16-o-05 15:15-15:30 MATSUZAKI Hiroyuki et al.S04-o-02 15:15-15:30 CHAVAN Shweta et al. S16-INV-06 15:30-16:00 LIMER Laura et al.S04-o-03 15:30-15:45 BRIDOUX Maxime et al. S04-o-04 15:45-16:00 FENG Xiaojuan et al.

Coffee Break and Poster Session AKEYNoTE-02 17:45-18:45 SPALDING Kristy

Table of conTenT

5

Wednesday July 11Room II Room IVSession 06 - reservoir effects Session 15 - atmospheric carbon cycleS06-o-01 08:15-08:30 OLSEN Jesper et al. S15-o-01 08:15-08:30 LEHMAN Scott et al.S06-o-02 08:30-08:45 MATOS MARTINS José M. et al. S15-o-02 08:30-08:45 DUSEK Ulrike et al.S06-o-03 08:45-09:00 SIANI Giuseppe et al. S15-o-03 08:45-09:00 KUC Tadeusz et al.S06-o-04 09:00-09:15 FINK David et al. S15-o-04 09:00-09:15 ZOTTER Peter et al.S06-o-05 09:15-09:30 FOHLMEISTER Jens et al. S15-o-05 09:15-09:30 VOGEL Felix Robert et al.S06-o-06 09:30-09:45 NORONHA Alexandra et al. S15-o-06 09:30-09:45 TURNBULL Jocelyn et al.S06-o-07 09:45-10:00 GENTY Dominique et al. S15-o-07 09:45-10:00 MAY Barbara et al.

Coffee Break and Poster Session B

Session 06 - reservoir effects Session 05 - statistical tools S06-o-08 10:30-10:45 BROOK George A. et al. S05-o-01 10:30-10:45 BRONK RAMSEY Christopher et al.S06-o-09 10:45-11:00 FERNANDES Ricardo et al. S05-o-02 10:45-11:00 BLAAUW Maarten et al.S06-o-10 11:00-11:15 CRAIG Ol. E et al. S05-o-03 11:00-11:15 MEADOWS John et al.

Session 09 - archaeology - Americas and Oceania S05-o-04 11:15-11:30 FERNANDES Ricardo et al.

S09-INV-01 11:15-11:30 SANZ Nuria S05-o-05 11:30-11:45 DEE Michael et al.S09-o-02 11:30-11:45 TUROSS Noreen et al. S05-o-06 11:45-12:00 STRANO Sarah et al.S09-o-03 11:45-12:00 HOLDAWAY Richard et al. S09-o-04 12:00-12:15 FONTUGNE Michel et al.

Lunch Break and Poster Session B

Thursday July 12 Room II Session 01 - calibrationS01-INV-01 08:15-08:45 REIMER Paula Jo et al. S01-o-02 08:45-09:00 HEATON Timothy John et al. S01-o-03 09:00-09:15 DURAND Nicolas et al. S01-o-04 09:15-09:30 FAIRBANKS Richard et al. S01-o-05 09:30-09:45 BRONK RAMSEY Christopher et al. S01-o-06 09:45-10:00 HOGG A et al. S01-o-07 10:00-10:15 HAJDAS Irka et al.


Room II Room IVSession 11 - continental paleo Session 12 - ocean carbon cycleS11-o-01 10:45-11:00 IMAMURA Mineo et al. S12-o-01 10:45-11:00 CATHALOT Cécile et al.

S11-o-02 11:00-11:15 DRAKE Brandon Lee S12-o-02 11:00-11:15 ZIGAH Prosper Kojo et al.S11-o-03 11:15-11:30 MICHCZYNSKA Danuta J. et al. S12-o-03 11:15-11:30 DRUFFEL Ellen et al.S11-o-04 11:30-11:45 PESSENDA Luiz Carlos Ruiz et al. S12-o-04 11:30-11:45 KUMAMOTO Yuichiro et al.S11-o-05 11:45-12:00 BLYTH Alison et al. S12-o-05 11:45-12:00 GUILDERSON Thomas et al.S11-o-06 12:00-12:15 ZHOU Weijian et al. S12-o-06 12:00-12:15 SKINNER Luke et al.S11-o-09 12:15-12:30 DAMBLON Freddy et al.


Session 11 - continental paleo Session 10 - oceanic paleoS11-o-07 14:30-14:45 ARSLANOV Khikmatulla et al. S10-o-01 14:30-14:45 RODGERS Keith S11-o-08 14:45-15:00 LEAVITT Steven et al. S10-o-02 14:45-15:00 FALLON Stewart et al.

Session 18 - cosmogenic nuclides S10-o-03 15:00-15:15 MARIOTTI Véronique et al.

S18-INV-01 15:00-15:15 HIPPE Kristina et al. S10-o-04 15:15-15:30 TISNÉRAT-LABORDE Nadine et al.S18-o-02 15:15-15:30 PETRENKO Vasilii et al. S10-o-05 15:30-15:45 MORTLOCK Richard et al.S18-o-03 15:30-15:45 BELMAKER Reuven et al. S10-o-06 15:45-16:00 SEPULCRE Sophie et al.S18-o-04 15:45-16:00 SADIER Benjamin et al.

Coffee Break and Poster Session BKEYNoTE-03 17:45-18:45 GENESTE Jean-Michel

GENERAL SCHEDULE

Table of conTenT

6

GENERAL SCHEDULEFriday July 13 Room II

Session 07 - PalaeolithicS07-o-01 08:15-08:30 HIGHAM T et al.

S07-o-02 08:30-08:45 TALAMO Sahra et al.

S07-o-03 08:45-09:00 BARSHAY-SZMIDT Carolyn et al.

S07-o-04 09:00-09:15 CONARD Nicholas et al.

S07-o-05 09:15-09:30 QUILES Anita et al.

S07-o-06 09:30-09:45 DOUKA Katerina et al.

S07-o-07 09:45-10:00 BARTON R. Nick E. et al.

S07-o-08 10:00-10:15 BAE Christopher J. et al.


Room II Room IV

Session 08 - archeology - Eurasia and Africa Session 14 - continental carbon cycleS08-o-01 10:45-11:00 CALCAGNILE Lucio et al. S14-INV-01 10:45-11:15 TRUMBORE Susan et al.

S08-o-02 11:00-11:15 DE CLERCQ Wim et al. S14-o-02 11:15-11:30 BAISDEN W Troy

S08-o-03 11:15-11:30 EDINBOROUGH Kevan et al. S14-o-03 11:30-11:45 TURCQ Bruno et al.

S08-o-04 11:30-11:45 ZAITSEVA Ganna et al. S14-o-04 11:45-12:00 HÖFLE Silke et al.

S08-o-05 11:45-12:00 VYBORNOV Aleksander et al. S14-o-05 12:00-12:15 GIERGA Merle et al.

S08-o-06 12:00-12:15 KUZMIN Yaroslav S14-o-06 12:15-12:30 EGLINTON Timothy et al.

S08-o-07 12:15-12:30 KUZUCUOGLU Catherine et al.

S08-o-08 12:30-12:45 JACOBSSON Piotr


Session 08 - archeology - Eurasia and Africa Session 19 - unusual applicationsS08-o-09 14:45-15:00 LEE Sharen et al. S19-INV-01 14:45-15:00 KRZEMNICKI Michael S. et al.

S08-o-10 15:00-15:15 OSLISLY Richard et al. S19-o-02 15:00-15:15 CULP Randy

S08-o-11 15:15-15:30 HEIMLICH Geoffroy et al. S19-o-03 15:15-15:30 SAKURAI Hirohisa et al.

S08-o-12 15:30-15:45 CLIST Bernard S19-o-04 15:30-15:45 HODGINS Gregory et al.

S08-o-13 15:45-16:00 BAE Kidong et al. S19-o-05 15:45-16:00 KULKOVA Marianna et al.

S08-o-14 16:00-16:15 SCHARF Andreas et al. S19-o-06 16:00-16:15 CALCAGNILE Lucio et al.

S08-o-15 16:15-16:30 PANYUSHKINA Irina et al.


17:00-17:30 IntCal12/Marine 12 ratification vote

17:30-18:00 Next conference Presentation

18:00-18:30 Meetting summary

Table of conTenT

7

INDEX BY SESSION

S1 Calibration ORAL POSTER SESSION B

S2 Advances in physical measurement techniques of Radiocarbon, and other long-lived radionuclides ORAL POSTER SESSION A

S3 Advances in radiocarbon pretreatment protocols ORAL POSTER SESSION A

S4 Specific compounds: Towards new applications ORAL POSTER SESSION A

S5 Statistical tools ORAL POSTER SESSION B

S6 Variations in radiocarbon reservoir effects ORAL POSTER SESSION B

S7 Radiocarbon dating and the Palaeolithic ORAL POSTER SESSION B

S8 Archeology - Eurasia and Africa ORAL POSTER SESSION B

S9 Radiocarbon and Archaeology of the Americas and oceania: Improving Chronologies and Theoretical Insights ORAL POSTER SESSION B

S10 oceanic paleoclimatology and paleoceanography ORAL POSTER SESSION B

S11 Continental paleoclimatology and paleohydrology ORAL POSTER SESSION B

S12 Insights into the ocean carbon cycle from radiocarbon measurements ORAL POSTER SESSION B

S13 Radiocarbon as a tracer of sources, fluxes and time in continental water ORAL POSTER SESSION A

S14 Continental carbon cycle ORAL POSTER SESSION B

S15 Atmospheric carbon cycle ORAL POSTER SESSION B

S16 Anthropogenic impacts ORAL POSTER SESSION A

S17 14C tracer of life ORAL POSTER SESSION A

S18 Cosmogenic nuclides ORAL POSTER SESSION B

S19 Unusual Applications of 14C measurement ORAL POSTER SESSION B

S20 14C and modeling ORAL POSTER SESSION A

8

INDEX BY AUTHORS

AA FEDORINA A.N. .................................. S08-O-04ABAY Esref ............................................ S08-P-251ABBASOVA Dinara ................................ S03-P-085ABDUL Nicole ..................... S01-O-04, S10-O-05ABRIL Gwenael ..................................... S14-P-319ACHOUNDONG Gaston ..... S11-P-295, S14-O-03ADAM Z. Csank .................................... S03-P-086ADKINS Jess F. ....................................... S01-O-07ADLER Jon ............................................ S03-P-087ADOLPHI Florian ............. S03-O-07, S01-P-144,

S01-P-147AERTS-BIJMA Anita T. ...... S03-P-046, S02-O-01,

S03-O-11AESCHBACH-HERTIG W. ....................... S13-P-098AGARWAL Deb ..................................... S14-P-324AGGARWAL Pradeep ............................ S13-O-04AGNIHOTRI Rajesh ............................... S12-P-303AIZAWA Jun ......................................... S11-P-285AKCAR Naki .......................................... S18-P-352AL-BASHAIREH Khaled ......................... S08-P-224ALARY Jean-François ........................... S02-P-009ALBERIC Patrick .................................... S13-P-111ALBRECHT Achim ................................. S20-P-136ALBUQUERQUE Ana Luisa S. ............... S11-P-294ALDANESE Raffaele .............................. S14-P-323ALEXANDRE Anne E. ............................. S03-O-05ALFORD Susan ................. S03-P-054, S10-P-261ALLENTOFT Morten .............................. S09-O-03ALLISON Colin ...................................... S15-P-341ALLISON Mead ...................................... S13-O-10ALPIN Ken ............................................ S06-P-176ALTENBURG Melanie ........ S03-P-082, S03-P-083ALVES Eduardo ................. S02-P-002, S10-P-258AN Zhisheng ........................................ S18-P-351ANDERSEN Gidske ............................... S11-P-282ANDERSEN Nils .................................... S14-P-322ANDERSON Robert ............................... S04-O-03ANDREWS Arlyn E. ............. S15-O-01, S15-P-340ANICETO Keila C. P. ............................... S14-P-317ANJOS Roberto ................ S02-P-002, S10-P-258ANSHITA Minoru .............. S02-P-004, S03-P-045ANTONELLI Christelle ...... S16-P-121, S16-P-127AO Hong .............................................. S18-P-351ARAGUÁS-ARAGUÁS Luis ..................... S13-O-04ARAMAKI Takafumi ........ S13-P-101, S12-P-301,

S13-P-104ARJOMAND Ali ..................................... S03-P-087ARMSTRONG Alix L. ............................. S11-P-292ARNOLD Maurice ............... S18-O-04, S07-P-206ARRIZABALAGA Alvaro ........................ S07-P-200ARROYO Juan ....................................... S17-P-131

ARSLANOV Khikmatulla ........................ S11-O-07ASAHARA Yoshihiro ............................. S13-P-109ASAI Kazumi ......................................... S13-P-110ASAI Kazuyoshi .................................... S13-P-110ASCOUGH Phillipa ............. S03-O-04, S04-P-090ASGEIRSSON Birgir ............................... S20-P-135ASMUSSEN Brit ..................................... S06-P-176AULAGNIER Céline ................................ S16-O-02AUMASSIP Ginette ............................... S11-P-273

BBACHA Tulu .......................................... S02-P-019BAE Christopher J. ............... S07-O-08, S08-O-13BAE Kidong ......................... S07-O-08, S08-O-13BAGGENSTOS Daniel ............................ S18-O-02BAISDEN W Troy .............. S14-O-02, S14-P-314,

S20-P-133BAKKE Jostein ...................................... S14-P-318BAKRAN-PETRICIOLI Tatjana ................ S10-P-259BALESDENT Jérôme ............................. S14-P-313BALL Richard J. ..................................... S03-P-044BALTENSPERGER Urs ............................. S15-O-04BAO Hongyan ....................................... S04-O-04BAR-MATTHEWS Myriam ..................... S07-P-210BARBECOT Florent ............. S13-O-02, S13-P-115BARBOSA Marcelo ............................... S11-P-277BARD Edouard ............... S01-INV-01, S01-O-02,

S01-O-03, S06-P-188, S10-O-06BAREŠIĆ Jadranka ................................ S10-P-264BARNABÁS István ................................. S16-P-128BARROS Márcia .................................... S14-P-317BARRY Chris D. ...................................... S13-O-08BARSHAY-SZMIDT Carolyn .................... S07-O-03BARTA Peter ......................................... S11-P-293BARTALINI S. ...................................... KEYNOTE 01BARTH Monika O. ................................. S14-P-317BARTOLOMEI Paolo .............................. S02-P-018BARTON R. Nick E. ................................. S07-O-07BARZILAI Omry ................ S03-P-076, S07-P-210BASARAN Mihriban ............................... S08-O-07BATTAGLIA Michael ............................. S02-P-007BATTIN Tom ........................................... S03-O-01BAUDRON Paul .................................... S13-P-115BAUMGARTNER Timothy ..................... S10-P-269BAUSKA Thomas ................................... S18-O-02BAVAY Dominique .......... S03-P-080, S02-O-08,

S02-P-021, S13-P-112BAYLISS Alex ................... S01-INV-01, S08-P-229BEAUPRE Steven R. ........ S03-P-030, S03-P-031,

S12-P-302, S12-P-310, S13-O-10, S14-P-314BEAVAN Nancy ..................................... S08-P-212BECK J Warren ................ S01-INV-01, S18-P-351

InDeX bY aUTHoRS

9

INDEX BY AUTHORSBECK Lucile ... S03-O-15, S07-P-195, S07-P-196,

S07-P-205BEECKMAN Hans .................................. S08-P-252BEEN Henk A. ... S02-O-01, S03-O-11, S03-P-046BEER Juerg ......................... S18-O-03, S18-P-345BEITENBACH Sebastian F. M. ................. S01-O-07BEKADDOUR Toufik .............................. S18-P-344BELMAKER Reuven ............. S18-O-03, S18-P-345BELMECHERI Soumaya ........................ S11-P-278BEN MOHAMED A. ............................... S02-P-024BENCH Graham .................................... S15-P-336BENEDETTI Lucilla ................................. S18-O-04BENTALEB Ilham ................. S08-O-10, S16-P-121BERAAOUZ El Hassane ......................... S13-P-108BERAMENDI-OROSCO Laura ............. S16-P-124,

S16-P-130BERGONZINI Laurent ........................... S13-P-111BERNA Francesco ................................. S07-P-210BERNALDO DE QURIOS Federico ........ S07-P-200BERNARDES Marcelo ........................... S14-P-319BERNARDONI Vera .......... S15-P-330, S15-P-336BERNASCONI Stefano M. ................... S04-P-094,

S14-O-05, S14-P-318BERTHIER Bernard ................................. S02-O-08BERTRAND Chanda .............................. S12-P-309BESOMBES Jean-luc ............................. S15-P-331BESSUDNOV Alexander ....................... S07-P-204BHUSHAN Ravi ..................................... S12-P-303BIAGETTI Stefano ................................. S05-P-164BICHLER Max ........................................ S18-P-349BIECHELE Carol ................ S01-O-07, S03-P-058,

S19-P-362BINDER Michaela ................................. S03-P-084BIRCH Steven ....................................... S05-P-162BIRD Michael ......................................... S03-O-04BIRKHOLZ Axel ..................................... S14-P-318BLAAUW Maarten ................................. S05-O-02BLACKWELL Paul G. ............................ S01-INV-01BLAIR Neal ............................................. S13-O-09BLAMART Dominique ........ S06-O-07, S07-P-196BLANC-VALLERON Marie-madeleine .. S08-P-234BLATTMANN Thomas ........................... S12-P-307BLEICHER Niels ...................................... S03-O-07BLUSZTAJN Jerzy ................................. S12-P-308BLYTH Alison ......................................... S11-O-05BOËDA Eric ........................................... S09-P-253BOARETTO Elisabetta ..... S03-P-076, S19-P-360,

S07-P-210BOCQUENTIN Fanny ............................ S03-P-076BOECKX Pascal .................... S03-O-03, S14-O-04BOLOGNA Michele .............................. S02-P-012BOMBARDIERI Luca .............................. S03-P-056

BONANI Georges ............ S01-O-07, S03-P-058, S19-INV-01, S19-P-362

BONDIOLI L. .......................................... S06-O-10BONNAILLIE Patrick .............................. S07-P-205BOPP Laurent ........................................ S10-O-03BORDIER Louise .................................... S10-O-04BORONKAY Stephen ............................ S02-P-003BOROTTI FILHO Marcos Antonio ........ S11-O-04,

S11-P-281BORRI S. ............................................. KEYNOTE 01BÖSCHEN Tebke ................................... S10-P-266BOUCHAOU Lhoussaine ...................... S13-P-108BOUDIN Mathieu .............. S03-O-03, S03-P-078BOULET Béatrice .................................. S16-P-127BOUQUILLON Anne ............................. S08-P-234BOURDIN Clément ................................ S06-O-07BOURGEOIS Jean ................................. S08-P-211BOURGES François ................................ S13-O-05BOURLÈS Didier Louis ........ S18-O-04, S18-P-350BOURLAND Nils ................................... S08-P-252BOUROVA Nd ....................................... S08-P-241BOUTTES Nathaëlle .............................. S10-O-03BOUZOUGGAR Abdeljalil ...................... S07-O-07BOWLES Kathy ...................................... S12-O-01BOYÉ Marie ............................................ S10-O-04BOYER Marina ...................................... S19-P-353BRÄUER Tino ........................................ S14-P-322BRÄUNING Achim ................................. S08-O-14BRABEC Marek ....................................... S05-O-04BRACCI Susanna ................................... S03-P-053BRAILSFORD Gordon ......... S18-O-02, S05-P-165BRAIN S. ................................................ S11-P-274BRAIONE Eugenia .......... S02-P-020, S03-P-079,

S08-P-245, S19-O-06BRAUER Achim ................... S01-O-05, S01-P-139BREIER Robert .................... S02-P-012, S13-O-04BRIDOUX Maxime ................................. S04-O-03BROCK Fiona ................... S03-P-049, S07-P-198,

S08-P-247, S01-O-05, S01-P-139, S03-O-02, S03-P-029, S03-P-036, S08-P-227, S08-P-255

BRONK RAMSEY Christopher ............. S01-INV-01, S01-O-05, S01-O-06, S01-P-139, S03-P-029, S05-O-01, S05-O-05, S05-P-160, S07-O-01,

S07-O-06, S08-O-09, S08-P-227, S08-P-229, S08-P-247, S08-P-228, S08-P-255

BROOK Edward ..................................... S18-O-02BROOK George A. ................................. S06-O-08BROWN K. ............................................. S12-P-312BRYANT Charlotte ........... S01-O-05, S01-P-139,

S03-P-060, S03-P-061, S04-P-090BUCHHOLZ Bruce ................................ S04-P-092BUCK Caitlin E .................................... S01-INV-01BUCKLEY Brendan ................................ S08-P-212

InDeX bY aUTHoRS

INDEX BY AUTHORS

10

BUCZAK Kathrin ................................... S18-P-349BUDD Chelsea ...................................... S06-P-181BUIZERT Christo .................................... S18-O-02BUNCE Michael ..................................... S09-O-03BUONINCONTRI Mauro ........................ S08-P-250BURG Avihu .......................................... S13-P-103BURR George S. ............... S03-O-13, S03-P-066,

S18-P-346BURTON Joshua ............. S03-P-030, S03-P-031,

S12-P-311BUSH Shari ........................................... S10-P-263BUSO JR Antonio Alvaro .... S11-O-04, S11-P-281BUTZIN Martin ................................... S20-INV-01BUZHILOVA Alexandra ......................... S06-P-172

CCAFFY Ingrid S02-P-021, S03-P-080, S13-P-112CAFORIO Lucia ............... S03-P-053, S03-P-055,

S03-P-056CALCAGNILE Lucio .......... S02-P-020, S03-P-044,

S03-P-079, S08-O-01, S08-P-230, S08-P-244, S08-P-245, S19-O-06, S19-P-359

CALZOLAI Giulia ............. S03-P-055, S15-P-330, S15-P-336

CAMBALIZA Maria Obiminda ............... S15-O-06CAMOIN Gilbert .................................... S01-O-03CANCIO P. .......................................... KEYNOTE 01CAMPS Marta ....................................... S07-P-200CANDUCCI Chiara ................................ S02-P-018CANOSA Elyse ...................................... S19-P-361CAO Fang ............................................. S03-P-039CAO Li ................................. S01-O-04, S10-O-05CAPANO Manuela ........... S03-O-08, S06-P-191,

S08-P-248, S08-P-250, S17-O-03, S14-P-323, CAQUINEAU Sandrine ..... S10-P-269, S14-P-316CARDOZO Laio ................. S02-P-002, S10-P-258CAREL Mélanie ...................................... S06-O-03CARMI Israel .......................................... S13-O-01CARPELAN Christian ............................ S06-P-177CARRARESI Luca ................................... S03-P-055CARRILLI J. ............................................. S06-O-04CARRIQUIRY José ................................. S06-P-184CARSON Cantwell ................................ S02-P-019CARVALHO Carla Regina .. S02-P-002, S10-P-258CASTALDI S. ........................................... S17-O-03CASTALDO Nicola ................................ S08-P-250CATHALOT Cécile ............... S12-O-01, S13-P-105CATTANEO Cristina .............................. S19-P-359CAUQUOIN Alexandre ......................... S01-P-146CHABBI Abad ....................................... S14-P-315CHAMBERS Frank ................................. S11-P-274CHANG C. .............................................. S08-O-15CHAPRON Emmanuel .......................... S13-P-111

CHARMASSON Sabine ......................... S16-P-121CHATTERS Jim ...................................... S03-P-087CHAVAN Shweta ................................... S04-O-02CHEKHA Vitaly P. .................................... S11-O-09CHEN Yue-gau ...................................... S03-O-13CHENG Li .............................................. S18-P-351CHENG Peng ........................................ S03-P-070CHERKINSKY Alexander . S02-P-005, S03-P-051,

S05-P-164, S06-O-08, S11-O-04CHERNOV Sergei ................................... S11-O-07CHHEM Keith Rethy ............................. S08-P-212CHIARI Massimo ............... S15-P-330, S15-P-336CHILDRESS Laurel ................................. S13-O-09CHIOTTI Laurent .............. S03-O-15, S07-O-06,

S07-P-202CHMURA Gail ....................................... S06-P-178CHOE Kyumin .................. S03-P-040, S03-P-041CHOI H.W. .............................................. S16-O-04CHRÓST Leszek .................................... S08-P-235CHRISTEN J. Andres ............................... S05-O-02CHRISTL Marcus ................ S04-O-01, S18-O-03,

S18-P-343, S18-P-345CISNEROS-DOZAL Luz Maria ............ S03-P-060,

S04-P-090CLIST Bernard ........................................ S08-O-12COHEN Marcelo Cancela Lisboa ......... S11-P-281COMBY Clothilde ........... S02-P-021, S03-P-080,

S13-P-112CONARD Nicholas ................................ S07-O-04CONCEIÇÃO Marcela ....... S11-P-277, S14-P-321COOK Gordon ................ S01-P-142, S01-P-143,

S05-P-162, S08-P-229COOKE Ashley ...................................... S08-P-228COPPOLA Alysha ................................. S12-P-306CORBINEAU Remi .................................. S03-O-05CORCHO ALVARADO Jose Antonio ...... S13-O-02CORCHON Soledad .............................. S07-P-205CORDEIRO Renato Campello ........... S11-P-277,

S11-P-294, S14-P-316, S14-P-317, S14-P-321CORVAGLIA Carla ................................. S08-P-245CORVAGLIA Elisa ................................... S08-O-01COSSONNET Catherine ....................... S16-P-127COSTA Renata L. ................................... S11-P-294COUDERT Magali ................................. S03-P-033COUNTS Ronald ................................... S11-P-271COURTIN-NOMADE Alexandra ............ S11-P-278COUSINS Lisa M. ................................... S02-P-009COZIC Julie ........................................... S15-P-331COZZUOL Mario Alberto ..................... S03-P-051CRÉPIN Laurent .................................... S07-P-208CRAIG Oliver E. ................... S06-O-10, S08-P-249CRANN Carley Angela .......................... S06-P-171CROSTA Xavier ...................................... S04-O-03

InDeX bY aUTHoRS

INDEX BY AUTHORS

11

CRUCIFIX Michel .................................. S05-P-159CUIF Jean-Pierre .................................... S03-O-15CULLETON Brendan J. ........................... S03-O-16CULP Randy ....................... S02-P-005, S19-O-02CURRIE Margaret .................................. S03-P-060CYREK Krzysztof ................................... S07-P-207CZERNIK Justyna .................................. S11-P-282CZIMCZIK Claudia ............ S03-P-071, S15-P-336CZY

.ZEWSKI Lukasz ............................... S07-P-207

DD’ANDREA William J. ............................ S06-P-173D’ELIA Marisa .................. S02-P-020, S03-P-044,

S03-P-079, S08-O-01, S08-P-244, S08-P-245, S19-O-06, S19-P-359

DAMBLON Freddy .......... S03-P-047, S07-P-199, S11-O-09

DANTAS Mario Andre Trindade ........... S03-P-051DARAGON Frederique .......................... S08-O-14DAVID Bruno ........................................ S06-P-176DAVIS Kenneth ...................................... S15-O-06DE CLERCQ Wim ................................... S08-O-02DE LA RASILLA Marco .......................... S07-P-200DE LANGHE Kaat .................................. S08-P-211DE MARINIS Raffaele C. ......................... S05-O-03DE MULDER Guy ................................... S08-O-02DE NATALE P. .................................... KEYNOTE 01DE OLIVEIRA Paulo Eduardo ................ S11-P-281DE POL-HOLZ Ricardo ....... S06-O-03, S06-P-174DE ROOIJ Marietta ................................ S02-O-01DE SAULIEU Geoffroy ........................... S09-P-256DE-POL HOLZ Ricardo .......................... S06-O-03DEBLASIS Paulo .................................... S09-P-257DECRI Anna .......................................... S08-P-230DEE Michael .. S05-O-05, S08-P-227, S08-P-228,

S08-P-232, S08-P-246DEGEAI Jean-Philippe ........................... S08-O-07DEGUZMAN Mark ................................ S02-P-019DELANNOY Jean Jacques ..................... S18-O-04DELILLE Bruno ....................................... S10-O-04DELLUC Brigitte .................................... S07-P-196DELLUC Gilles ....................................... S07-P-196DELMOTTE Marc ................ S13-O-05, S15-P-335DELQUE-KOLIC Emmanuelle ............ S02-P-021,

S03-O-09, S03-P-080, S13-P-112DERENDORP Leonie ............................. S15-P-336DERENNE Sylvie ................................... S14-P-313DERRIEN Delphine ............................... S14-P-313DESCHAMPS Marianne ......................... S07-O-03DESCHAMPS Pierre ............. S01-O-03, S10-O-06DESHPANDE R. D. ................................. S13-P-098DESJARDINS Thierry ........... S11-P-295, S14-O-03

DEWALD Alfred .................................... S03-P-077DEZILEAU Laurent ............................... S16-P-121DI LERNIA Savino ................................. S05-P-164DI PASQUALE Gaetano ......................... S08-P-250DIAGNE Tomas ..................................... S19-P-363DIAZ-GOMEZ Claudia I. ........................ S11-P-292DICKENS Angela ................................... S14-O-06DICKSON Andrew ................................. S18-O-02DIKOVA M.A. ......................................... S08-P-217DILLMANN Iris ...................................... S18-P-349DILLMANN Philippe .............................. S03-O-09DING Ping ... S11-P-276, S12-P-299, S16-P-120,

S18-P-342DING Xingfang ................ S02-O-02, S11-P-276,

S12-P-299, S16-P-120, S18-P-342DINNIS Rob ........................................... S07-O-06DITTMAR Thorsten ............................... S04-P-094DLUGOKENCKY Edward J. .................... S15-P-340DOI Naomi ........................................... S08-P-243DOLBY Nic ............................................ S06-P-176DOMETT Kate ....................................... S08-P-212DONG Kejun S02-P-001, S02-P-011, S02-P-016DOUARIN Melanie ............................... S06-P-193DOUCET Jean-Louis ............................. S08-P-252DOUKA Katerina ............. S03-P-049, S07-O-01,

S07-O-06, S07-P-199DOUVILLE Eric .................... S06-O-07, S10-P-270DOWDESWELL Julian A. ....................... S03-P-057DOWNEY Sean ...................................... S08-O-03DRAKE Brandon Lee .............................. S11-O-02DRENZEK Nicholas ................................ S14-O-06DREVES Alexander .......... S03-P-073, S06-O-09,

S10-P-266, S13-O-06DROZDOV Nicolai I. .............................. S11-O-09DRUCKER Dorothée ............................. S07-P-208DRUFFEL Ellen ................ S03-P-038, S06-P-184,

S12-O-03, S12-P-297, S12-P-306, S12-P-309, S12-P-310

DRYSDALE R. N. .................................... S06-P-169DUEKER Stephen ............... S02-O-04, S03-P-067DULINSKI Marek .................................... S13-O-03DUMOULIN Jean-Pascal .. S02-P-021, S03-O-09,

S03-P-080, S06-O-07, S07-P-196, S11-P-278, S12-P-304, S13-P-112

DUNBAR Robert ................................... S12-P-297DUNGAIT Jennifer ................................ S04-P-090DUNN Gregory ..................................... S15-P-341DURAND Nicolas ............... S01-O-03, S02-P-021DUSEK Ulrike ..................... S15-O-02, S15-P-336DUTTA Koushik .................................... S12-P-303DVORACEK D. ....................................... S02-P-005DVORNIKOV Eduard Pavlovitch ........... S08-P-211

InDeX bY aUTHoRS

INDEX BY AUTHORS

12

EEDINBOROUGH Kevan .......................... S08-O-03EDWARDS R. Lawrence ...................... S01-INV-01ÉGASSE Céline ...................................... S14-P-313EGLINTON Timothy .......... S04-O-04, S12-P-302,

S12-P-307, S12-P-308, S12-P-312, S14-O-06, S17-P-132

EIRÍKSSON Jón ....................................... S06-O-01EIZENBERG Laura .................................. S07-O-03EKSTRÖM Peter .................................... S16-P-117EL HADDAD Imad .............. S15-O-04, S15-P-331ELALOUF Jean-marc ............................. S07-O-05ELDER Kathryn L. .............. S12-P-311, S15-P-336ELLIOT Mary ......................................... S06-P-193ELLIOTT F. M. ........................................ S04-P-090ELLIOTT Frank ...................................... S03-P-060ELSÄSSER Christoph ............................ S20-P-135EMANUELE Guy .................................... S18-O-02EMERY-BARBIER Aline ........................... S08-O-07EMMENEGGER Lukas ........................... S16-P-118ENGOVATOVA Asya .............................. S08-P-221ENTERS Dirk .......................................... S05-P-161ERAMO Giacomo ................................. S08-P-236ESPOSITO Massimo .............................. S02-P-018

FFACORELLIS Yorgos .............................. S07-P-198FAHRNI Simon Martin ...... S01-P-149, S01-P-150FAIRBANKS Richard ............. S01-O-04, S10-O-05FAIRBANKS-HARRIS Theresa .................. S19-O-04FAIVRE Sanja ......................................... S10-P-259FALLON Stewart ................ S03-P-054, S06-O-04,

S08-P-212, S10-O-02, S10-P-261, S10-P-264, S12-O-06, S16-P-125

FASCHING Christina .............................. S03-O-01FATTORE L. ............................................. S06-O-10FAVIER Charly ........................................ S08-O-10FEDI Maria Elena ........ KEYNOTE 01, S03-P-053,

S03-P-055, S03-P-056, S15-P-330, S15-P-336FEIGE Jenny .......................................... S18-P-349FEJGL Michal ........................................ S01-P-141FENG Xiaojuan .................... S04-O-04, S14-O-06FENTON C.R. ......................................... S18-P-348FENWICK Pavla ...................................... S01-O-06FERGUSON Julie ............. S03-P-072, S06-P-184,

S06-P-185FERNANDES Ricardo ....... S03-P-078, S05-O-04,

S06-O-09, S06-P-190FERNEX François ................................... S13-O-07FERREIRA Vicente ................................. S10-P-269FIEDEL Stuart ........................................ S07-P-201FIELD David .......................................... S10-P-269

FIFIELD Keith ........................................ S16-P-125FIGUTI Levy .......................................... S09-P-257FINK David .... S06-O-04, S18-P-345, S18-P-348,

S18-P-347FIORETTO Antonietta .......................... S14-P-323FISCHER Peter ....................................... S03-O-14FOHLMEISTER Jens ......... S06-O-05, S06-P-169,

S13-P-098FONTES Daiana .................................... S14-P-317FONTUGNE Michel ........... S08-O-07, S08-O-10,

S09-P-253, S09-P-254, S09-O-04, S12-P-300, S16-P-121

FORTEA Javier ...................................... S07-P-200FOURRÉ Elise ........................................ S16-P-121FOY Robert H. ....................................... S13-O-08FRANCISQUINI Mariah Izar ................... S11-P-281FRANK Norbert ................ S09-P-253, S10-P-270FRANZ Peter .......................................... S18-O-02FREEMAN Stewart P. H. T. . S03-P-060, S19-P-358FRIEDRICH Michael ...... S01-INV-01, S01-P-149,

S03-O-07FRIGG Silvio .......................................... S08-P-232FROHLICH François .............................. S08-P-234FRUMKIN Amos .................................... S07-P-210FU Dongpo .. S02-O-02, S11-P-276, S12-P-299,

S16-P-120, S18-P-342FUJIKI Toshiyuki .................................... S11-P-285FUJITA Masaki ...................................... S08-P-243FUJITAKE Nobuhide ............................. S13-P-104FUKASAWA Masao ................................ S12-O-04FULLER Benjamin ................................. S19-P-356FULLER Benjamin Thomas ................... S01-P-149FÜLÖP Réka-Hajnalka ...... S03-P-059, S03-P-077FURU Enikö .......................................... S16-P-129

GGABALLO Valentina ........ S02-P-020, S03-P-079,

S08-O-01, S08-P-245GAGAN M. K. ........................................ S06-P-169GAGNON Alan .................. S02-P-025, S12-P-311GAKUHARI Takashi ............................... S08-P-243GALLET Xavier ...................................... S08-P-234GALLI I. ............................................. KEYNOTE 01GALY Valier ........................ S04-O-04, S13-O-10,

S14-O-06GANDOLFO Nathalie ..... S03-P-033, S03-P-037,

S08-O-11, S19-P-353GANESHRAM Raja S. ............................ S03-P-061GAO Pan ........................... S03-P-069, S03-P-072GARATE MAIDAGAN Diego ................. S07-P-205GARCIA-AROSTEGUI Jose Luis ............. S13-P-115GARCIA-TENORIO Rafael ...................... S16-P-119GARNAUD Sébastien ........................... S19-P-363

InDeX bY aUTHoRS

INDEX BY AUTHORS

13

GARNETT Mark H. ............ S03-P-034, S03-P-060GARRETA Vincent ................................. S06-P-188GASIOROWSKI Michal .......................... S05-P-158GAUTHIER Agnès .................................. S08-O-07GAUTHIER Caroline ............................... S03-O-15GENBERG Johan .............. S03-O-10, S15-P-336,

S16-P-116GENESTE Jean Michel . KEYNOTE 03, S07-O-05,

S18-O-04GENTY Dominique ........... S06-O-07, S07-O-05,

S07-P-195, S07-P-196, S13-O-05GEORGIADOU Elisavet ....... S16-P-116, S17-O-02GESHI Nobuo ....................................... S11-P-284GHALEB Bassam .................................... S06-O-07GHEYLE Wouter .................................... S08-P-211GHOLAMREZA Javahery ...................... S02-P-009GIACOMO Jason ................ S02-O-04, S03-P-067GIBERT Elisabeth ................................... S13-O-02GIERGA Merle ... S01-O-07, S04-P-094, S14-O-05GIFFONI Massimo ................................. S19-O-06GIGLI Stefania ....................................... S06-P-191GILLET Jean-François ......... S08-O-10, S08-P-252GILLON Marina ...................................... S13-O-02GILMAN ROMANO David ...................... S03-O-17GIOSAN Liviu ...................... S12-P-308, S14-O-06GIRAUD Xavier ..................................... S20-P-134GISCARD Marlene D. ............................ S18-P-346GIUSFREDI G. .................................... KEYNOTE 01GLAVATSKAYA Elena ............................. S06-P-183GLYKOU Aikaterini ............................... S08-P-249GLYNN Danielle .................................... S12-P-297GOLDSTEIN Steven .............................. S13-P-114GOMES Paulo Roberto ..... S02-P-002, S10-P-258GOMES NÍCOLI Iêda ............................. S16-P-117GOMEZ-MARTINEZ Isabel S16-P-119, S17-P-131GONÇALVES Isabel ................................ S17-O-02GÖNCZI Renáta .................................... S03-P-081GONTIER Gilles ..................................... S16-P-127GONZALES-ROUBAUD Cécile .............. S10-P-270GONZALEZ-HERNANDEZ Galia ........ S16-P-124,

S16-P-130GONZE Marc-André .............................. S16-O-02GOOD Irene ......................................... S08-P-228GORCZYCA Zbigniew ........................... S15-O-03GORYACHEV A ....................................... S08-O-15GOSLAR Tomasz ............... S08-P-215, S11-P-282GOTANDA Katsuya ............. S01-O-05, S01-P-139GOTTDANG Andreas ............................ S02-O-05GOURLET-FLEURY Sylvie ...................... S08-P-252GRADZINSKI Michal ............................. S11-P-283GRAVEN Heather ............ S15-P-338, S15-P-341,

S16-O-01, S20-P-134

GRIFFIN Sheila S03-P-072, S03-P-086, S12-O-03, S12-P-309

GRIFFITH David .............. S12-P-307, S12-P-312, S17-P-132

GRIFFITH Fritz ....................................... S06-P-171GRIFFITHS Michael L. ........................... S06-P-169GRIGGS Carol ....................................... S08-P-247GRIGORIEV F. ......................................... S08-O-15GROEN C. Peter ..................................... S02-O-01GROOTES Pieter M. ....... S01-INV-01, S01-P-153,

S03-P-078, S05-O-04, S06-O-09, S06-P-190, S08-O-04, S13-O-06, S14-P-322

GROS Valérie ........................................ S15-P-335GRUBER Nicolas ................. S16-O-01, S20-P-134GSCHWEND Philip ............................... S17-P-132GUAN Yongjing .................................... S08-P-216GUENDOUZ Abdelhamid .................... S13-P-107GUENTHER Douglas .............................. S15-O-06GUIBERT Pierre ..................................... S11-P-273GUILDERSON Thomas ..... S01-INV-01, S04-O-03,

S12-O-05, S12-P-310, S15-P-338, S15-P-340, S15-P-341

GUILLES Marcela C. C. .......................... S14-P-317GUILLOU Herve .................................... S11-P-278GULLIVER Pauline ........... S03-P-060, S03-P-088,

S13-P-099GUPTA S. K. ........................................... S13-P-098GUR-ARIEH Shira ............. S07-P-210, S19-P-360GURNEY Kevin ....................................... S15-O-06GURRIARAN Rodolfo ............................ S16-P-127GUSTAFSSON Örjan ............................. S15-P-336GUTIERREZ Dimitri ............................... S10-P-269GÜTTLER Dominik ............ S01-P-144, S03-O-07,

S16-P-128

HHAESAERTS Paul ............ S03-P-047, S07-P-199,

S11-O-09HAFLIDASON Haflidi ...... S01-INV-01, S10-P-262HAIN Stéphane .............. S02-P-021, S03-P-080,

S13-P-112HAJDAS Irka .. S01-INV-01, S01-O-07, S03-P-058,

S03-P-081, S04-P-094, S05-P-166, S13-P-098, S14-O-05, S14-P-318, S16-P-129, S18-P-352,

S19-INV-01, S19-P-362HAJNALOVA Maria ............................... S11-P-293HÅKANSSON K. ..................................... S17-O-01HALCROW Sian .................................... S08-P-212HALL Grant ........................................... S19-P-363HALL-SPENCER Jason ........................... S10-P-270HALTIA-HOVI Eeva ............................... S06-P-192HAMELIN Bruno .................................... S01-O-03

InDeX bY aUTHoRS

INDEX BY AUTHORS

14

HAMILTON Derek ........... S05-P-162, S05-P-163, S08-P-212

HANDA Hiroko ..................................... S13-P-100HANSON Danielle C. ............................. S03-O-16HAO Changtong .................................. S02-P-009HARAGUCHI Tsuyoshi ........ S01-O-05, S01-P-139HARDEN Jennifer ................................. S14-P-324HARDIMAN Mark .................................. S05-P-160HARTH Christina ................................... S18-O-02HARTZ Sönke ....................................... S08-P-249HATTÉ Christine ............. S01-INV-01, S10-O-04,

S12-P-300, S14-P-313HAUG Gerald H. .................................... S01-O-07HAYASHIDA Akira ................................. S04-P-091HAYES Patrick ........................................ S15-O-04HE Ming ....... S02-P-001, S02-P-011, S02-P-016HEATON Timothy John .... S01-INV-01, S01-O-02HEBERT Didier ....................................... S16-O-02HEDGES Robert E. M. ..... S04-O-02, S04-P-089,

S06-O-10, S07-P-197HEIMLICH Geoffroy ............................... S08-O-11HEINEMEIER Jan .............. S02-O-10, S06-P-189,

S08-P-242, S08-P-249HEINZE Stefan ................ S03-P-059, S03-P-077,

S14-P-320HELLSTROM J. C. ............. S06-O-07, S06-P-169,

S07-P-196HENDERSON Gideon M. ....................... S01-O-03HENDRICKSON Mitch .......................... S08-P-219HENLEY Sian F ...................................... S03-P-061HENSEL Zdzisław ................................. S08-P-235HERCMAN Helena .......... S03-P-043, S05-P-158,

S11-P-283HERNANDO ALVAREZ Clara ................. S07-P-205HERON Carl P. ....................................... S08-P-249HERSHKOVITZ Israel ............................. S07-P-210HIGHAM Charles .................................. S08-P-218HIGHAM Thomas F. G. ........ S03-O-02, S04-O-02,

S06-O-10, S06-P-172, S06-P-181, S07-O-01, S07-O-04, S07-O-06, S07-P-197, S07-P-198,

S07-P-199, S07-P-200, S07-P-201, S08-P-218, S08-P-255, S19-P-355

HILASVUORI Emmi ............................... S08-P-222HILLENBRAND Claus-dieter ................. S03-P-057HIPPE Kristina ................. S18-INV-01, S18-P-343HIROTA Akinari ..................................... S13-P-100HODGINS Gregory ............ S03-O-17, S19-O-04,

S19-P-361HOFFMANN Helene .............................. S15-O-07HÖFLE Silke .... S03-P-077, S14-O-04, S14-P-320HÖFLMAYER Felix .................................. S03-O-14HOGEVEEN Peter .................................. S12-P-305HOGG Alan G. .................. S01-INV-01, S01-O-06

HOGUE Joshua ...................................... S07-O-07HOLDAWAY Richard .............................. S09-O-03HOLM Elis ............................................. S16-P-119HOLMES R. Max ..................................... S04-O-04HOLY Karol ....................... S02-P-012, S15-P-333HONDA Maki ......................................... S16-O-05HONG Gi-hoon .................................... S12-P-301HONG Wan . S01-P-145, S01-P-152, S03-P-065,

S03-P-068, S04-P-091, S06-P-186, S16-O-04HOOD Amber ...................................... S08-P-227HOPER Stephen T. ................................ S03-P-035HORVATINCIC Nada ......... S10-P-259, S13-P-099HOSHINO Yasuharu .......... S02-P-004, S11-P-284HOSHIZUMI Hideo ............................... S19-P-358HOSONO Takahiro ............................... S13-P-109HOTCHKIS Michael ............................... S02-P-003HOU Juzhi ............................................ S06-P-173HU Chaoyang ........................................ S06-O-06HUA Quan .. S06-P-169, S06-P-170, S08-P-219,

S11-O-05, S18-O-02HUANG Yongsong ............................... S04-P-096HUBLIN Jean-Jacques ........ S03-P-047, S07-O-02HUGHEN Konrad A. ........ S01-INV-01, S01-O-02,

S14-O-06HUGHES P. ............................................ S18-P-348HÜLS Christian Matthias ...................... S03-P-073HÜLS Matthias ..................................... S03-P-078HUTZLER Aurore .................................. S18-P-346HWANG Jeomshik ................................ S12-P-308

IILKMEN Erhan ...................................... S02-P-019IMAMURA Mineo .................................. S11-O-01INGALLS Anitra ...................................... S04-O-03INUI Emiko ............................................ S19-O-03IRIARTE María-josé ............................... S07-P-200ISRADE-ALCANTARA Isabel ................... S13-O-07ITAHASHI Yu ......................................... S08-P-243ITOH Shigeru ...................... S08-P-243, S11-O-01IVY-OCHS Susan ........... S18-INV-01, S18-P-343,

S18-P-352

JJACOBI Roger ........................................ S07-O-01JACOBSSON Piotr .................................. S08-O-08JACOMB Christopher ............................ S09-O-03JAFFREZO Jean-Luc ............................. S15-P-331JAILLET Stéphane ................................. S18-O-04JAKIMAVIČIŪTĖ-MASELIENĖ Vaidotė ...... S13-P-106JAMRICHOVA Eva ................................. S11-P-293JANOVICS Róbert ............. S03-P-081, S16-P-128JANSEN Henk G. .................................... S02-O-01JAY Mandy ............................................ S05-P-163

InDeX bY aUTHoRS

INDEX BY AUTHORS

15

JAYA Diego ........................................... S08-P-256JEAN-BAPTISTE Philippe ...................... S16-P-121JENKINS William .............. S04-P-093, S12-P-311JESKOVSKY Miroslav ............................. S02-P-012JETTMAR Barbara ................................. S11-P-279JEZEQUEL Didier .................................. S13-P-111JIANG Shan ....................... S02-P-011, S02-P-016JIMENEZ Jose-Luis ................................ S15-O-04JOHN Stephan ..................................... S14-P-320JOHNSON Kathleen R. ... S06-O-06, S06-P-169,

S06-P-185JOMURA Mayuko ................................. S14-P-326JONES Richard ...................................... S01-O-06JONKER Wigger .................................... S12-P-305JOUZEL Jean ........................................ S01-P-146JULL A. J. Timothy .......... S03-P-081, S08-P-215,

S11-P-292, S18-P-346JUNGNER Högne ................................. S11-P-273

KKABEL Karoline ..................................... S06-P-182KAISER Johannes ................................. S05-P-165KAISER K. Felix .................................... S01-INV-01KAIZER Jakub ....................................... S02-P-012KALTNECKER Evelyne ..... S07-P-196, S07-P-205,

S07-P-206KANG Jin .......................... S03-P-040, S03-P-041KANIA Jaroslaw ..................................... S13-O-03KÄPPELER Franz ................................... S18-P-349KAPUSTA Marcin ................................... S13-O-03KARION Anna ........................................ S15-O-06KARKANAS Panagiotis ......................... S07-P-198KATAGIRI Chiaki .................................... S08-P-243KATO Kazuhiro ............... S02-P-004, S03-P-045,

S15-P-334, S19-O-03KATSUKI Kota ........................................ S06-P-186KAWANO Takeshi .................................. S12-O-04KAZAHAYA Kohei ................................. S13-P-100KEATES Susan G. ................................... S07-P-194KEAVENEY Evelyn M. ............................. S13-O-08KEELING Ralph S15-P-338, S15-P-341, S18-O-02KEINONEN Juhani ................................ S03-P-048KELLER Elizabeth Diane ....................... S20-P-133KENNETT Douglas J. .............................. S03-O-16KEPPENS Eddy ...................................... S11-P-280KERHERVÉ Philippe ............................... S12-O-01KERN Zoltán ......................................... S16-P-128KERSCHNER Hanns .............................. S18-P-352KERTÉSZ Zsófia ..................................... S16-P-129KEY Robert ..... S12-O-05, S12-P-311, S20-P-134KHATIWALA Samar ............................... S20-P-134KHOKHLOVA Olga ................................ S08-P-238KIESER William E. .................................. S02-P-009

KIM G.D. ................................................. S16-O-04KIM J.-H. ................................................ S14-P-316KIM J.K. ................................................... S16-O-04KIM Jong Chan ............... S03-P-040, S03-P-041,

S07-O-08, S08-O-13KIM Y.E. ................................................... S16-O-04KIM Young-ill ........................................ S12-P-301KIMÁK Ádám ........................................ S03-P-074KINDER Malgorzata .............................. S05-P-161KING Stephanie ................ S03-P-066, S03-P-081KINSLEY Les .......................................... S10-P-261KIRILLOVA Elena ................................... S15-P-336KISHIMOTO Ayaka ................................ S14-P-326KITAGAWA Hiroyuki ......... S01-O-05, S01-P-139,

S01-P-145, S03-P-065, S04-P-091KLEIN Matthias ...................................... S02-O-05KLOS Ryk ............................................ S16-INV-06KNUDSEN Karen Luise .......................... S06-O-01KOBAYASHI Koichi ................................ S08-P-243KOBAYASHI Takeshi .............................. S02-P-004KOBER Florian ................. S18-INV-01, S18-P-343KODAMA Hiroki .................................... S13-P-104KOFLER Werner .................................... S11-P-279KOLACZEK Piotr ................................... S11-P-289KOLKER Alexander ................................ S13-O-10KOLKMAN H. Wim ................................. S02-O-01KONDO Miyuki ................. S14-P-326, S15-P-332KONDO Yasuhisa .................................. S20-P-137KONG Xianghui .................................... S18-P-351KÖNIG Svetlana .................................... S03-P-059KONO Makiko ...................................... S13-P-109KONOMATSU Masahiko ....................... S11-P-285KORSCHINEK Gunther ......................... S18-P-349KOTARBA-MORLEY Ania ....................... S08-P-246KOVALIUKH Nikolay ......... S06-P-183, S08-P-223KOYS Martin ......................................... S02-P-012KRAJCAR BRONIC Ines ..... S10-P-259, S13-P-099KRAPIEC Marek ............... S02-P-008, S05-P-156,

S11-O-03, S11-P-296KRASA Antonin .................................... S18-P-349KRETSCHMER Wolfgang .... S04-P-095, S08-O-14KRITZLER Karin ..................................... S04-P-095KROMER Bernd S01-INV-01, S01-O-06, S02-O-10,

S03-O-07, S03-P-052, S06-O-05, S15-P-327KRZEMNICKI Michael S. ...................... S19-INV-01KRZYWINSKI Knut ................................ S11-P-282KUBIK Peter W. ................ S18-INV-01, S18-P-343KUC Tadeusz ........................ S13-O-03, S15-O-03KULKOVA Marianna ........ S08-O-05, S08-P-215,

S08-P-223, S19-O-05KUMAMOTO Yuichiro ............................ S12-O-04KUNIKITA Dai .................... S08-P-231, S08-P-240KURIYAMA Yasunao ............................... S19-O-03

InDeX bY aUTHoRS

INDEX BY AUTHORS

16

KUS Peter .............................................. S02-P-012KUSANO Yukiko .................................... S13-P-110KUSCH Stephanie ................................ S14-P-325KUSHIBASHI Seiko ................................ S12-P-301KUTSCHERA Walter .............................. S11-P-279KUTSCHERA Walter .............................. S03-P-064KUZMIN Yaroslav ............ S07-P-194, S07-P-201,

S08-O-06, S08-P-217KUZNETSOV Vladislav ........................... S11-O-07KUZUCUOGLU Catherine ..................... S08-O-07KUZYAKOV Yakov ................................. S14-P-315KYPARISSI-APOSTOLIKA Nina ............... S07-P-198

LLAFRANCHI Brian W. ......... S15-P-340, S15-P-341LAHLIL Sophia ...................................... S07-P-195LAJ Carlo .............................................. S20-P-135LAL Shwaron ......................................... S03-O-04LAMB Henry F. .................... S01-O-05, S01-P-139LAMBERT Elsa ....................................... S07-P-195LAMY Frank ........................................... S06-O-03LANGE Todd ......................................... S03-P-081LANSARD Bruno .................................... S12-O-01LAROCCA Felice ................................... S08-P-244LASSERRE B ........................................... S17-O-03LAUKHIN Stanislav ................................ S11-O-07LAUVAUX Thomas ................................. S15-O-06LAVAL Eric .............................................. S08-O-11LAVENTO Mika ..................................... S08-P-225LAVIER Catherine ................................. S03-P-037LAWSON Graeme ................................. S05-P-162LAZAR Boaz ... S13-P-114, S18-O-03, S18-P-345LE CORRE Cédric .................................. S16-P-127LE DIZES Séverine ................................. S16-O-02LE DREZEN Yann ................................... S08-O-07LE PENNEC Jean-Luc ............................ S09-P-256LEAVESLEY Matthew ............................ S06-P-176LEAVITT Steven W. ........... S11-O-08, S11-P-286,

S11-P-292LEBATARD Anne Élisabeth .................... S18-O-04LEBON Matthieu ............ S07-P-195, S07-P-205,

S07-P-202LEDERER Claudia .................................. S18-P-349LEDUC Christian ................................... S13-P-115LEE James .............................................. S18-O-02LEE Jang Hoon ................. S03-P-040, S03-P-041LEE Jongeol .......................................... S01-P-152LEE K.H. .................................................. S16-O-04LEE Sharen .... S05-O-01, S05-P-160, S07-O-07,

S08-O-09, S08-P-227LEGRAND Michel .................................. S15-O-07

LEHMAN Scott J. ............... S01-O-02, S10-P-262, S10-P-267, S15-O-01, S15-O-06, S15-P-335,

S15-P-340, S15-P-341, S20-O-02LEITHOLD Elana .................................... S13-O-09LENOIR Guillaume ............................... S05-P-159LEONARD Alexander Gregory .......... S03-P-066,

S03-P-081, S11-P-292LEPETZ Sébastien ................................ S19-P-357LEREAH Yossi ........................................ S03-P-043LERICOLAIS Gilles ................................. S06-P-188LEROY Stéphanie .................................. S03-O-09LEVAC Elisabeth ................................... S06-P-178LEVCHENKO Vladimir ...... S03-O-04, S08-P-220,

S18-P-347LEVIN Ingeborg ............... S15-O-05, S15-P-327,

S15-P-339, S20-P-135LEWIS Mike ........................................... S06-P-178LEZINE Anne Marie ............ S11-P-295, S14-O-03LICCIOLI Lucia ...................................... S03-P-053LIEBL Jakob ........................ S03-P-064, S15-O-07LILLIE Malcolm ..................................... S06-P-181LIM Jaesoo ........................................... S06-P-186LIMA Fernanda T. W. .............................. S11-O-04LIMER Laura .................... S16-INV-06, S20-P-136LIN Hsiao - Wen .................................. S14-INV-01LIN Yin ................................................... S03-O-13LIN Ying-hsuan ...................................... S15-O-04LINARES Roberto ............. S02-P-002, S10-P-258LINDAUER Susanne .............................. S03-P-052LINDSAY Colin ...................................... S10-P-267LIPPERT Andreas .................................. S11-P-279LITHERLAND Albert E. .......................... S02-P-009LIU Guangshan .................................... S02-P-011LIU Kexin .......S02-O-02, S11-P-276, S12-P-299,

S16-P-120, S18-P-342LIU Zhao ................................................ S11-O-06LIU Zhonghui ....................................... S06-P-173LOCATELLI Christine ............................. S03-P-037LOHMANN Gerrit ............................... S20-INV-01LONG David ......................................... S06-P-193LONG Patricia ........................................ S02-O-03LONGWORTH Brett L. ............................ S02-O-03LOPEZ Morgan ................. S15-P-335, S15-P-339LORDKIPANIDZE David ........................ S11-P-278LOUGHEED Bryan ................................ S06-P-182LOUTE Stéphanie ................................. S08-P-211LOVENDUSKI Nicole .............................. S12-O-05LOWY Daniel A ..................................... S19-P-363LU Xuefeng .......................................... S03-P-070LUBRITTO Carmine .......... S03-O-08, S08-P-248,

S08-P-236, S08-P-237LUCARELLI Franco ................................ S15-P-330

InDeX bY aUTHoRS

INDEX BY AUTHORS

17

MMACARIO Kita .................. S02-P-002, S10-P-258MACCHIA Maria ................................... S03-P-079MACDONALD Robie ............................ S12-P-312MACH Lubomir .................................... S02-P-012MACHTS Heike ................. S03-P-082, S03-P-083MAEJIMA Yuji ........................................ S16-O-05MAGNANI Giuseppe ............................ S02-P-018MAIR Klaus ......................... S03-O-01, S03-P-064MAISCH Max ........................................ S18-P-352MAJOR István ....................................... S16-P-129MAKAROV N.A. ...................................... S08-O-04MAKSIMOV Fedor ................................. S11-O-07MAKSYUTOV Shamil ............................ S15-P-332MALGORA Sabina ................................ S08-P-245MALMENDIER Anne ............................. S08-P-211MANDENG-YOGO Magloire .............. S11-P-294,

S11-P-295, S14-O-03, S14-P-319MANDO’ Pier Andrea .. KEYNOTE 01, S03-P-053,

S03-P-056MANDUI Herman ................................. S06-P-176MANETTI Marco ................................... S03-P-055MANGANINI Steven ............................. S12-P-308MANGINI Augusto ................................ S06-O-05MANN Michael ..................................... S03-P-027MANN Paul ............................................ S04-O-04MANNING Sturt W. ......... S01-INV-01, S08-P-247MAR’YASHEV A.N. .................................. S08-O-15MARANG Laura ................ S16-P-121, S20-P-136MARCHAND Nicolas ............................ S15-P-331MARCHETTI M. ...................................... S17-O-03MARCHITTO Thomas ........................... S10-P-267MARCOTT Shaun .................................. S05-O-06MARDER Ofer ....................................... S07-P-210MARGIELEWSKI Wlodzimierz .............. S11-O-03,

S11-P-289MARIOTTI Véronique ............................. S10-O-03MARO Denis ....................... S16-O-02, S16-P-127MAROM Anat ................... S04-P-089, S07-P-197MAROTO Julia ...................................... S07-P-200MARQUES Aguinaldo .......................... S10-P-258MARSHALL Michael H. ....... S01-O-05, S01-P-139MARSHALL Peter .............. S05-P-163, S08-P-229MARTINELLI Nicoletta .......................... S06-P-191MARTINEZ DE LA TORRE Hector ......... S03-O-05,

S19-P-356MARTINEZ-VICENTE David ................... S13-P-115MARTINS Gabriel Souza ... S14-P-317, S14-P-321MARTMA Tõnu ..................................... S13-P-106MARUCCIO Lucio ........... S02-P-020, S08-O-01,

S08-P-245

MARZAIOLI Fabio ...............S03-O-08, S06-P-191, S08-P-236, S08-P-248, S08-P-250, S14-P-323,

S17-O-03MASARIK Jozef ..................................... S02-P-012MASSAULT Marc ................ S13-O-02, S13-O-05,

S13-P-108, S13-P-111, S13-P-113MASSUÉ Jean-Pierre ............................ S11-P-273MASUDA Kimiaki ................ S01-P-148, S19-O-03MATOS MARTINS José M. ...................... S06-O-02MATSUZAKI Hiroyuki ...... S08-P-231, S08-P-240,

S16-O-05MAURER Mantana ........... S01-O-07, S03-P-058,

S19-P-362MAY Barbara .......................................... S15-O-07MAYAKI Salla ......................................... S02-P-024MAŽEIKA Jonas .............. S11-P-288, S11-P-291,

S13-P-106, S16-P-126MAZERAT Julie ..................................... S10-P-264MAZUY Arnaud .................................... S11-P-278MAZZOTI Davide .............................. KEYNOTE 01MCCARTHY Matthew ........................... S12-P-310MCCULLAGH James S. O. S04-O-02, S04-P-089,

S07-P-197MCFADGEN Bruce ................................ S08-P-212MCGEEHIN J. ......................................... S03-O-13MCGREGOR H. ....................................... S06-O-04MCHARGUE Lanny R. ........................... S18-P-346MCINTYRE Cameron ............................ S04-P-093MCLAUGHLIN Fiona ............................. S12-P-312MCNICHOL Ann P. ......... S02-P-025, S04-P-093,

S12-O-02, S12-P-311, S12-P-312, S15-P-336MCNIVEN Ian ........................................ S06-P-176MCPHERRON Sahnnon ......................... S07-O-02MEADOWS John ................ S03-P-084, S05-O-03MEHTONEN Heidi ................................ S08-P-222MEIJER Harro A. J. .............. S02-O-01, S02-P-019,

S03-O-11, S03-P-046, S12-P-305, S15-O-02, S15-P-341, S19-P-354

MEIJLINK Bernard .................................. S05-O-04MEJIAS Jose Antonio ........................... S17-P-131MELAZO DIAS Cintia ............................ S16-P-117MELLSTRÖM Anette ............................ S06-P-192MÉNABRÉAZ Lucie ............................... S18-P-350MENDEZ-MILLAN Mercedes ................ S14-P-313MENGONI Alberto ............................... S18-P-349MÉNOT Guillemette ............................. S06-P-188MENU Michel ..................... S07-P-195, S08-O-11MESSAGER Erwan ................................ S11-P-278MESSILI Lamia ...................................... S08-P-234MEYER Laura ........................................ S06-P-185MGELADZE Ana ................................... S11-P-278MICHARD Gil ........................................ S13-P-111MICHCZYNSKA Danuta J. ... S11-O-03, S11-P-289

InDeX bY aUTHoRS

INDEX BY AUTHORS

18

MICHCZYNSKI Adam ..... S05-P-166, S05-P-167, S11-O-03, S11-P-289

MICHEL E. .............................................. S06-O-03MICHELETTO Egle ................................ S08-P-230MICHELOT Jean Luc ......... S13-P-108, S13-P-113MIFSUD Charles ................................... S18-P-347MIGNARDI Silvano ............................... S08-P-248MIKSIC John ......................................... S08-P-212MILES Natasha ...................................... S15-O-06MILLARD Andrew .............. S03-P-084, S05-O-04MILLER Benjamin R. ............................. S15-P-340MILLER John .. S01-O-02, S15-O-01, S15-P-340,

S15-P-341, S20-O-02MINAMI Masayo ............. S03-P-075, S13-P-101,

S13-P-109MINDAOUDOU Zeinabou ................... S02-P-024MINOR Elizabeth C. ............................... S12-O-02MINTZ Eugenia .................................... S19-P-360MITSUTANI Takumi ............. S01-P-151, S11-O-01MIYAHARA Hiroko ................................ S02-P-004MIYAKE Fusa ......................................... S01-P-148MIYAKE Yasuto ....................................... S16-O-05MIYATA Yoshiki ..................................... S13-P-101MIYAZAKI Yumiko ................................. S08-P-240MOBBS Shelly ....................................... S20-P-136MOHN Joachim ................................... S16-P-118MOHTADI Mayhar ................................ S06-P-174MOLLENHAUER Gesine ..... S14-O-04, S14-P-325MOLLIER-VOGEL Elfi ............................. S10-P-266MOLNÁR Mihály ............. S02-P-022, S03-P-074,

S03-P-081, S16-P-128, S16-P-129MONACO Mattia ................................... S15-O-02MONDELAIN Didier .............................. S15-P-335MONGE SOARES António M. ................ S06-O-02MONTAGNA Paolo ........... S10-P-270, S12-P-304MONTERO-SERRANO Juan Carlos ....... S10-P-270MONTLUCON Daniel ......... S04-O-04, S14-O-06MONTZKA Steven A. ......... S15-O-01, S15-P-340MOREAU Christophe .........S02-O-08, S02-P-021,

S03-O-09, S03-P-080, S06-O-07, S06-P-175, S07-P-196, S07-P-205, S07-P-206, S10-O-04,

S13-O-05, S13-P-112, S16-P-127MOREIRA Luciane Silva .. S14-P-316, S14-P-317,

S14-P-321MOREIRA-TURCQ Patricia S14-P-316, S14-P-319,

S14-P-321MORETON Steven G. ...... S03-P-057, S03-P-060,

S06-P-193MORGUNOVA Nina .............................. S08-P-238MORI Yuichi .......................................... S11-P-285MORIKAWA Noritoshi ........................... S13-P-110MORIN-RIVAT Julie ............................... S08-P-252MOROS Matthias .................................. S06-P-182

MORTLOCK Richard ............ S01-O-04, S10-O-05MOSS Rowena ..................................... S05-P-165MOTIEJUNAS Stasys ............................. S16-P-126MOUCHET Anne .................................. S20-P-138MOULE Yann ........................................ S13-P-113MOULLA Adnane ................................. S13-P-107MOUS Dirk J.W. ...................................... S02-O-05MUELLER Markus .................................. S20-O-03MUKAI Hitoshi .................. S15-P-332, S15-P-341MÜLLER Arnold M. ................................ S02-O-02 MÜLLER Carsten W. ............ S14-O-04, S14-P-320MULLEROVA Monika ............................ S15-P-333MUNOZ Olivia ...................................... S06-P-175MÜNSTERER Caroline ........................... S02-P-014MURAMATSU Yasuyuki ......................... S16-O-05MURATA Akihiko ................................... S12-O-04MURNICK Daniel E. ............................... S02-P-019MURRAY Callum ............. S03-P-034, S03-P-060,

S03-P-061MUSCHELER Raimund .. S01-P-144, S01-P-147,

S01-P-149, S06-P-182, S06-P-192, S20-P-135

NNADEAU Marie-Josée .... S01-P-153, S03-P-073,

S03-P-078, S05-O-04, S06-O-09, S06-P-190, S07-P-201, S13-O-06, S14-P-322

NADEL Dani ......................................... S03-P-076NAGAO Seiya ....................................... S13-P-104NAGAOKA Shinji .................................. S11-P-285NAGASAWA Shigenobu ....................... S04-P-091NAGAYA Kentaro .................................. S01-P-148NAHM Wook Hyun ............................... S06-P-186NAITO Yuichi ........................................ S08-P-243NAKAGAWA Takeshi ........... S01-P-139, S01-O-05NAKAMURA Shinya .............................. S03-P-042NAKAMURA Toshio ......... S01-P-148, S03-P-042,

S03-P-075, S08-P-251, S11-P-284, S11-P-285, S13-P-100, S13-P-101, S13-P-109, S15-P-337,

S15-P-341NAKANISHI Toshimichi ...... S06-P-186, S16-O-04NAKASHIMA Rei ................................... S06-P-186NAKATSUKA Takeshi ............................ S01-P-151NAKAZAWA Takakiyo ........................... S15-P-341NALEPKA Dorota ................ S05-P-155, S11-O-03NAMAI Saori .......................................... S19-O-03NAVA Silvia ........................................... S15-P-330NAVE Lucas .......................................... S14-P-324NAYSMITH Philip .............. S01-P-142, S01-P-143NDEYE Maurice .................................... S16-P-122NEELMEIJER Christian .......................... S03-P-064NEHLICH Olaf ........................................ S05-O-04NELSON Michael .................................. S04-P-092NESJE Atle ............................................ S11-P-272

InDeX bY aUTHoRS

INDEX BY AUTHORS

19

NESPOULET Roland ......... S03-O-15, S07-O-06, S07-P-202

NESTEROV Evgeny ................................ S19-O-05NEUHUBER Stephanie ......................... S03-P-064NEULIEB Thomas .................................. S06-P-178NEWBERGER Timothy ......... S12-O-05, S15-O-06NEWBERRY J. ........................................ S11-P-274NEWTON Josanne A. ............................ S03-P-060NEY Claude .......................................... S11-P-273NGUETNKAM Jean Pierre ... S11-P-295, S14-O-03NGUYEN TU Thanh Thuy ...................... S14-P-313NIGGEMANN Jutta ............................... S04-P-094NIGST Philip ......................................... S03-P-047NILSSON Jan ......................................... S17-O-02NING Wenxin ........................................ S06-P-192NISHIMOTO Hiroshi .............................. S03-P-042NIU Mu ............................................... S01-INV-01NOAKES John E. ................................... S02-P-005NOBLE Stephen R. ................................ S06-P-193NOMADE Sebastien ............................. S11-P-278NONNI Sara .... S03-O-08, S08-P-236, S08-P-248NORDÉN Maria ................................... S16-INV-06NORET Aurelie ...................................... S13-P-115NORMAN Rebecca ................................ S10-O-02NORONHA Alexandra ........................... S06-O-06NORRIS Simon ...................................... S20-P-136NOTHDURFT Luke ................................ S06-P-170NTINOU Maria ...................................... S07-P-198

OO’COFAIGH Colm ................................. S03-P-057O’REILLY Dougald ................................ S08-P-212OBIDOWICZ Andrzej ............................ S11-P-289OCHIAI Shinya ...................................... S13-P-104OEGGL Klaus ........................................ S11-P-279OGNIBENE Ted ...................................... S02-O-07OGRINC Nives ....................................... S13-O-04OHASHI Mami. S. .................................. S03-P-045OHKURA Toshiaki .................................. S16-O-05OHTA Tomoko ...................................... S13-P-101OHTANI Hajime .................................... S03-P-042OHYAMA Motonari .............................. S02-P-004OIKAWA Teruki ..................................... S11-P-284OINONEN Markku ......... S03-P-048, S03-P-063,

S06-P-177, S08-P-222, S08-P-225OKUNO Mitsuru ............... S11-P-284, S11-P-285OLIVEIRA Fabiana ............. S02-P-002, S10-P-258OLLAGNIER Céline ............................... S11-P-273OLLIVIER Vincent .................................. S11-P-278OLSEN Jesper . S03-P-032, S06-O-01, S06-P-168OLSSON Mattias .................................... S03-O-10OMORI Takayuki ............... S08-P-251, S20-P-137ONDOV John ....................................... S04-P-092

ONKAMO Päivi ..................................... S06-P-177ONUKI Shizuo ....................................... S08-P-231ORLOVA Lyoba A. .................................. S11-O-09ORMSBY Kaelyn ............... S03-P-062, S19-P-356ORSI Anais ............................................. S18-O-02ORSOVKSZI Judit .............. S03-P-074, S03-P-081ORSOVSZKI Gergely ............................. S03-P-074ORTIZ Joseph ....................................... S10-P-267ORTLIEB Luc ......................................... S10-P-269ORYSHAKA Aleksandr .......................... S16-P-126OSBORNE Michael ............................... S12-P-297OSKAM Charlotte .................................. S09-O-03OSLISLY Richard .................................... S08-O-10OSLISLY Richard ................................... S08-P-252OSTAPKOWICZ Joanna ........................ S08-P-255OUK Sokha ........................................... S08-P-212OVCHINIKOV Sergej ............................. S16-P-126OZAKI Hiromasa ................. S01-P-151, S11-O-01

PPACHNEROVA BRABCOVA Katerina ..... S01-P-141PACK Mary A. .................... S03-P-071, S03-P-072PAILLARD Didier ................. S01-P-146, S10-O-03PAILLET Patrick ..................................... S07-P-195PAK Edwin ............................................ S11-P-279PALMER Jonathan ................................. S01-O-06PALMER Suzanne ................................. S03-P-088PALONEN Vesa .................. S03-P-048, S03-P-063PALSTRA Sanne ................ S03-P-046, S19-P-354PANYUSHKINA Irena P. ...... S08-O-15, S11-O-08,

S11-P-286, S11-P-292PAPA Stefania ....................................... S14-P-323PARK Gyujun S01-P-152, S03-P-065, S03-P-068,

S16-O-04PARK Junghun ................ S01-P-145, S01-P-152,

S03-P-065, S03-P-068, S16-O-04PARK Wongyu ...................................... S01-P-152PARKER PEARSON Mike ....................... S05-P-163PASSARIELLO Isabella ...... S03-O-08, S06-P-191,

S08-P-248, S08-P-250, S14-P-323, S17-O-03PASSARINI JUNIOR Jaime Rissi ............ S11-O-04,

S11-P-281PASTOR Lucie ........................................ S12-O-01PATERNE Martine ............ S06-O-03, S07-P-206,

S10-O-04, S12-P-304PATOU-MATHIS Marylène .................... S07-P-208PATRUT Adrian ..................................... S19-P-363PATRUT Roxana .................................... S19-P-363PATT Ulrike ........................................... S03-P-077PATTERSON R Timothy ......................... S06-P-171PATZELT Gernot .................................... S11-P-279PAUL Dipayan ....................................... S02-P-019PAUL Michael ....................................... S18-P-349

InDeX bY aUTHoRS

INDEX BY AUTHORS

20

PAULLEY Alan ....................................... S20-P-136PAWELCZYK Slawomira ......................... S16-O-03PAWLAK Jacek ...................................... S05-P-158PAWLYTA Miroslawa ......... S03-P-043, S16-P-123PAYNE Rebecca L. ............... S01-O-05, S01-P-139PAZDUR Anna S02-P-010, S08-P-235, S11-O-03,

S15-P-337, S16-O-03, S16-P-123PÉAN Stéphane .................................... S07-P-208PEARSON Charlotte ............................. S08-P-247PEARSON Emma J. ............................... S04-P-090PENDEA Florin ...................................... S06-P-178PENDERGRAFT Matthew ...................... S03-O-12PEREZ Marcela ..................................... S14-P-319PERRON Nolwenn ........... S03-O-10, S15-P-336,

S16-P-116PERRY Chris .......................................... S03-P-088PESCE Giovanni Luca A. ... S03-P-044, S08-P-230PESONEN Antto ................................... S03-P-063PESONEN Petro .................................... S06-P-177PESSENDA Luiz Carlos Ruiz S11-O-04, S11-P-281PETCHEY Fiona ..................................... S06-P-176PETRENKO Vasilii ................................... S18-O-02PETRON Gabriel ................................... S15-P-340PETROŠIUS Rimantas ........................... S13-P-106PEUCKER-EHRENBRINK Bernhard ....... S04-O-04,

S14-O-06PHILIPPSEN Bente ............ S06-P-189, S08-P-249PICCOLI Angela .................................... S02-P-018PICHON Laurent .................................... S03-O-15PIGNATELLI Olivia ................................. S06-P-191PIOT Christine ...................................... S15-P-331PIOTROWSKA Natalia ...... S05-P-161, S16-O-03,

S16-P-123PIRSON Stéphane ................................ S07-P-199PLAIN Caroline ...................................... S13-O-02PLANTE Alain F. .................................... S14-P-314PLASSARD Frederic .............................. S07-P-195PLENS Claudia ...................................... S09-P-257PLETS Gertjan ....................................... S08-P-211PLICHT VAN DER Johannes .................. S03-P-046PLOMPEN Arjan .................................... S18-P-349POLLARD Mark ..................................... S08-P-228PONS BRANCHU Edwige ..................... S07-P-205PONTON Camilo ................................... S14-O-06PORTER Robert .................................... S08-P-232POSSNERT Göran ............... S08-P-223, S17-O-01POTEKHINA Inna .................................. S06-P-181POVINEC Pavel ............... S01-P-141, S02-P-012,

S13-O-04, S15-P-333PRÉVÕT André S15-O-04, S15-P-328, S15-P-329PRANGE Matthias ............................... S20-INV-01PRASAD Gurazada. V. Ravi .. S02-P-005, S19-O-02PRAT Sandrine ...................................... S07-P-208

PREUNKERT Susanne ............................ S15-O-07PREVOT André S. H. .............................. S15-P-336PRICE Gilbert ........................................ S06-P-170PRILLER Alfred .................... S03-O-01, S11-P-279PRIOR Christine .................................... S06-P-187PUAUD Simon .................. S07-P-208, S11-P-278

QQIANG Xiaoke ...................................... S18-P-351QUARTA Gianluca ........... S02-P-020, S03-P-044,

S03-P-079, S08-O-01, S08-P-244, S08-P-230, S08-P-245, S19-O-06, S19-P-359

QUERRÉ Guirec .................................... S08-P-234QUILES Anita S02-O-08, S02-P-021, S03-P-080,

S07-O-05, S07-P-206QUINIF Yves .......................................... S11-P-280QUIROS CASTILLO Juan Antonio ......... S08-P-237

RRABOUILLE Christophe ...... S12-O-01, S13-P-105RAESSLER Michael ............................... S03-P-082RAIMUND Muscheler ............................ S03-O-07RAISBECK Grant .................................... S01-P-146RAKOWSKI Andrzej Z. .... S03-P-073, S15-P-337,

S16-O-03RAMIREZ-SANCHEZ Hermes Ulises ...... S13-O-07RAMONET Michel ............ S15-P-335, S15-P-339RAMSEY Christopher ........................... S08-P-242RANDERSON James T ........................ S14-INV-01RASMUSSEN Tine L .............................. S06-P-168RAZLIVANOV Igor .................................. S15-O-06REBOLLO Noemi .................................. S03-P-076REICHE Ina .... S03-P-064, S07-P-195, S07-P-202REIMER Paula Jo ............ S01-INV-01, S03-P-032,

S03-P-035, S06-O-01, S06-P-168, S06-P-171, S13-O-08

REIMER Ron W. ............... S01-INV-01, S03-P-032RELLA Stephan ..................................... S10-P-268RENAUD Philippe ................................. S16-P-127RENGARAJAN R. ................................... S12-P-303RENGASWAMY Ramesh ....................... S06-P-179REPETA Daniel ..................... S04-O-04, S12-O-02RESZEL Maciej ...................................... S08-P-215RETHEMEYER Janet ........ S03-P-059, S03-P-077,

S14-O-04, S14-P-320, S14-P-325REYERSON Paul E. .................................. S03-O-05REYNARD Linda .................................... S03-P-029REYSS Jean-Louis ................................. S10-P-269RIBECHINI Erika .................................... S08-P-255RICCI Paola ........................................... S06-P-191RICHARDIN Pascale ........ S03-P-033, S03-P-037,

S08-O-11, S19-P-353RICHARDS David A. ............................ S01-INV-01

InDeX bY aUTHoRS

INDEX BY AUTHORS

21

RICHARDS Mike ..................................... S07-O-02RICHARDS Thomas ............................... S06-P-176RICHARDSON Scott ............................... S15-O-06RICHTARIKOVA Marta ...... S02-P-012, S13-O-04,

S15-P-333RIECK Anke ........................................... S03-P-073RIEDEL Katja .......................................... S18-O-02RINYU László S02-P-022, S03-P-074, S16-P-129RISHKO Sa ............................................. S08-P-241RIVERA CASANOVAS Claudia ............... S18-P-347RIVERO VILA Olivia ............................... S07-P-205RIZZO Antonietta ................................. S02-P-018ROBERT Vincent .................................... S08-O-07ROBERTS Brian ...................................... S13-O-10ROBERTS J. Murray ............................... S06-P-193ROBERTS Mark L. ............ S02-O-03, S02-P-025,

S03-P-030, S03-P-031, S04-P-093, S14-P-314ROBLES GARCIA Nelly ........................... S09-O-02ROCHE Didier M. ................................... S10-O-03RÖCKMANN Thomas ............................ S15-O-02RODGERS Keith ..................................... S10-O-01RODRIGUES Renato Aragão ............. S11-P-277,

S14-P-317, S14-P-321ROE Kimberly ........................................ S13-O-10ROMAIN Odile ...................................... S08-P-234ROOBROECK Dries ................................ S14-O-04ROSENHEIM Brad ................ S03-O-12, S13-O-10ROSENSTEIN Dana Drake ...................... S19-O-04ROSTEK Frauke ..................................... S06-P-188ROTHACKER Leo ................................... S13-O-06ROUSSEL Morgan ................................. S07-O-02ROUSSEL-DEBET Sylvie ........................ S16-P-127ROWE Cassandra .................................. S06-P-176ROZANSKI Kazimierz ........... S13-O-03, S15-O-03RUACHO Mariela .................................. S03-P-086RUAN Jiaoyang ..................................... S06-O-06RUAN Xiangdong ........... S02-P-001, S08-P-213,

S08-P-216RUGGIERO Grazia ................................. S08-P-236RUMPEL Cornelia ................................. S14-P-315

SSABATIER Pierre .................................... S10-P-270SADIER Benjamin ................ S07-O-05, S18-O-04SAKAMOTO Minoru ........... S01-P-151, S11-O-01SAKURAI Hirohisa ........... S02-P-004, S03-P-045,

S15-P-334, S19-O-03SALAMANACA Eric ............................... S03-P-069SALAZAR Gary .................... S02-O-07, S02-P-007SALCHER Bernhard .............................. S18-P-343SALEHPOUR Mehran ............................ S17-O-01SALIÈGE Jean-François ... S06-P-175, S08-P-234,

S19-P-357SALIFOU Soumana .............................. S02-P-024SALVATTECI Renato .............................. S10-P-269SALVINI Antonella ................................ S03-P-053SALZANI Luciano .................................. S05-O-03SAMANIEGO Pablo ............................... S09-P-256 SANAULLAH Muhammad ................... S14-P-315SANTAMARIA David ............................. S07-P-200SANTOS Alice Bosco ............................ S14-P-317SANTOS Guaciara Macedo ................. S01-P-150,

S03-O-05, S03-P-038, S03-P-062, S03-P-072, S03-P-086, S06-P-185, S10-P-263, S15-P-336,

S19-P-356SANTOS-AREVALO Francisco Javier .. S16-P-119,

S17-P-131SANZ Nuria ......................................... S09-INV-01SAPRYKINA Irina ................................... S08-P-226SARMIENTO Jorge ................................. S12-O-05SATO Taiichi ....................... S15-P-334, S19-O-03SAWICKA Natalia ................................... S16-O-03SCHÄTZEL Gabriele .............................. S18-P-349SCHAEFER Hinrich ................................ S18-O-02SCHARF Andreas ................ S04-P-095, S08-O-14SCHEFUSS Enno .................................... S14-O-06SCHIAVO Jolimar Antonio .................... S11-O-04SCHINDLER Matthias ........................... S04-P-095SCHLÜCHTER Christian .. S18-INV-01, S18-P-352SCHLOLAUT Gordon .......... S01-O-05, S01-P-139SCHMIDT Martina ............ S15-P-335, S15-P-339SCHMIDT Michael ................................ S04-P-094SCHMIERER James ............................... S11-P-286SCHNEIDER Ralph R. ............................ S10-P-266SCHNITZER Caitlin J. ............................. S18-P-346SCHOLZ Denis ...................................... S06-O-05SCHVOERER Max .................................. S11-P-273SCHWIKOWSKI Margit ...... S03-P-039, S11-P-272SCIRE’ CALABRISOTTO Caterina ........... S03-P-056SCOTT E. Marian ........... S01-INV-01, S01-P-142,

S01-P-143, S03-P-060SCRIVNER Adam .................................... S12-O-06SECCO Michele .................................... S08-P-248SEILER Martin S02-O-06, S02-P-013, S02-P-014,

S02-P-015, S02-P-022SEJRUP Hans Petter .............................. S10-P-262SEMENTSOV Aa .................................... S08-P-241SENSULA Barbara ............... S16-O-03, S16-P-123SEOANE José Carlos Sícoli ................ S11-P-277,

S14-P-317, S14-P-321SEPULCRE Sophie ................................. S10-O-06SETTI Valérie . S02-P-021, S03-P-080, S13-P-112SEVERINGHAUS Jeffrey ......................... S18-O-02SHAH Sunita ......................................... S02-P-025SHAHACK- GROSS Ruth ... S07-P-210, S19-P-360

InDeX bY aUTHoRS

INDEX BY AUTHORS

22

SHANKS Richard P. ............................... S03-P-061SHAO Qingfeng ................................... S09-P-253SHARIFI Mahnaz ................................... S08-P-233SHAW George ................ S16-INV-06, S20-P-136SHEN Chengde .............. S11-P-276, S12-P-299,

S16-P-120, S18-P-342SHENNAN Stephen ............................... S08-O-03SHEPSON Paul ....................................... S15-O-06SHEVKOMUD Igor ................................ S08-P-231SHEWAN Louise ................................... S08-P-212SHIBATA Katsumasa .............................. S19-O-03SHIBATA Yashuyuki ......... S13-P-104, S14-P-326,

S15-P-332SHIN Kyung-Hoon ............................... S12-P-298SHIRATO Yasuhito ................................. S14-P-326SHORTLAND Andrew .......................... S08-P-227SIANI Giuseppe .................. S06-O-03, S12-P-304SICLET Françoise .................................. S16-P-121SIEPMAN Daniel ................................... S12-P-305SIERRA Carlos A. .................................... S20-O-03SIFEDDINE Abdel ................................. S10-P-269SIFEDDINE Abdelfettah S11-P-277, S14-P-317,

S14-P-321SILENZI Sergio ...................................... S12-P-304SIMÔES-FILHO F.F.L. .............................. S14-P-321SIMONASSI Jose Carlos ........................ S10-P-258SIMONEIT Bernd .................................... S13-O-07SINCLAIR Daniel ................................... S06-P-193SINITSYN Andrei A. ......... S07-P-197, S07-P-199,

S07-P-203SINNINGHE DAMSTÉ Jaap ................... S14-P-316SIQUEIRA Geovane ............ S11-O-04, S11-P-281SIRIGNANO Carmina ............................ S06-P-191SIROCKO Frank ...................................... S13-O-06SIRONIC Andreja .............. S10-P-259, S13-P-099SIVO Alexander ............... S02-P-012, S13-O-04,

S15-P-333SKINNER Luke ..................... S10-P-265, S12-O-06SKOG Goeran ................... S01-P-144, S16-P-117SKRIPKIN Vadim ................ S06-P-183, S08-P-223SKURATOVIČ Žana ............ S13-P-106, S16-P-126SLUSARZ Malgorzata ........................... S11-P-283SMITH Andrew ............... S02-P-003, S03-P-027,

S03-P-028, S15-P-341, S18-O-02SMITH Colin ........................................... S11-O-05SMITH Graham ..................................... S20-P-136SMITH Karen ......................................... S20-P-136SMITH Lydia ......................................... S14-P-324SMITHERS Scott .................................... S03-P-088SMITTENBERG Rienk H. .... S04-P-094, S14-O-05,

S14-P-318SMOLSKA Ewa ...................................... S11-P-288SNOWBALL Ian ................. S06-P-182, S06-P-192

SOLER Joaquim .................................... S07-P-200SOLER Narcis ........................................ S07-P-200SOLIS-ROSALES Corina ........................ S16-P-130SONG Sujin ....................... S03-P-040, S03-P-041SONG Tang ............................................ S15-O-06SONG Young Mi ............... S03-P-040, S03-P-041SORESSI Marie ....................................... S07-O-02SOULET Guillaume ............................... S06-P-188SOULEY Idé .......................................... S02-P-024SOUPRAYEN Christelle ... S02-P-021, S03-P-080,

S13-P-112SOUTHON John R. ........... S01-INV-01, S01-O-06,

S01-P-140, S01-P-149, S01-P-150, S03-O-05, S03-O-16, S03-P-038, S03-P-072, S03-P-086,

S06-P-174, S06-P-178, S07-P-201, S10-P-263, S15-O-01, S15-P-341

SPALDING Kristy ............................... KEYNOTE 02SPEICH Sabrina ..................................... S10-O-04SPENCER Neal ...................................... S03-P-084SQUIRE Joe ........................................... S11-P-292STÜTE Martin ....................................... S02-P-019STACEY Rebecca .................................. S09-P-255STACHOWICZ-RYBKA Renata ............... S11-P-283STAFF Richard Andrew ... S01-O-05, S01-P-139,

S03-P-029STAFFORD Tom W. ................................ S03-O-16STANICEK Jaroslav ................................ S02-P-012STARKEL Leszek ..................................... S11-O-03STARKOVICH Britt .................................. S03-O-17STEIER Peter .. S03-O-01, S03-O-14, S03-P-064,

S11-P-279, S15-O-07, S18-P-349STEIN Mordechai ............. S13-P-114, S18-O-03,

S18-P-345STEINHOF Axel ............... S02-P-023, S03-P-082,

S03-P-083STENSTRÖM ERIKSSON Kristina .......... S03-O-10,

S15-P-336, S16-P-116, S16-P-117, S17-O-02STEVENSON Alice ................................. S08-P-227STICHELBAUT Birger ............................ S08-P-211STILLS Aubrey .................. S03-P-071, S03-P-086STONER Joseph ..................................... S05-O-06STRANO Sarah ....................................... S05-O-06STREET M. ............................................. S07-P-201STRZEPEK Kelly ..................................... S03-P-054STUHL Alexander ................................. S04-P-095STWORZEWICZ Ewa ............................ S11-P-283SUDOł Magdalena ............................... S07-P-207SUMERLING Trevor ............................... S20-P-136SUN Ming-yi .......................................... S12-O-01SUNG Kisuk S01-P-145, S01-P-152, S03-P-068,

S06-P-186, S16-O-04SUNGATOV Flarit .................................. S08-P-220SURRAT Jason ........................................ S15-O-04

InDeX bY aUTHoRS

INDEX BY AUTHORS

23

SUTER Martin ... S02-O-06, S02-P-013, S02-O-02 SUVOROV Alexander ........................... S06-P-172SVEINBJORNSDOTTIR Arny Erla ........... S08-P-242SVENSSON Anders ............................... S01-P-147SVETLIK Ivo ........................................... S01-P-141SVYATKO Svetlana V. ............................. S03-P-035SWANSTON Christopher ...................... S14-P-324SWEENEY Colm . S12-O-05, S15-O-01, S15-O-06SWIETLICKI Erik ..................................... S15-P-336SYNAL Hans-Arno ............. S02-O-06, S02-P-007,

S02-P-013, S02-P-014, S02-P-022, S03-O-07, S04-O-01

SZIDAT Sönke .................. S02-P-007, S03-P-039, S11-P-272, S15-O-02, S15-O-04, S15-P-328,

S15-P-329, S15-P-336, S16-P-118SZMYT Marzena ................................... S08-P-215SZWARCZEWSKI Piotr ...... S11-P-288, S11-P-291SZYCHOWSKA-KRAPIEC Elzbieta ......... S11-P-296

TTACCETTI Francesco ............................ S15-P-330TAKAHASHI Hiroshi A. ...... S13-P-100, S13-P-110TAKAHASHI Taro .................................... S12-O-05TAKAHASHI Yui ................... S15-P-334, S19-O-03TAKEMURA Keiji ................................... S04-P-091TAKESHITA Yui ....................................... S18-O-02TAKIGAMI Mai ....................................... S08-P-243TALAMO Sahra ...................................... S07-O-02TALLAVAARA Miikka ............................. S06-P-177TANAKA S. Shinichi .............................. S12-P-301TANAKA Takayuki ................................. S13-P-104TANDOH Joseph Bremang S14-P-323, S17-O-03TANI Sayaka ...................... S01-P-145, S03-P-065TANIMIZU Masaharu ............................ S13-P-109TANS Pieter ....... S15-O-01, S15-O-06, S15-P-340TARASOV Pavel E. ............... S01-O-05, S01-P-139TAVAGNA Maria-luisa ........................... S12-P-307TAVERA Wilfredo .................................. S15-P-334TAYLOR R. Ervin ................ S01-P-149, S07-P-201TEP Sokha ............................................. S08-P-212TEPELYAKOV Natalya ............................. S18-O-03TERAO Yukio ......................................... S15-P-332TEREYGEOL Florian .......... S07-P-195, S07-P-196TERRASI Filippo ................. S03-O-08, S06-P-191,

S08-P-216, S08-P-248, S08-P-250, S14-P-323, S17-O-03

TESTA Nicholas ..................................... S11-P-292THEODORSSON Pall ....... S02-P-006, S02-P-008,

S08-P-239THOMAS Alex L. .................................... S01-O-03THOMAS Jim ........................................ S03-P-066THOMAS Mark ....................................... S08-O-03THORNE Mike ....................................... S20-P-136

THOUVENY Nicolas .............................. S18-P-350TIKKANEN Pertti ................................... S03-P-048TIMPSON Adrian ................................... S08-O-03TIMS Stephen ....................................... S16-P-125TISNERAT LABORDE Nadine ............... S07-P-205,

S07-P-206, S10-O-04, S10-P-270, S12-O-01, S12-P-304, S13-P-105

TOHJIMA Yasunori ................................ S15-P-332TOKANAI Fuyuki ............. S02-P-004, S03-P-045,

S15-P-334, S19-O-03TOKUNAGA Tomochika ....................... S13-P-110TOMASKOVA Lenka .............................. S01-P-141TOMKINS Helene ................................. S06-P-176TOMS Philip .......................................... S11-P-274TONGHINI Cristina ............................... S08-P-248TORINO Mariaelva ................................ S08-P-250TORN Margaret .................................... S14-P-324TOSITTI Laura ....................................... S02-P-018TOUSSAINT Flora ................ S12-O-01, S13-P-105TOYOGUCHI Teiko ................................ S02-P-004TRAVI Yves ............................................ S13-P-115TREIGNIER Claire ................................... S12-O-01TRICHET Jean ....................................... S12-P-300TRIFONOV Va ........................................ S08-P-241TRIPATI Aradhna ................................... S06-P-185TRONCZYNSKI Jacek ............................. S12-O-01TRUMBORE Susan .......... S20-O-03, S14-INV-01,

S14-P-324TRZCINSKI Jerzy ................................... S08-P-246TSUCHIYA S Yoko .................................. S16-O-05TSUKAMOTO Hitoshi ........................... S13-P-100TUDYKA Konrad ............. S02-P-010, S08-P-235,

S16-O-03, S16-P-123TUERLER Andreas ................................. S02-P-007TURCQ Bruno ................. S11-P-277, S11-P-294,

S11-P-295, S14-O-03, S14-P-316, S14-P-317, S14-P-321

TUREK Karel .......................................... S01-P-141TURNBULL Jocelyn C. ...... S05-P-165, S15-O-01,

S15-O-06, S15-P-340TURNEY Christian S.M. ..... S01-INV-01, S01-O-06TUROSS Noreen ................. S07-P-209, S09-O-02TYERS Cathy ......................................... S08-P-229TYLMANN Wojciech ............................. S05-P-161

UUCHIDA Masao .............. S10-P-268, S13-P-104,

S14-P-326, S15-P-332UEDA Kyoko ......................................... S11-P-285UGGÈ Sofia ........................................... S08-P-230ULM Sean ............................................. S06-P-176UOTILA Kari .......................................... S08-P-222USHIDA Masao ..................................... S15-P-336UTO Kozo ............................................. S19-P-358

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INDEX BY AUTHORS

24

VVAIDOTAS Algirdas ............................... S16-P-126VAITKEVICIENE Violeta .......................... S16-P-126VALENTINI R .......................................... S17-O-03VALLADAS Hélène ............. S03-O-15, S07-O-05,

S07-P-195, S07-P-196, S07-P-205, S07-P-206, S07-P-208

VALLI Gianluigi ..................................... S15-P-330VALZOLGHER Erio ................................. S05-O-03VAN DE WATER Peter ............................ S11-P-292VAN DER LINDEN Marjolein ................. S11-P-274VAN DER PLICHT Johannes ................ S01-INV-01,

S01-O-05, S01-P-139, S02-O-01, S07-P-199, S07-P-201, S07-P-208, S08-P-241, S11-O-09,

S11-P-274, S15-O-02VAN GEEL Bas ....................................... S11-P-274VAN GEEN Alexander ........................... S10-P-267VAN HEUVEN Steven ............................ S12-P-305VAN STRYDONCK Mark .... S03-O-03, S03-P-078,

S08-O-02, S08-P-211, S11-P-280VAN ZONNEVELD Dicky ........................ S03-O-11VANDENABEELE Peter ........................... S03-O-03VANDERVEER Michael .......................... S04-P-092VASKS Andrejs ...................................... S08-P-225VAUBAILLON Sylvain ............................. S03-O-15VECCHI Roberta ................................... S15-P-330VECCHIATTINI Rita ................................ S03-P-044VECCHIO Giuseppe .............................. S08-P-250VELAZCO Federico ............................... S10-P-269VENTURA SANTOS Roberto ................. S16-P-117VERES Mihály .................. S02-P-022, S03-P-074,

S03-P-081, S16-P-128VERHEYDEN Sophie ............................. S11-P-280VERLINDEN Charlotte .......................... S08-P-211VESALA Timo ........................................ S03-P-048VIGNAUD Colette ................................. S07-P-195VILLAESCUSA Julio ............................... S06-P-184VINCENT Julien .............. S02-P-021, S03-P-033,

S03-P-080, S13-P-112VIOLLIER Eric ........................................ S13-P-111VIRTASALO Joonas ............................... S06-P-182VODILA Gergö ...................................... S16-P-129VOGEL Edith ......................................... S02-P-007VOGEL Felix Robert ............................... S15-O-05VOGEL John ....................... S02-O-04, S03-P-067VOINCHET Pierre .................................. S11-P-278VOLKMER-RIBEIRO Cecília .................... S11-P-281VON GRAFENSTEIN Ulrich ................... S11-P-278VON REDEN Karl F. ............ S02-O-03, S04-P-093,

S12-P-311, S19-P-363VONK Jorien E. ...................................... S04-O-04VOSS Britta .......................... S04-O-04, S14-O-06

VOYATSIS Mary ...................................... S03-O-17VUILLEMIN Cyrille ................................. S15-P-335VYBORNOV Aleksander ... S08-O-05, S08-P-215,

S08-P-223VYBORNOVA Maria ............................... S08-P-223

WWACKER Lukas .S01-O-06, S01-O-07, S01-P-144,

S01-P-149, S02-O-06, S02-P-007, S02-P-013, S02-P-014, S02-P-015, S02-P-022, S03-O-07,

S03-P-039, S03-P-058, S03-P-077, S03-P-081, S04-O-01, S04-P-094, S06-P-182, S11-P-272, S14-O-05, S14-P-318, S15-O-04, S15-P-328,

S15-P-329, S15-P-336, S16-P-128, S17-P-132, S18-INV-01, S18-P-343, S19-INV-01, S19-P-362

WAGAI Rota .......................................... S14-P-326WAGENBACH Dietmar ....... S15-O-07, S20-P-135WAHLMÜLLER-OEGGL Notburga ........ S11-P-279WALANUS Adam ............ S02-P-008, S05-P-154,

S05-P-155, S05-P-156WALKE Russell .................................... S16-INV-06WALKER Brett ....................................... S12-P-310WALLNER Anton .................................. S18-P-349WALTER Richard .................................... S09-O-03WANG Hong ....................... S03-O-06, S11-P-271WANG Huijuan ..................................... S08-P-216WANG Ning .................... S11-P-276, S12-P-299,

S16-P-120, S18-P-342WANG Shing-lin .................................... S03-O-13WANG Xiang-Gao ................................ S02-P-016WANINGER Scott .................................. S11-P-271WATANABE Shuichi ............................... S12-O-04WATT Geoff .......................................... S02-P-003WEAVER Gawain .................................. S19-P-361WEBB Gregory ...................................... S06-P-170WEBER Rodney ..................................... S15-O-04WEIJAN Zhou ....................................... S18-P-351WEINER Steve ....................................... S07-P-210WEISS Ray .............................................. S18-O-02WEN Wei ........................... S12-P-299, S18-P-342WENGROW David ................................ S08-P-227WERNE J.P. ............................................. S12-O-02WEST John ........................................... S05-P-165WHITE Lara ........................................... S18-P-351WIEDEMEIER Daniel ............................. S04-P-094WIEDENHOEFT Alex J. ..... S11-O-08, S11-P-286,

S11-P-292WIELER Rainer .................................... S18-INV-01WIESER M. ............................................. S13-P-098WILD Eva Maria ............... S03-O-14, S08-P-247,

S11-P-279WILLIAMS Elizabeth .............................. S03-O-12WOLAK Chad ..................... S15-O-01, S15-P-341

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INDEX BY AUTHORS

25

WOO H.J. ............................................... S16-O-04WOOD Rachel E. ............ S03-P-049, S03-P-050,

S03-P-054, S06-P-172, S07-O-01, S07-P-200WOODBORNE Stephan ........................ S19-P-363WOODROFFE C. .................................... S06-O-04WORTHY Doug E. J. ............................... S15-O-05WRIGHT James .................... S01-O-04, S10-O-05WU Tzu-shuan ....................................... S03-O-13WU Ying .............................. S04-O-04, S14-O-06WU Zhenkun ........................................ S18-P-351WURSTER Chris ..................................... S03-O-04

XXIAN Feng .......................... S11-O-06, S18-P-351XIONG Zhaoming ............ S08-P-213, S08-P-216XU Li ............... S02-P-025, S12-O-02, S12-P-312XU Sheng ....................... S03-P-057, S03-P-060,

S19-P-358XU Shulan ...................... S16-INV-06, S20-P-136XU Xaiomei S01-P-150, S03-P-038, S03-P-069, S03-P-071, S03-P-072, S03-P-086, S10-P-263,

S12-P-306, S15-P-341XUEREF-REMY Iréne ............................. S15-P-335

YYADAVA Madhusudan ......................... S06-P-179YAMAGATA Takeyasu ............................ S16-O-05YAMAHARA Toshiro .............................. S08-P-231YAMAMOTO Masayoshi ....................... S13-P-104YAMASAKI Shinji ................................... S08-P-243YANEVICH Oleksandr ........................... S07-P-208YANG Bin .............................................. S03-P-027YASUHARA Masaya .............................. S13-P-110YASUR Gal ............................................ S07-P-210YATSUZUKA Shinya .............................. S11-P-284YECHIELI Yoseph .................................. S13-P-103YELOFF Dan .......................................... S11-P-274YESHURUN Reuven .......... S03-P-076, S07-P-210YI Hi-il ................................................... S12-P-298YI Weixi ....... S11-P-276, S12-P-299, S16-P-120,

S18-P-342YOKOYAMA Yusuke ........... S01-O-03, S01-O-05,

S01-P-139YONEDA Minoru .............. S08-P-243, S20-P-137YONEMURA Seiichiro ........................... S14-P-326

YONENOBU Hitoshi ........... S01-O-05, S01-P-139YOON Suk-hee ..................................... S12-P-298YOSHIDA Kunio ................ S08-P-231, S08-P-240YOSHIMITSU Takahiro .......................... S01-P-148YUN Myoung-Ho ............. S03-P-040, S03-P-041

ZZAHN David ......................................... S18-P-346ZAITSEVA Ganna ............... S08-O-04, S08-O-05,

S08-P-223ZANESCO Alexander ............................ S11-P-279ZAPF Alexander .............. S03-P-039, S11-P-272ZARAGOSI Sébastien ........................... S06-P-188ZARATE-DEL-VALLE Pedro F. ................. S13-O-07ZAWISKIE John ...................................... S11-O-08ZAYTSEVA Ganna ................................. S08-P-241ZAZZO Antoine .............. S06-P-175, S07-P-202,

S19-P-357ZELLER Bernd ....................................... S14-P-313ZENG Fanwei ........................................ S03-P-086ZENISOVA Zlatica .................................. S13-O-04ZETTERBERG Pentti .............................. S08-P-222ZEYER Kerstin ....................................... S16-P-118ZHANG Dachun ................................... S03-P-038ZHANG Xiaolu ....................................... S15-O-04ZHANG Yan Lin .............. S02-P-007, S03-P-039,

S15-O-04, S15-P-328, S15-P-329, S15-P-336ZHAO Jian-xin S06-O-04, S06-P-169, S06-P-170ZHAO Xiao-lei .................... S02-O-09, S02-P-009ZHENG Dachun .................................... S12-P-306ZHOU Aifeng ........................................ S06-P-180ZHOU Liping ...................... S02-O-02, S03-P-072ZHOU Weijian ....................................... S11-O-06ZHU Yizhi ............................................... S11-O-06ZIGAH Prosper Kojo .............................. S12-O-02ZINK Antoine ........................................ S05-P-157ZIOLKOWSKI Lori A. ............................. S12-P-306ZLATNANSKY Jozef .............................. S02-P-012ZOCATELLI Renata ............................... S11-P-294ZONDERVAN Albert ............................. S05-P-165ZONNEVELD VAN Dicky ....................... S03-P-046ZOPPI Ugo .......................... S02-O-10, S03-P-087ZOTTER Peter ..................... S15-O-04, S15-P-329ZOUARI Kamel ...................................... S13-P-102

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Caption of the abstract authorsMAIN AUTHORPReSenTInG aUTHoR

26

Keynote Lectures

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Monday July 9, KEYNOTE LECTURE 01Optical detection of radiocarbon dioxide at natural and enriched abundance Mazzotti D.

Tuesday July 10, KEYNOTE LECTURE 02Radiocarbon analysis of cell and tissue regeneration in humans Spalding K.

Thursday July 12, KEYNOTE LECTURE 03 Geneste J.M.

27

KEYNOTE LECTURE 01

OPTICAL DETECTION OF RADIOCARBON DIOXIDE AT NATURAL AND ENRICHED ABUNDANCE

GallI I.(1)(2), baRTalInI S.(1)(2), boRRI S.(3), cancIo P.(1)(2), De naTale P.(1)(2), feDI M.(4), ManDÒ P.a.(4)(5), MaZZoTTI D.(1)(2), GIUSFREDI G.(1)(2)

(1) Istituto nazionale di ottica (Ino) - cnR, SeSTo fIoRenTIno fI, ITalY ; (2) european laboratory for nonlinear Spectroscopy (lenS), SeSTo fIoRenTIno fI, ITalY ;(3) Istituto di fotonica e nanotecnologie (Ifn) - cnR, baRI ba, ITalY ; (4) Istituto nazionale di fisica nucleare (Infn) - Sez. firenze, SeSTo fIoRenTIno fI, ITalY ; (5) Dipartimento di fisica e astronomia, Università di firenze, SeSTo fIoRenTIno fI, ITalY.

AbstractRadiocarbon optical detection, based on infrared laser spectroscopy, was proposed more than 30 years ago [1]. Indeed, radiocarbon dioxide (14C16O2) has strongly absorbing ro-vibrational bands at 4.5 μm, making it an ideal target molecular species for radiocarbon sensing, even below its natural abundance (about 1 part per trillion).We have developed a new high-sensitivity spectroscopic technique, named saturated-absorption cavity ring-down (SCAR) [2], benefiting from both advantages of conventional cavity ring-down and saturation spectroscopy. The former allows highly sensitive detection of absolute trace gas concentrations, the latter allows to retrieve the gas absorption signal, subtracting the background due to mirror losses, in the same short ring-down event (100 μs). At low pressure regimes this technique also enables sub-Doppler resolution. A novel cw mid-IR coherent source, based on difference-frequency generation (DFG), has also been developed [3], with tuning range between 3.85 and 4.54 μm, narrow-linewidth, Cs-standard traceability, TEM00 spatial mode, and 30 mW power. By combining the SCAR technique with the DFG source, we have very recently demonstrated experimentally the first radiocarbon detection at natural abundance with all optical technique [4].We report on latest results obtained for detection sensitivity, linearity, and accuracy of laser-based radiocarbon dioxide concentration measurements, with abundance ranging from natural one up to values about 6000-times higher (enriched samples). For intercomparison purposes, radiocarbon content in samples with sub-natural abundance has been measured both by this spectroscopic technique and by AMS [5].We discuss on possible future upgrades of our system, towards an optimization of the averaging time, a reduction of the carbon mass content of the sample, and a more compact, simplified, and transportable optical setup.

References[1] «Radiocarbon dating by infrared laser spectroscopy. A feasibility study», Labrie et al., J. Appl. Phys. A 24, 381 (1981).[2] «Saturated-absorption cavity ring-down spectroscopy», Giusfredi et al., Phys. Rev. Lett. 104, 110801 (2010).[3] «Ti:sapphire laser intracavity difference-frequency generation of 30 mW cw radiation around 4.5 μm», Galli et al., Opt. Lett. 35, 3616 (2010).[4] «Molecular gas sensing below parts per trillion: radiocarbon-dioxide optical detection», Galli et al., Phys. Rev. Lett. 107, 270802 (2011).[5] «The 14C AMS facility at LABEC, Florence», Fedi et al., Nucl. Instrum. Meth. B 259, 18 (2007).

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KEYNOTE LECTURE 02

RADIOCARBON ANALYSIS OF CELL AND TISSUE REGENERATION IN HUMANS

SPALDING K.

Karolinska Institute, STocKHolM, SWeDen

AbstractMuch of the impetus in regenerative medicine is fuelled by the prospect of promoting cell replacement, or blocking unwanted cell production. Without knowing, however, if a specific cell type is renewed in the healthy or pathological situation, it remains uncertain whether it may be realistic and rational to modulate this process. Despite the importance of this information, remarkably little is known about the age of cells in many regions of the adult human brain and body. This is largely due to difficulties in studying this process in humans. Using recently established methodology, which integrates biomedical approaches with recent developments in nuclear physics, it is possible to establish the turnover of cells in human tissues. By measuring 14C derived from nuclear bomb tests in DNA, triglyceride and tooth enamel, it is possible to retrospectively establish the birth date of cells, lipids and humans. Findings of neuronal turnover in the adult human brain, fat cell turnover in humans (lean and obese) and age-determination in humans will be discussed.

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OralCommunications

3030

SESSION 1

CALIBRATION

ConvenersE. Bard (FRA), J. van der Plicht (NLD), P. Reimer (UKGBR)

DescriptionRadiocarbon calibration is essential for correcting for the variability of the initial 14C content of the carbon reservoir where a sample grew or was formed. This session will cover all aspects of calibration including new and/or refined potential calibration data from a variety of archives, regional and/or time-dependent reservoir offsets, statistical methods for calibration and curve construction and techniques which help to constrain past 14C production changes such as 10Be or palaeomagnetics

Keywordscalibration, reservoir ages, 14C production

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S01-INV-01

PROPOSED UPDATE TO THE INTCAL09, SHCAL04 AND MARINE09 RADIOCARBON CALIBRATION CURVES

REIMER P.J.(1), baRD e.(2), baYlISS a.(3), becK J.W.(4), blacKWell P.G.(5), bRonK RaMSeY c.(6), bUcK c.e.(5), eDWaRDS R.l.(7), fRIeDRIcH M.(8)(9), GRooTeS P.M.(10), GUIlDeRSon T.P.(11)(12), HaflIDaSon H.(13), HaJDaS I.(14), HaTTÉ c.(15), HeaTon T.J.(5), HoGG a.G.(16), HUGHen K.a.(17), KaISeR K.f.(18)(19), KRoMeR b.(8), MannInG S.W.(20), nIU M.(5), ReIMeR R.W.(1), RIcHaRDS D.a.(21), ScoTT e.M.(22), SoUTHon J.R.(23), TURneY c.S.M.(24), Van DeR PlIcHT J.(25)(26)

(1) Queen’s University belfast, belfaST, UnITeD KInGDoM;(2) ceReGe, aIX-en-PRoVence, fRance;(3) english Heritage, lonDon, UnITeD KInGDoM;(4) University of arizona, TUcSon, UnITeD STaTeS;(5) University of Sheffield, SHeffIelD, UnITeD KInGDoM;(6) University of oxford, oXfoRD, UnITeD KInGDoM;(7) University of Minnesota, MInneaPolIS, UnITeD STaTeS;(8) Heidelberger akademie der Wissenschaften, HeIDelbeRG, GeRManY;(9) University of Hohenheim, STUTTGaRT, GeRManY;(10) christian-albrechts-Universität, KIel, GeRManY;(11) lawrence livermore national laboratory, lIVeRMoRe, UnITeD STaTeS;(12) University of california - Santa cruz, SanTa cRUZ, ca, UnITeD STaTeS;(13) Universitetet i bergen, beRGen, noRWaY;(14) labor für Ionenstrahlphysik, ZURIcH, SWITZeRlanD;(15) laboratoire des Sciences du climat et de l’environnement (lSce), GIf-SUR-YVeTTe, fRance;(16) University of Waikato, HaMIlTon, neW ZealanD;(17) Woods Hole oceanographic Institution, WooDS Hole, UnITeD STaTeS;(18) Physical Geography, University of Zurich-Irchel, ZURIcH, SWITZeRlanD;(19) Swiss federal Institute for forest, Snow and landscape Research, WSl bIRMenSDoRf, SWITZeRlanD;(20) cornell University, ITHaca, UnITeD STaTeS;(21) University of bristol, bRISTol, UnITeD KInGDoM;(22) University of Glasgow, GlaSGoW, UnITeD KInGDoM;(23) University of california - Irvine, IRVIne, UnITeD STaTeS;(24) University of new South Wales, SYDneY, aUSTRalIa;(25) leiden University, leIDen, neTHeRlanDS;(26) Rijksuniversiteit Groningen, GRonInGen, neTHeRlanDS

AbstractRadiocarbon dates form the basis for many Late Quaternary chronologies in geosciences and archaeology but are not equivalent to calendar ages. Due to the fluctuations in atmospheric levels, radiocarbon dates require calibration before they can be compared and/or combined with date estimates derived from other dating techniques. The need for a consensus calibration curve to cover the entire radiocarbon dating range has been previously recognized but bona fide records of atmospheric 14C levels beyond the absolutely dated tree-rings at 12.594 cal kBP are not yet available [1]. The IntCal09/Marine09 curves were the first attempt by the IntCal Working Group (IWG) to provide calibration curves extending to 50 cal kBP based on carefully screened high-resolution data and robust statistical techniques [2,3]. The IWG recognizes that calibration is a work in progress and that modifications are necessary as more data from suitable archives become available and our understanding of 14C production changes and the earth’s carbon cycle improves.Together with the IntCal Oversight Committee the IWG has screened new and recently

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32

published 14C measurements for inclusion into the proposed updates (IntCal12, SHCal12 and Marine12). The selected records include independently dated tree-rings, speleothems and coral. Also included are the late glacial floating tree-ring chronologies linked to the independently dated tree-rings by wiggle-matching and foraminifera from marine sediments with timescales derived using a Gaussian process sediment age-depth model and tie-points with the revised Hulu Cave δ18O record. Together with previous calibration datasets, these new measurements and revisions provide the opportunity to evaluate offsets observed between records and consider the physical processes responsible. The group has constructed radiocarbon calibration curves, using appropriate uncertainty estimates and bespoke statistical techniques. We expect these curves to be another step along the path towards what everyone can agree is a calibration in the true sense of the word. We will also discuss plans for future refinements.

References[1] Schaub, M., et al., lateglacial environmental variability from Swiss tree rings. Quaternary Science Reviews,

2008. 27(1-2): p. 29-41.[2] Heaton, T.J., P.G. Blackwell, and C.E. Buck, A Bayesian approach to the estimation of radiocarbon calibration

curves: the IntCal09 methodology. Radiocarbon, 2009. 51(4): p. 1151-1164.[3] Reimer, P.J., et al., IntCal09 and Marine09 radiocarbon age calibration curves, 0 - 50,000 years cal BP.

Radiocarbon, 2009. 51(4): p. 1111-1150.

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S01-O-02

ELASTIC TIEPOINTING – TRANSFERRING CHRONOLOGIES BETWEEN RECORDS

HEATON T.J.(1), baRD e.(2), HUGHen K.a.(3)

(1) University of Sheffield, SHeffIelD, UnITeD KInGDoM;(2) ceReGe, aIX-en-PRoVence, fRance;(3) Woods Hole oceanographic Institution, WooDS Hole, UnITeD STaTeS

AbstractConsider the situation where we are presented with a depositional record we wish to date but which does not possess any direct age information of its own. In such instances it may however still be possible to identify a set of depths within the unknown record that can be tied or matched to a reference record which does have age information. These tie points may typically be expected to correspond to either approximately or exactly contemporaneous events seen in both records or events separated by a known or estimated time period.In this talk we present a general and portable methodology for the transfer of dating information from a reference record (Hulu Cave) to un-dated records of interest (Cariaco Bassin, Iberian and Pakistani Margins) via such elastic tie-pointing. Our approach creates a full chronology for the new record using Gaussian Processes and importantly provides a clear and justifiable handling of potential uncertainties at all stages of the process.We are able to account for uncertainty not solely in the dating information of the reference record but also in the identification and contemporaneity of the tie-points themselves. Furthermore our method also allows the transfer of the dependence structure that will always be created in age-depth modelling of the reference record to the new chronology. The incorporation and acknowledgement of such dependence is important since its presence

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34

S01-O-03

NEW INSIGHT INTO THE RADIOCARBON CALIBRATION USING 14C AND U-TH AGES OF CORALS DRILLED OFFSHORE TAHITI (IODP EXPEDITION #310)

DURAND N.(1) (2), DeScHaMPS P.(1), baRD e.(1), HaMelIn b.(1), caMoIn G.(1), THoMaS a.l.(3), HenDeRSon G.M.(3), YoKoYaMa Y.(4) (5) (6)

(1) ceReGe, aix-Marseille Univ, cnRS, IRD, collège de france, Technopole arbois, bP 80, aIX-en-PRoVence, fRance; (2) now at: lMc14 UMS 2572, cea Saclay, 91191, GIf-SUR-YVeTTe, fRance; (3) Department of earth Sciences, South Parks Road, oXfoRD, oX1 3an, UnITeD KInGDoM;(4) atmosphere and ocean Research Institute and Department of earth and Planetary Science University of Tokyo, 5-1-5

Kashiwanoha, Kashiwashi, cHIba 277-8564, JaPan; (5) national Institute of Polar Research, Tachikawashi, ToKYo 190-8518, JaPan; (6) Institute of biogeosciences, JaMSTec, YoKoSUKa, JaPan.

AbstractBeyond the high-precision tree-ring calibration, the fossil shallow-water tropical corals constitute a suitable and reliable marine archive that can be used to calibrate the radiocarbon time scale. In this contribution, we present a new radiocarbon dataset based on paired 14C and U-Th dating of fossil shallow-water corals drilled offshore Tahiti during the IODP Expedition 310 «Tahiti Sea-Level». In order to select pristine aragonitic coral skeletons and avoid those displaying any post-mortem diagenesis that alters original ages, rigorous mineralogical and geochemical screening criteria have been applied. In particular, we made a significant effort to improve detection and quantification of very small amount of secondary calcite in the aragonitic coral lattice using X-ray diffraction measurements [1]. In addition, the new Tahiti dataset allow to refine the previous tolerance range of the screening criterion based on the initial (234U/238U)0 ratio previously adopted. More than 60 14C dates were processed at the Laboratoire de Mesure du Carbone 14 (ARTEMIS AMS facility, Saclay, France). The Tahiti record provides new data to the radiocarbon calibration for two distinct time windows: 7 data for the interval between 29 and 36 cal kyr BP and 58 for the last deglaciation period, with, especially, a higher resolution for the 14-16 cal kyr BP time interval.These new data extend the previous Tahiti record beyond 13.9 cal kyr BP, the oldest U-Th age obtained on cores drilled onshore in the modern Tahiti barrier reef [2,3]. The results obtained on Tahiti corals for the radiocarbon calibration curve are compared with 14C chronologies from other corals [4,5] from marine sediments [6,7] and from speleothems [8,9] records.The new 14C dataset from the corals drilled offshore Tahiti allows to validate the precision and accuracy of other records either directly dated by U-Th or tuned to a dated target, with a special emphasis for the Heinrich 1 event for which there is a debate about the discrepancies observed between the different records [10]. For this time period, the Tahiti record supports the few data from the Iberian Margin and from the previous coral records, but is in clear disagreement with the Cariaco Basin record. The Tahiti record also allows to refine the significant variations of the atmospheric Δ14C during Bølling warming period, that might reflect complex changes in the global carbon cycle due to variations in the rates of exchange between the different carbon pools.

References1. Sepulcre et al. 2009, Global Planet change 66, 12. Bard et al. 1996, nature 382, 2413. Bard et al. 2010, Science DOI:10.1126/science.11805574. Fairbanks et al. 2005, Quaternary Sci Rev 24, 17815. Bard et al. 1998, Radiocarbon 40(3), 10856. Hughen et al. 2006, Quaternary Sci Rev 25, 32167. Bard et al. 2004, Science 303, 1788. Hoffmann et al. 2010, earth Planet Sc lett 289, 19. Southon et al. 2012,Quaternary Sci Rev 33, 32

10. Reimer et al. 2009, Radiocarbon 51, 1111.

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S01-O-04

ELASTIC TIEPOINTING – TRANSFERRING CHRONOLOGIES BETWEEN RECORDS

FAIRBANKS R.(1), MoRTlocK R.(1), abDUl n.(1), WRIGHT J.(1), cao l.(2)

(1) University of Sheffield, SHeffIelD, UnITeD KInGDoM;(2) ceReGe, aIX-en-PRoVence, fRance;(3) Woods Hole oceanographic Institution, WooDS Hole, UnITeD STaTeS

AbstractA recent coral drilling expedition offshore Barbados provides abundant new pristine coral samples for improving the resolution of our radiocarbon calibration curve. In total, more than 600 radiocarbon measurements and over 500 230Th /234U dates have been completed using our new and existing offshore drill cores and include the dating of the raised Araki reefs. Twenty-five concordant paired 230Th /234U and Pa/U dates have been measured to demonstrate quality control of the uranium dating system. Forty-two inter-calibration measurements have been made comparing leading AMS laboratories. Combined with published tree ring and coral paired 14C and 230Th /234U dates that adopted our rigorous sample quality control criteria, an improved stand alone coral radiocarbon calibration curve is presented.We assert that it is imperative that any radiocarbon calibration curve be constructed of radiocarbon-dated samples that also have an independent and reliable calendar age estimate. Tree rings and corals meet this criterion. Radiocarbon calibration reliance on radiocarbon dated marine sediments that are calendar dated via imported age models from other climate archives is unsatisfactory and will not stand the test of time. A good example is the INTCAL MARINE09 calibration through the “Mystery Interval” that is offset by as much as 800 calendar years from new paired 14C and 230Th /234U data (see Mortlock et al., 2012; this meeting). Dozens of abstracts and papers are likely affected by this mistake and considerable research resources may have been targeted to projects based on an inaccurate time interval of the MARINE 09 calibration curve. Equally important, a radiocarbon calibration curve should not be based on absolute ages inferred from correlating climate proxies from one dated archive to another. This negates the independence of the age models based on radiocarbon calibration from the climate system that is the subject of study. Paleo-research relies heavily on deducing leads and lags of various parts of the climate system and their frequencies. The radiocarbon calibration must therefore be completely independent of the climate system. For example, anyone familiar with the physics of oxygen isotope fractionation should hesitate to correlate an oxygen isotope record from Asian speleothems to color changes in semi-laminated sediments in a restricted basin offshore Venezuela. Although surface corals must have reservoir corrections applied to their radiocarbon ages, we show that the assumption of constant reservoir age over time may be most reasonable for the western Atlantic warm pool where Barbados is located. We conclude that the estimated reservoir age uncertainty is small compared to the radiocarbon analytical uncertainty for samples older than 14,000 years BP.

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S01-O-05

IMPLICATIONS OF THE 55ka ATMOSPHERIC RADIOCARBON RECORD FROM LAKE SUIGETSU, JAPAN

BRONK RAMSEY C.(1), STaff R.a.(1), bRYanT c.l.(2), bRocK f.(1), KITaGaWa H.(3), Van DeR PlIcHT J.(4), ScHlolaUT G.(5), MaRSHall M.H.(6), bRaUeR a.(5), laMb H.f.(6), PaYne R.l.(7), TaRaSoV P.e.(8), HaRaGUcHI T.(9), GoTanDa K.(10), YonenobU H.(11), YoKoYaMa Y.(12), naKaGaWa T.(7)

(1) University of oxford, oXfoRD, UnITeD KInGDoM;(2) neRc Radiocarbon facility - environment (nRcf-e), Scottish enterprise Technology Park, eaST KIlbRIDe, UnITeD KInGDoM;(3) Department of earth and environmental Sciences, nagoya University, naGoYa, JaPan;(4) Department of Isotope Research, energy and Sustainability Research Institute, University of Groningen, GRonInGen,

neTHeRlanDS;(5) German Research center for Geoscience (GfZ), PoTSDaM, GeRManY;(6) Institute of Geography and earth Sciences, aberystwyth University, abeRYSTWYTH, UnITeD KInGDoM;(7) Department of Geography, University of newcastle, neWcaSTle-UPon-TYne, UnITeD KInGDoM;(8) Institute of Geological Sciences, Palaeontology, freie Universität berlin, beRlIn, GeRManY;(9) Department of biology and Geosciences, osaka city University, oSaKa, JaPan;(10) faculty of Policy Informatics, chiba University of commerce, cHIba, JaPan;(11) college of education, naruto University of education, naRUTo, JaPan;(12) Department of earth and Planetary Sciences, faculty of Science, University of Tokyo, ToKYo, JaPan;

AbstractThe lake sediment of Suigetsu, Japan (Kitagawa and van der Plicht, 1998 and Nakagawa et al. in press), provides us with a continuous record of atmospheric radiocarbon extending over the last ~55 ka BP. The chronology for this sequence of radiocarbon dates is constrained not only by the ordered and relatively uniform sedimentation rate, but also, for the Glacial period, by varves produced as a result of the annual cycle of seasonal deposition. This gives us very good relative age control. For the Holocene period and end of the Late Glacial, we can link the chronology to that of the tree-ring data compiled in the IntCal09 calibration curve (Staff et al. 2011, Reimer et al. 2009).This paper will look at the implications of this comprehensive dataset in relation to other global records of radiocarbon deriving from the oceans. The paper will discuss the different ways in which we might consider records with direct dating evidence (corals) and those where the linkage to an absolute timescale is based on assumptions of climate synchrony (foraminifera). The paper will also explore the difficulties in interpreting some of the data from different records at the older end of the spectrum (>30 ka BP).The continuous atmospheric record from Suigetsu clearly has implications for calibration, but also for our understanding of the ways in which the different elements of the earth system record the radiocarbon signal, and the timescales that we apply to those records.

References1. Kitagawa H. and van der Plicht J. (1998) Science 279, 1187-1190.2. Nakagawa T. et al. (in press) Quaternary Science Reviews.3. Staff R.A. et al. (2011) Radiocarbon, 53 (3) 511-528.4. Reimer P.J. et al. (2009) Radiocarbon, 51 (4) 1111-1150.

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S01-O-06

NEW ZEALAND KAURI YOUNGER DRYAS RESEARCH PROJECT – SCOPE AND INITIAL RESULTS

HOGG A.(1), PalMeR J.(2), TURneY c.(3), SoUTHon J.(4), bRonK RaMSeY c.(5), fenWIcK P.(6), KRoMeR b.(7), WacKeR l.(8), JoneS R.(2)

(1) University of Waikato, HaMIlTon, neW ZealanD;(2) University of exter, eXeTeR, UnITeD KInGDoM;(3) University of new South Wales, SYDneY, aUSTRalIa;(4) University of california, IRVIne, UnITeD STaTeS;(5) University of oxford, oXfoRD, UnITeD KInGDoM;(6) Gondwana Tree-Ring laboratory, cHRISTcHURcH, neW ZealanD;(7) University of Heidelberg, HeIDelbeRG, GeRManY;(8) laboratory of Ion beam Physics, ZURIcH, SWITZeRlanD

AbstractThe Younger Dryas (YD) cold event, from ca 12,950 to 11,600 cal BP has been closely scrutinized by Quaternary geologists, paleoclimatologists and archaeologists for more than two decades. Research focused upon the causes, timing, duration, geographic extent and impact on hunter-gatherer groups of this important cooling episode, has been hampered by inconsistencies in radiocarbon, ice core and varve chronologies.Hua and colleagues in 2009 made an important contribution towards improving the radiocarbon chronology by decadal measurement of a 617-yr-long floating sequence of tree-rings of Huon pine from Tasmania, Australia. However, the huon pine sequence, which is composed of only 4 logs which could not be cross-matched by ring-width correlations, relies upon 14C wiggle matching thereby introducing extra uncertainties. In addition, the 617-yr huon chronology provides minimal over-lap between the older Lateglacial Pine and younger absolute European tree-ring chronologies.We describe here a new initiative using New Zealand kauri, which will not only significantly improve linkage of the floating Lateglacial Pine record to the absolute tree-ring timescale, but will also increase the sample density of both records.The 1450-yr-long New Zealand YD kauri chronology, which is constructed from 30 (26 new and 4 original) trees, is also floating and presently spans the time interval ca 12,860 - 11,700 cal BP. We present dendrochronology data showing that approximately 1150 (EPS>0.85) years are securely cross-matched, with efforts continuing to increase replication for the remaining 150 years at each end.Sequential, decadal 14C tree-ring samples are currently being analyzed by 3 carbon dating laboratories – University of California at Irvine (UCI - AMS), University of Oxford (OxA - AMS) and University of Waikato (Wk – radiometric, LSC), with additional analyses by the Laboratory of Ion Beam Physics (ETH - AMS) and University of Heidelberg (Hd – radiometric, GPC). We compare analytic procedures for the participating laboratories, including chemical blank correction, and the efficacy of various pretreatment regimes (ABA, holo-cellulose and alpha-cellulose) for removing modern contamination from sub-fossil wood.We also present the results for 12 successive decadal samples analyzed by all 5 laboratories for Quality Assurance purposes and discuss possible causes and implications of inter-lab variability.

ReferencesQ Hua et al., 2009. Atmospheric 14C variations derived from tree rings during the early Younger Dryas. Quaternary Science Reviews, doi:10.1016/j.quascirev.2009.08.013.

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S01-O-07

TESTING THE POTENTIAL OF A STALAGMITE FROM NE INDIA FOR EXTENSION OF THE 14C CALIBRATION CURVE

HAJDAS I.(1), beITenbacH S.f.M.(2), GIeRGa M.(2), HaUG G.H.(2), aDKInS J.f.(3), bIecHele c.(1), bonanI G.(1), MaUReR M.(1), WacKeR l.(1)

(1) laboratory of Ion beam Physics, eTH, ZURIcH, SWITZeRlanD;(2) climate Geology, eTH, ZURIcH, SWITZeRlanD;(3) Geological Planetary Sciences calTecH, PaSaDena, UnITeD STaTeS

AbstractArchives that date close to the limit of the radiocarbon time scale and can provide additional information about 14C variability are rare.Stalagmite MAW-3 has been collected in 2006 from Mawmluh Cave, Meghalaya, NE India and subsequently U-series dated at Caltech. Stable isotopes (δ13C and δ18O) were measured at the Geological Institute of the ETH Zurich.MAW-3 grew through a large part of Marine Isotope Stage 3 and stable isotope results clearly show millennial scale climatic fluctuations known as Dansgaard-Oeschger events. U-series dating shows that our sample covers the time interval corresponding to the geomagnetic low intensity interval, called Laschamp Event at ca. 40 ka BP. Therefore, we test its usefulness for studies of potential 14C variability at the time.Samples for 14C dating were taken following the method of Hoffman et al. (2010). After preparation of a slab from the centre of the stalagmite small sub-samples for 14C and U-series analysis were cut with a wire saw. Samples containing ca. 10 mg of carbonate were dissolved in concentrated (85%) phosphoric acid and graphitized prior to AMS analysis at the ETH AMS facility.Preliminary results indicate that despite of the very high correction for the dead carbon fraction DCF (ca. 6000 14C yrs) and close proximity to the limit of the 14C dating method, we are still able to measure reliable 14C ages of this portion of MAW-3. We show a series of ages for comparison with other records. Moreover, we argue that, based on available results, fluctuations of DCF could be reconstructed. DCF changes show a correlation with stable isotope changes (δ18O), i.e. precipitation patterns in the region.

ReferencesHoffmann, D.L., Beck, J.W., Richards, D.A., Smart, P.L., Singarayer, J.S., Ketchmark, T., and Hawkesworth, C.J., 2010, Towards radiocarbon calibration beyond 28 ka using speleothems from the Bahamas: Earth and Planetary Science Letters, v. 289, p. 1-10.

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SESSION 2

ADVANCES IN PHYSICAL MEASUREMENT TECHNIqUES OF RADIOCARBON, AND OTHER

LONG-LIVED RADIONUCLIDES

ConvenersA. Hogg (NZL), J. Southon (USA), H.S. Synal (CHE)

DescriptionThis session aims to provide a comprehensive overview on the latest developments in measurement technology, particularly for Radiocarbon, but also including other long-lived radionuclides.The session also focuses on advances in sample preparation and handling procedures. Here we expect AMS contributions on ion sources (conventional sputter or hybrid systems), gas interfaces to ion sources, ultra small (micro gram size) sample preparation and measurement procedures. Radiometric contributions could include quench correction in liquid scintillation counting. Contributions on improvements in background blank assessment (applicable to all methods) will be welcome.In addition, we encourage contributions on alternative methods such as laser-based spectroscopy or conventional mass spectrometric systems.

KeywordsAMS, Ion source, micro gram samples, new detection technologies, liquid scintillation counting, gas proportional counting

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S02-O-01

14C ENRICHMENT IN SAMPLES BY ULTRA-CENTRIFUGE: FINALLY A REAL EXTENSION OF THE AGE LIMIT

De RooIJ M.(1), GRoen c.P.(2), KolKMan H.W.(2), aeRTS-bIJMa a.T.(1), been H.a.(1), JanSen H.G.(1), Van DeR PlIcHT J.(1), MEIJER H.A.J.(1)

(1) centre for Isotope Research, University of Groningen, GRonInGen, neTHeRlanDS;(2) Urenco nederland b.V., alMelo, neTHeRlanDS

AbstractEnrichment of 14C in samples (isotope separation, concentrating 14C in a fraction of the original sample) to extend the possible age limit of 14C dating, is an old idea (Haring et al. 1958). The method exclusively used so far is thermodiffusion. CO (and sometimes CH4) has been used for this process, and enrichment factors up to almost 10 have been reported.The enrichment process as such worked fine, and even quantities large enough for proportional counters could be enriched (Grootes et al., 1975). Nevertheless, in terms of age extension the attempts failed, because the 14C background (contamination with «modern» C) in old samples and «dead» references was too high, and variable. Furthermore, the huge amount of sample required, the large installation and the long enrichment times impaired extensive data collection (and thus for example a detailed study on sources of background).This situation improved when samples could be prepared for AMS (Kitigawa and van der Plicht, 1997). Again, however, the enrichment process resulted merely in co-increasing the background, such that the age limit was not improved. The extra treatment of the sample in the form of the reduction of CO2 to CO contributed to this extra background.In our present attempt, therefore, we have concentrated on reducing the modern background in all our normal procedures (see our contributions elsewhere in the conference). Furthermore, we had the opportunity to use a totally different technique for enrichment: an ultra-centrifuge (originally developed for uranium enrichment for the nuclear power industry). These ultra high vacuum machines offer a very clean environment, and enable the direct enrichment of CO2. This fact, together with extreme care in all sample and standard preparation steps, resulted in a clear extension of the age limit. In our first experiments, the enrichment was still modest (about a factor of 2.5). We could indeed realise the theoretical age extension of 7500 years, as both our background level and its variability were virtually the same before and after enrichment.As a first demonstration of this enrichment technique, we dated a large mammoth bone from Khatanga (Siberia*), which –before enrichment- was on the edge of significantly different from background (net activity 0.10 ± 0.05 %, 1σ). After the enrichment process, its net activity was 0.45 ± 0.05 %, corresponding to an original activity of 0.18 ± 0.02 %, or equivalently to 50800 (+950,-850) BP. The background variability level we have achieved this way would result in a (2σ) age limit of 63000 BP.

References1. A. Haring et al., 1958. Radiocarbon Dating Up to 70,000 Years by Isotopic Enrichment. Science, 128, pp. 472-4732. Grootes, P.M., et al., 1975. Enrichment of Radiocarbon for dating samples up to 75,000 years. Z. N.forsch. 30A, 1-143. Kitagawa, H., & J. van der Plicht 1997: Enrichment of sub-milligram size carbon sample, NIM B 123, 218-220. *Obtained from Dr. A. Tikhonov, St. Petersburg

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S02-O-02

A SIMPLE WAY OF UPGRADING A COMPACT NEC-RADIOCARBON AMS FACILITY FOR 10Be

MÜLLER A.M.(1), SUTeR M.(1), fU D.(2), DInG X.(2), lIU K.(2), ZHoU l.(2)

(1) laboratory of Ion beam Physics, eTH Zurich, ZURIcH, SWITZeRlanD; (2) State Key laboratory of nuclear Physics and Technology and Institute of Heavy Ion Physics, Peking University, beIJInG, cHIna

AbstractToday, 14C and 10Be are the most important isotopes measured by AMS. For radiocarbon, compact facilities operating at terminal voltages in the range of 0.2-1 MV are available. The ETH AMS group has demonstrated that energies above 700 keV are sufficient to perform 10Be analysis and therefore this category of compact instruments has also some potential for 10Be measurements. In this paper we show a simple way of upgrading a dedicated radiocarbon NEC facility (500 kV) at the Peking University for 10Be measurements. First ion optics calculations for the transport of 10Be have been performed for the high energy system and the appropriate focal planes have been determined. Then a silicon nitride foil for the degrader method was mounted and a new faraday cup for the measurement of 9Be was installed. The Si-detector at the end of the beam line was replaced with a high resolution gas ionization chamber with a 4 x4 mm entrance window. First tests with this arrangement showed promising results: The 10Be background was at the level 3.5 10-14 and an overall transmission for 10Be of 2% has been obtained. Also very good stability and reproducibility for standards and blank has been found. It is planned to add a second magnet for reducing background and refocusing the energy spread introduced by the silicon nitride foil. With this final arrangement a performance with background levels at 10-15 and transmissions of 10Be of 6-8 % are expected. Our design has the advantage, that the existing components can be used; the size of the arrangement is very compact and the radiocarbon measurements are not affected by the modifications.

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S02-O-03

A LARGE-ACCEPTANCE TANDETRON AMS SYSTEM

VON REDEN K.F., lonGWoRTH b.l., lonG P., RobeRTS M.l.

Woods Hole oceanographic Institution, WooDS Hole, UnITeD STaTeS

AbstractThe trends in modern AMS have been toward smaller sample size, higher precision and ever smaller AMS systems. While small systems are highly competitive regarding measurement quality, they usually have higher levels of background in the 14C detector. Ultimately, the size of the background signal determines the minimum samples size or the level of precision that is achievable with any AMS system. Following a study on improvements of the NOSAMS Tandetron1, we designed a new large-acceptance sequential injector that, together with the highly selective Dipole-ESD-Dipole high-energy analysis section, will reduce background to unprecedented levels for our system. We also expect the ion efficiency (ions analyzed versus carbon atoms sputtered) to go up significantly due to the increased acceptance (~50 π mm mrad for the upgraded system versus ~20 π mm mrad for the old Recombinator injector). Here, we present first results obtained with the new injector.

ReferencesK.F. von Reden, “Future of the NOSAMS Tandetron AMS System”, NIMB 268 (2010) 854ff.

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S02-O-04

PHYSICS AND CHEMISTRY OF A 15 KeV ABSOLUTE ISOTOPE RATIO MS FOR 14C

VOGEL J., GIacoMo J., DUeKeR S.

Vitalea Science, DaVIS ca, UnITeD STaTeS

AbstractAn “absolute” measurement without normalization of instrument response arises only from use of a fundamental dependence of quantification on a physical process which is measured without prejudice to at least the stated accuracy. Absolute isotope ratio measurements allow development of directly linked separation, such as UPLC-IRMS, without use of internal reference standards. Absolute 13C/12C ratios from the same measurement permit wide range isotope dilution determination of natural sample masses within a carrier without reference standards. Ratio depencence on sample size is also minimized in an absolute spectrometer. We identified the dependence of gas collision charge-exchange on projectile velocity as physical process capable of producing absolute measurements after finding that AMS measured OxII SRM to 2.2‰ average accuracy over one year despite the 1% precision of the measurements. AMS results are reported as absolute isotope ratios, correcting the raw 14C/13C count-rate per ion-current only for counting deadtime, the assumed sample ∂13C (-20‰ for biological samples), and a fixed transmission ratio between the isotopes of 1.077 (14/13) that is specific to anion-gas collisions at 235 keV. A differential model of charge-changing transmission through gases uses as complete a set of collision cross sections as can be found to define a set of analytic functions that control the differential progression of carbon anions, atoms, and cations through argon. The model predicts that 14C transmission equals that of 13C at 15 keV (17%) and at 65 keV (13%). 13C transmission equals that of 12C at slightly lower energies. As at 235 keV, 14C/13C transmissions are inversely proportional to ion mass at 6.5 and 115 keV collision energies. Methylidyne (CH) dissociation was also modeled using the few available data and functions derived from carbon data. This highly reactive radical ion is easily destroyed at low (chemical) energies (0.01-10 eV) by dissociative recombination (DR). Chemical reactivity can be exploited to reduce collision cell density for lower ion losses. A lab-sized instrument (1m x 1m x 1m) is described that uses anions not only in the ion source but also in MS sectors to minimize scattered backgrounds. The required fractionation-free negative ion source is discussed elsewhere.

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S02-O-05

HIGH CURRENT 14C MEASUREMENTS ON A HVE 1 MV AMS SYSTEM

KLEIN M., GoTTDanG a., MoUS D.J.W.

High Voltage engineering europa b.V., aMeRSfooRT, neTHeRlanDS

AbstractHigh 14C sample throughput is an increasingly important characteristic of AMS systems, which in turn requires high source output. For this, the HVE AMS systems apply the model SO-110B ion source, which can run at outputs of more than 200 µA 12C. It is known that high source output may compromise the precision. To quantify this effect, we have tested on an HVE 1 MV AMS system the influence of moderate (<50 µA), medium (100 µA) and high (200 µA) source outputs on the precision. These early measurements indicate for 200 µA 12C- source output, equivalent to ~600 Hz 14C count rate for Ox II samples, a 13C/12C precision below 2 ‰, and a 14C/12C precision below 0.5 %.

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S02-O-06

PROGRESS IN MASS SPECTROMETRIC RADIOCARBON DETECTION TECHNIqUES

SYNAL H.A., SeIleR M., SUTeR M., WacKeR l.

eTH Zurich, ZURIcH, SWITZeRlanD

AbstractAccelerator Mass Spectrometry (AMS) has been established as the best-suited radiocarbon detection technique in particular, in cases where only minute amounts of sample materials are available. In the past ten years, significant progress with AMS instrumentation has been made resulting in a boom of new AMS facilities around the World. Today, carbon only AMS systems predominantly utilize 1+ charge state and molecule destruction in multiple ion gas collisions in stripper gas cell. This has made possible a significant simplification of the instruments, a reduction of ion energies and related to this less required space and costs of the installations. However, state-of-the-art AMS instruments have still not reached a development stage where they can be regarded as table-top systems comparable to e.g. standard mass spectrometers. In this respect, more development is needed to further advance the applicability of radiocarbon not only in the traditional fields of dating but also in biomedical research and new fields in Earth and environmental sciences.Based on the proof-of-principle experiment to demonstrate the feasibility of radiocarbon detection over the entire range of dating applications using a pure mass spectrometer at ion energies below 50 keV, we have now set-up an experimental platform to test performance and to explore operation and measurement conditions of pure mass spectrometric radiocarbon detection. We will overview the physical principles which make this development possible and discuss key parameters of the instrumental design.

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S02-O-07

STUDY OF CO2 ABSORPTION AND NEGATIVE ION FORMATION DURING DIRECT IONIZATION OF CO2 WITH A CS+ BEAM

SALAZAR G., oGnIbene T.

lawrence livermore national lab, lIVeRMoRe, UnITeD STaTeS

AbstractSecondary ionization (SIMS) by the interaction of a high-energy Cs+ beam with carbon graphite is widely applied in AMS. It has been used to directly create C- from injections of CO2 when the gas is brought in contact with a metal surface (ca titanium) and the Cs+ beam. The ionization process is still not well understood. From SIMS theories, this negative ionization can be seen as: CO2 (absorbed) + high energy --> C- + O- + other negative ions + neutrals. In this work, we studied the CO2 absorption process, the negative ions and neutral products of the ionization reaction of CO2. The experiment consisted on leaking CO2 into a gas-accepting AMS source. A silica capillary (180 μm ID, 3 m long) connected a pressurized CO2 tank with the ion source and the gas flow was selected with a mass flow controller. The silica capillary was connected to the stainless steel tubing (1/16 OD) feedthru of the ion source. The end of the feedthru tubing was in tight contact with the back of a modified Cs+ beam target. Inside of the target, the gas flowed through cavities that directed the CO2 onto a Ti surface where the Cs+ beam was continuously sputtering at 9 keV. The negative ions were accelerated at 49 keV; then guided through an extractor, einzel lenses, steerer lenses; analyzed with an electromagnetic sector and detected with a Faraday Cup at 45 deg. In the absorption study, pulses of CO2 were injected with a constant flow of helium. The amount of C-, detected as m/z 12, represented the amount of absorbed CO2 on the Ti surface. The CO2 transient pressure on the surface depended in the amount of injected CO2 and this pressure was semi empirically determined with computer simulations. The data of absorbed CO2 vs CO2 pressure was interpreted with the Jovanovic-Freundlich isotherm model. It was found that the absorbed CO2 reached a saturation point, similar as any other absorption system. At optimum conditions, the ionization efficiency was 1% and it was affected by how the CO2 was directed onto the surface (aerodynamics). Thermodynamic parameters were extracted from the model and they were in good agreement with other works. The study of the ionization products showed that the most abundant negative ions were O-, CO- and C-. The O-/C- proportion was 6/1. Other ions were Ti-, Al2- and a small amount of H- coming from water contaminant and metal parts. The detected neutrals were CO2, CO, C, O, O2, H2O, OH, N2, N. These results explain the low ionization efficiency because most of the charge goes into O, followed by CO and C (electron affinity order). In addition, only a fraction of the CO2 molecules fragment completely into C. A considerable amount becomes CO or stays as CO2 neutral.Work performed at the Research Resource (RR) for Biomedical AMS, which is operated at LLNL under the auspices of the U.S. DOE under contract DE-AC52-07NA27344. The RR is supported by the NIH, NCRR, Biomedical Technology Program grant #P41 RR13461.

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S02-O-08

SIMULATIONS OF THE ARTEMIS AMS FACILITY OF LMC14, BY TRANSPORT AND GEANT4 NUCLEAR COMPUTER TOOLS

QUILES A.(1)(2), beRTHIeR b.(3), baVaY D.(2), MoReaU c.(2)

(1) lSce, GIf SUR YVeTTe, fRance;(2) lMc14, SaclaY, fRance;(3) IPn orsay, oRSaY, fRance

AbstractThe Artemis facility is a NEC Accelerator Mass Spectrometer (AMS) installed in 2003 at Saclay in France and dedicated to radiocarbon dating. It routinely measures 4500 samples a year for French organizations covering a large field of research (e.g environmental science, archaeology, geology…). We focused on the settings of the beam line facility as sample’s age measurements can be distorted by loss of ions. The aim of the present work is to evaluate this age measurements’ dependence on the beam line settings’ variability, by using nuclear physics simulation tools.The most sensitive parts of the machine were first identified. The trajectories and interactions of the carbon ion beams across the elements along the beam line were simulated using the complementary Transport and Geant4 calculation codes. Using the Transport tool, we obtained the X-Y envelopes and emittance of the beam, ensuring that there was no beam loss, and we identified the most sensitive points of the facility. Then, we used the Geant4 tool-kit to simulate the interactions of the incident ions in different media. These simulations took into account the physical processes involved: magnetic and electrostatic deflections, energy loss and straggling. We were then able to establish the tolerances of the settings on electric and magnetic fields as well as the acceptance of the beam. Finally, we proposed, by simulation, an optimization of the detector which would allow to subtract 13CH and 12CH2 molecular ions from the counting of 14C ions.After a brief description of the Artemis facility to highlight physical processes involved, we will detail the simulation’s tools that we used and their implementations. An ion beam simulation of the full beam line will be presented, as well as the comparison of simulated settings’ acceptance of the different parameters with experimental data.

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S02-O-09

A REFINED STUDY OF KF3- ATTENUATION IN AN RFq GAS CELL FOR

41CA AMS

ZHAO X.

University of ottawa, oTTaWa, canaDa

AbstractIn recent years, the use of a radiofrequency quadrupole RFQ gas cell for isobar separation, as implemented in the Isobar Separator for Anions (ISA), has been shown to have great potential for AMS measurement of, for example, 36Cl, 90Sr and 135,137Cs using small tandem accelerators. The first prototype of the ISA was designed only as a proof-of-principle instrument with a single cooling/reaction cell. The design of a production-orientated version requires that detailed attention must be paid also to ion optics and gas flow. The beam optics before and after the ISA, including the ISA column itself, have been simulated using SIMION-8.1, and the main sources of several inefficiencies have been identified. Modifications of the original prototype, based on these calculations, has resulted in a much improved system, which has allowed us to reinvestigate, with greater refinement, the case for CaF3

-/KF3

- separation. This study was preceded by a theoretical calculation of the detailed properties of KF3

– [1] indicating the unique nature of that superhalogen anion. The new experimental results show that KF3

-, entering the single gas cell at 5-7 eV, can be readily attenuated in ≈ 2 mTorr of CH4 by 2 orders of magnitude with no significant loss to the superhalogen CaF3. The destruction of KF3

- was found in this case to be accompanied by the formation of KF2-,

and all fluxes were found to remain steady from 2.5 to 8 mTorr pressure in the 23 cm long gas cell. Furthermore, it was found that the KF3

- attenuation can be extended another order of magnitude by applying a larger axial electric drift gradient in the gas cell, to maintain a larger forward ion momentum which naturally decreases due to the non-reactive cooling collisions. These findings suggest strongly that the destruction of KF3

- is energy dependent, that it requires a modest threshold of about 1-5 eV to occur, which is yet still not sufficient to trigger processes that might also lead to CaF3

- losses. The results reported here already indicate the feasibility of an efficient small 41Ca ISA-AMS system for cosmogenic and medical applications with a sensitivity of 41Ca/Ca ≈ 10-14. It could be expected that with an ISA that utilizes segmented RFQ rods [2], KF3

- attenuation could be extended still further at no significant loss to CaF3

-, making it widely useful for small AMS systems.

References[1] S. Lo and A.C. Hopkinson, computational and Theoretical chemistry, 973 (2011) 9[2] Jean-François Alary et al., Design of a commercial ISa for aMS applications, in this conference

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S02-O-10

δ13C AND HIGH PRECISION RADIOCARBON DATING

ZOPPI U.(1), KRoMeR b.(2), HeIneMeIeR J.(3)

(1) accium bioSciences, SeaTTle, Wa, UnITeD STaTeS;(2) curt-engelhorn-centre for achaeometry, MannHeIM, GeRManY;(3) University of aarhus, aaRHUS, DenMaRK

AbstractHigh precision radiocarbon dating with uncertainties as low as 20-25 years are becoming common practice. However, to obtain similar accuracies, the excellent counting statistic must be supplemented by very accurate δ13C values. In this paper we investigate whether it is better to use δ13C values measured on a stable isotope mass spectrometer or determined during the AMS experiment itself.We present the results of a statistical analysis of more than a thousand cathodes measured using the 0.5 MV NEC AMS system at Accium BioSciences in Seattle and the 200 keV MICADAS AMS systems in Mannheim. The distribution of the differences in δ13C values is analyzed in details. Particular emphasis is placed on the determination of the fractionation taking place during reduction, as evidenced by a slightly skewed distribution for certain sample types, and its influence on the reliability of final results.

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SESSION 3

ADVANCES IN RADIOCARBON PRETREATMENT PROTOCOLS

ConvenersP. Ascough (GBR), K. Douka (GBR), A. Zazzo (FRA)

DescriptionPretreatment chemistry is one of the most important parameters in the application of radiocarbon dating and like other factors that affect dating accuracy it is continuously upgraded. Over the last decade, a suite of methodological advances has improved the characterization (using FTIR, SEM and XRD prior to 14C dating) and removal of chemical and physical contaminants from all sample materials (e.g. bone, charcoal and carbonates). Specialized pretreatment techniques, including preparation of very small sized samples, add another dimension in the ever-evolving preparation of samples prior to AMS measurement. In this session we will be focusing on novel developments in the field of radiocarbon pretreatment chemistry, and their application on archaeological, environmental and other samples.

KeywordsPretreatment methodology, sample characterization, physical/chemical contaminantremoval, improved sample isolation

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S03-O-01

UV OXIDATION - A NEW EXTRACTION METHOD FOR RADIOCARBON DATING

STEIER P.(1), faScHInG c.(2), MaIR K.(1), baTTIn T.(2), PRIlleR a.(1)

(1) University of Vienna, faculty of Physics, VIenna, aUSTRIa;(2) University of Vienna, faculty of life Sciences, VIenna, aUSTRIa

AbstractThe requirements of extracting minute amounts of DOC (dissolved organic carbon) with high yield and minimum background are a prerequisite for radiocarbon dating of microgram amounts of carbon. Samples for biomedical or environmental research often arrive at the AMS lab as concentrates dissolved in 1 mL of water or less. We have developed a new extraction method based on oxidation by ultraviolet light.The solution is transferred into UV-transparent quartz vials with a head volume of pure oxygen and UV from a low-pressure mercury discharge lamp is applied. To exclude the introduction of carbon background we avoid any additional oxidizing agents. Under these conditions only the 185 nm line is considered effective for oxidizing organic carbon [Golimovski and Golimowska, 1996]. To characterize the yield and the background we have investigated artificial samples, partly from 13C pure reagents [Liebl et al., 2010]. The setup developed allows parallel oxidation of 9 samples within typically 2 hours, connected directly to our graphitization setup for extremely small samples.The method was applied successfully for a study on DOC in ice from 26 Austrian glaciers. A special advantage of the UV oxidation method in this case was that phosphoric acid could be used to remove carbonates, while it’s low vapor pressure prevented complete lyophilization.

References1. J. Golimowski, K. Golimowska. UV-photooxidation as pretreatment step in inorganic analysis of environmental

samples. Analytica Chimica Acta 325 (1996) 111-133.2. J. Liebl, R. Avalos Ortiz, R. Golser, F. Handle, W. Kutschera, P. Steier, E. M. Wild. Studies on the preparation of

small 14C samples with an RGA and 13C-enriched material. Radiocarbon 52/2-3 (2010) 1394-1404.

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S03-O-02

ULTRAFILTRATION OF BONE COLLAGEN: WHAT DOES IT ACTUALLY DO?

BROCK F., HIGHaM T.

University of oxford, oXfoRD, UnITeD KInGDoM

AbstractThe use of ultrafiltration in the preparation of collagen for radiocarbon dating is now well documented (Brown et al., 1988; Bronk Ramsey et al., 2004; Higham et al., 2006; Brock et al., 2007). Often, dates on ultrafiltered collagen give far more archaeologically coherent results than radiocarbon dates on collagen from the same bone that has not been ultrafiltered. This is especially so for older, Palaeolithic, samples. However, the precise reason or reasons for the improvement in collagen quality when ultrafiltration is used is unclear. It is often assumed that the ultrafilters remove short-chain, degraded and potentially contaminated collagen and other proteins and amino acids, as well as fulvic and other organic acids, the presence of which may result in an erroneous date. However, little published data exists to support this assumption.Here we compare the results of analysis on ultrafiltered and non-ultrafiltered collagen from several bones, including protein analysis using SDS-PAGE gel electrophoresis and liquid chromatography-mass spectrometry (LCMSMS).

References1. Brock, F., Bronk Ramsey, C., Higham, T.F.G. 2007. Quality assurance of ultrafiltered bone dating. Radiocarbon

49: 187-192.2. Bronk Ramsey, C, Higham, T.F.G., Bowles, A. and Hedges, R. 2004. Improvements to the pretreatment of

bone at Oxford. Radiocarbon 46: 155-63.3. Brown, T.A., Nelson, D.E., Vogel, J.S. and Southon, J.R. 1988. Improved collagen extraction by modified

Longin method. Radiocarbon 30: 171-177.4. Higham, T.F.G., Jacobi, R.M. and Bronk Ramsey, C. 2006. AMS radiocarbon dating of ancient bone using

ultrafiltration. Radiocarbon 48:179-195.

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S03-O-03

RADIOCARBON DATING OF CROSS FLOW NANOFILTRATED AMINO ACIDS FROM CONTAMINATED ARCHAEOLOGICAL BONE COLLAGEN, SILK, WOOL AND HAIR

BOUDIN M.(1), Van STRYDoncK M.(1), VanDenabeele P.(2), boecKX P.(2)

(1) Royal institute for cultural heritage, bRUSSel, belGIUM;(2) University Ghent, GHenT, belGIUM

AbstractRadiocarbon dating of bone collagen, wool (hair) and silk contamined with humic substances (HS) doesn’t yield reliable results if these materials were pre-treated with the conventional methods (Boudin et al. 2010, Van Strydonck et al. 2005).Ultrafiltration of bone collagen has received considerable attention as a means to obtain more reliable dates (Brown et al. 1988; Bronk Ramsey et al. 2004; Higham et al. 2006; Mellars 2006). Ultrafiltration is an effective method of removal of low-molecular weight contaminants from bone collagen but it does not remove high-molecular weight contaminants, such as cross-linked humic collagen complexes (Brock et al. 2007). However, comparative dating studies have raised the question whether this cleaning step itself may introduce contamination with carbon from the filters used (Bronk Ramsey et al. 2004; Brock et al. 2007; Hüls et al. 2007; Hüls et al. 2009).Compound-specific 14C dating of individual amino acids (Van Klinken and Cook 1990; Tripp et al. 2006; McCullagh et al. 2010) can be a potential method for dating proteinic material showing HS contamination. However, column bleeding is a common phenomenon in chromatography. Therefore sample blanks should be measured. The drawback of the technique is that it is time consuming.Cross flow nanofiltration is more straightforward and less labour intensive than individual amino acid isolation by HPLC.In this study a cross flow nanofiltration method was developed using a ceramic filter as a means to avoid extraneous carbon contamination via the filter. This method should be applicable on various protein materials e.g. collagen, hair, silk, wool, leather and should be able to remove low-molecular and high molecular weight contaminants, depending on the choice of molecular weight cut off (MWCO) of the filter membrane . Here a filter membrane with a cutoff of 200 Dalton was used in order to collect the amino acids, released by hot acid hydrolysis of the protein material, in the permeate (MW of amino acids varies between 75.07 and 204.23 Dalton) and the contaminants ( > 200 Dalton) in the retentate.Radiocarbon dating was done on the bulk material of archaeological protein material, pre-treated with the conventional methods, and on the crossflow nanofiltrated amino acids (permeate).Quality control of the 14C dated samples was obtained by measuring the C:N ratio

References1. Boudin et al. 2010. Radiocarbon 53(3): 429-442.2. Brock et al.2007. Radiocarbon 49(2):187–92.3. Bronk et al. 2004.Radiocarbon 46(1):155–63.4. Brown et al. 1988.Radiocarbon 30(2):171–7.5. Hüls et al. 2007. Radiocarbon 49(2):193–200.6. Hüls et al. 2009.Radiocarbon 51(2):613–625.7. McCullagh et al. 2010. Radiocarbon 52(2–3):620–34.

8. Mellars. 2006. nature 439(7079):931–59. Tripp et al. 2006. Journal of Separation Science

29:41–8.10. Van Klinken et al. 1990. Radiocarbon 32(2):155–64.11. Van Strydonck et al. 2005. Monografies de la

Societat d’Història Natural de les Balears 12:369–76.

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S03-O-04

COMPARISON OF CLEANING METHODS FOR RADIOCARBON CONTAMINATION IN CHARCOAL

LEVCHENKO V.(1), bIRD M.(2), aScoUGH P.(3), WURSTeR c.(2), lal S.(1)

(1) anSTo, lUcaS HeIGHTS, nSW, aUSTRalIa;(2) James cook University, caIRnS, QUeenSlanD, aUSTRalIa;(3) Scottish Universities environmental Research centre, eaST KIlbRIDe, ScoTlanD, UnITeD KInGDoM

AbstractCharcoal is generally considered ‘inert’, but there is evidence that surface activity occurs rapidly upon environmental exposure. Also, charcoal takes up exogenous carbon that must be removed prior to dating, but samples can be completely destroyed in pretreatment due to their state of degradation. The goal of the study was to compare the performance of several charcoal cleaning protocols, namely ABA (acid-base-acid), ABOX (acid-base-oxidation) and newly developed ‘hypy’ (hydrogen pyrolysis – catalytic removal of non-charcoal carbon at 550 °C under >10MPa H2 gas pressure). Charcoal production, exposure and hypy treatment were carried out at JCU. ABA and ABOX - at the ANSTO, with 14C measurement done at ANSTO on the STAR AMS.The charcoal was made at 350 and 550 C from an 8 million year old log. 14C tests proved that both low and high T charcoals were radiocarbon-dead (14C content of 0.00 ± 0.02 and 0.00 ± 0.01 pMC respectively). Aliquots were left on a tropical rainforest soil surface for one year. The mass gain of ~30% and an increase in 14C to 1.12 pMC was observed for both. The mass gain was more than implied only by 14C, indicating likely use of the charcoal as a substrate for fungal/microbial tissues, with some of the mass derived from the other elements required by biomass.Raw and exposed samples were treated by standard ABA, ABOX and hypy. It was found that the 350 C charcoal cannot survive a complete ABOX treatment dissolving in oxidation step (standard length ~15 hrs at 60°C). A shorter oxidation step of 10 minutes at 60°C was used instead to preserve enough material for AMS. The high temperature charcoal withstood all procedures. Hypy was effective on high T charcoal and reduced the contamination of exposed samples by >90% from 1.12 pMC to 0.08 ± 0.02 pMC. ABA was less effective and brought the value down to 0.15 ± 0.03 pMC only. The most successful was the standard ABOX which returned the exposed sample to 0.00 ± 0.02 pMC - the background value.For the 350°C charcoal, hypy was not effective in reducing contamination, taking it down only to 0.88±0.04 pMC. This was due to the poorly pyrolysed nature of the 350°C sample, meaning that a large fraction of the ‘charcoal’ was also removed by the hypy. This agrees with sample poor durability in ABOX suggesting a large presence on unmodified original organics. Still, the shortened ABOX performed better reducing contamination to 0.07 ± 0.03 pMC. Standard ABA performed likewise with result of 0.08 ± 0.02 pMC.Tests suggest that for charcoal produced at a temperature high enough to convert a substantial share of the organic material to polycyclic aromatic structures (probably >400°C) hypy is a good treatment, but with ABOX still remaining the best. All methods are less able to decontaminate material not exposed to temperatures high enough to form robust aromatic structures in the resultant charcoal. In this situation ABA remains the safest, yet inefficient, option for removing contamination.

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S03-O-05

BIOSILICA OF HIGHER PLANTS: EXCLUSIVE PHOTOSYNTHETIC ORIGIN OF PHYTOLITH CARBON DEBUNKED BY 14C AND δ13C MEASUREMENTS OF EXTRACTED PHYTOLITHS FROM CONTEMPORARY LIVING GRASSES

SANTOS G.M.(1), coRbIneaU R.(2), ReYeRSon P.e.(3), aleXanDRe a.e.(2), SoUTHon J.R.(1), MaRTIneZ De la ToRRe H.(1)

(1) Department of earth System Science, University of california, Irvine, IRVIne, UnITeD STaTeS;(2) ceReGe, cnRS, UPcaM-III, europôle méditerranéen de l’arbois bP 80, aIX en PRoVence ceDeX, fRance;(3) Department of Geography, University of Wisconsin-Madison, MaDISon, UnITeD STaTeS

AbstractPlants acquire, transport, and accumulate silica (Si) from soils. The controlled crystallization of Si at a final location within plant results in biosilica structures known as phytoliths. During phytolith formation, a small amount of carbon (<2%) can become occluded and therefore protected from degradation by the environment. Since photosynthesis is the major mechanism in which green plants acquire C to synthesize their own food, it is assumed that the C trapped in phytoliths (phytC) should reflect the atmospheric CO2 isotopic values at the time the plant was growing. However, this assumption has been recently challenged by 14C data from phytoliths extracted from living grasses that yielded ages of few thousands of years (2 - 8 ka years BP1). Because plants take up small amounts of C of varying ages from soils (e.g. during nutrient acquisition), the “unexpected” 14C values from phytoliths extracted from living grasses lead to the hypothesis that this transported C once within the plant tissue could become attached or even trapped in the biosilica and, therefore bias the phytC 14C results. Moreover, present chemical extraction protocols do not lead to pure phytolith concentrates (i.e. free of attached organic matter residues). In order to assess the purity of the siliceous material, following extraction, phytoliths produced from common extraction protocols were checked by SEM/EDS. The presence of organic tissue aggregates in phytolith concentrates extracted from living plant tissue supports the hypothesis of recalcitrant soil organic matter (SOM) carbon biasing the 14C results. Indeed, any SOM C residues might become adsorbed on porous opal surfaces in vivo or during chemical processing, which could protect them from further chemical oxidation2. As a result of these tests, we developed two phytolith extraction protocols (one using a strong base, and a second one that involves repeated purification steps of dry ashing and acid digestions) that are far more rigorous and lead to 100% pure phytolith siliceous surface concentrates3. Second, to determine the origin of phytC, we measured 14C and δ13C of extracted phytoliths from grasses that were growing within a CO2 enriched versus a non-enriched environment. Photosynthesized plant material grown under elevated concentrations of CO2 should carry distinct δ13C and Δ14C “tags” derived from the excess CO2 relative to plant material growing in normal atmospheric air. Those results will be shown and discussed.

References1. Santos, GM et al. 2010 The Phytolith 14C puzzle: a tale of background determinations and accuracy tests,

Radiocarbon, 52: 113-128.2. Santos, GM et al. 2012 Possible source of ancient carbon in phytolith concentrates from harvested grasses,

Biogeosciences Discuss. 9: 329-356.3. Corbineau, R 2011 Assessment of 14C AMS dating of phytoliths as a new paleoenvironmental and

archaeological tool, B31A-0315 Poster, AGUFall Meeting 2011, San Francisco, USA.

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S03-O-06

PYROLYSIS-COMBUSTION (PY-C) PRETREATMENT FOR 14C DATING OF ORGANIC MATERIALS

WANG H.

Prairie Research Institute, University of Illinois at Urbana-champaign, USa, cHaMPaIGn, UnITeD STaTeS

AbstractSample pretreatments for 14C dating on organic remains, e.g. fossil wood, charcoal, collagen, and soil organic carbon (SOC) are onerous. When close to the dating limit, most methods e.g. acid-base-acid, acid-base-wet oxidation, extraction of humic acid, fulvic acid, and humin from soils, and ultra-filtration for bone collagen show problems on dating accuracy and the successfulness depends upon case specific applications. In an effort to develop a less cumbersome, more reliable, and more widely applicable method for dating organic remains, the Radiocarbon Dating Laboratory of Illinois State Geological Survey, Prairie Research Institute, University of Illinois has introduced a high temperature pyrolysis-combustion (Py-C) technique. The Py-C method heats organic remains under vacuum at high temperature with a flow of inert gas to decompose organic matter and bring all hydrocarbon and weak carbon-carbon bonded molecules to an oxidation chamber for combustion for 14C dating. Highly purified carbon black left in the pyrolysis chamber is separately oxidized or transferred for AMS 14C dating. This method partitions organic remains into pyrolysis volatile (Py-V) or low molecular weight and pyrolysis residue (Py-R) or high molecular weight organic compound fractions to examine their age differences. Because the Py-R fraction is highly purified carbon black resembling the graphitic-like carbon of the organic remains, it should yield more accurate 14C date for old fossil wood, charcoal, and collagen samples. For soil, lacustrine, peat or other sediment dating, either Py-V or Py-R fractions may yield a more reasonable chronology depending on the nature of the mobility of young or old organic carbon in the system. In general, Py-V fractions yield 14C dates much younger than their Py-R fractions. In some cases, the Py-V fractions yielded older dates than the Py-R fractions for human bone collagen due to deep burial, while Py-V and Py-R fractions yielded identical 14C dates for cave sediments due to lack of photosynthesis and continuous input of younger organic carbon. These case studies are presented here for discussion.

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S03-O-07

HIGH PRECISION 14C AMS-ANALYSIS OF TREE RINGS – AN EVALUATION OF SAMPLE PREPARATION AND REPRODUCIBILITY OF AMS MEASUREMENTS

GÜTTLER D.(1), aDolPHI f.(2), bleIcHeR n.(3), fRIeDRIcH M.(4)(5), KRoMeR b.(4), RaIMUnD M.(2), SYnal H.a.(1), WacKeR l.(1)

(1) eTH Zurich, ZURIcH, SWITZeRlanD;(2) Department of Geology, lund University, lUnD, SWeDen;(3) laboratory for Dendrochronology, ZURIcH, SWITZeRlanD;(4) Heidelberg academy of Sciences, HeIDelbeRG, GeRManY;5) Institute of botany, University of Hohenheim, HoHenHeIM, GeRManY

AbstractRadiocarbon dating relies on a calibration curve that connects radiocarbon age and calendar age.The presently used IntCal09 calibration curve lacks a high temporal resolution for samples older than 350 years and contains nearly exclusively tree ring data obtained from laboratories using gas counters and advanced liquid scintillation facilities. At the accelerator mass spectrometry (AMS) laboratory at ETH Zurich we aim to provide new 14C data of higher measurement precision and a higher temporal resolution to improve the Intcal09 calibration curve.Tree rings from the Southern Germany Oak chronology covering the years AD 1010-1300 and rings from the Zurich Oak chronology covering the years AD 1500-1585 have been processed following a base-acid-base-acid cellulose extraction method and graphitized with our automated AGE system. Samples have been analyzed for radiocarbon with the MICADAS AMS-system.Samples of annual and two-year temporal resolution show a modulation of the radiocarbon age most likely caused by the 11-year solar cycle. Such a feature is not visible in the calibration curve so far. The measurements with a precision down to 12 years (<2‰) yielded 14C ages that follow nicely the Intcal09 calibration curve; however, an offset towards older values is observed in comparison to Intcal09.Wood samples of known ages and samples covering a floating period of 100 years have been investigated in the framework of an inter-laboratory comparison. Moreover, these woods have been extensively analyzed in our laboratory to evaluate our 14C measurements and reveal possible sources of errors during sample preparation. Our cellulose extraction method and storage effects of cellulose and graphite targets have been investigated, by varying chemicals, test tubes, and process steps. Results of these tests will be presented and deviations from the Intcal09 calibration curve as well as inter-laboratory offsets will be discussed in this presentation.

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S03-O-08

ASSESSING THE FEASIBILITY OF THE CRYOSONIC (CRYOBRAKING, SONICATION, CENTRIFUGATION) PROCEDURE FOR MORTAR RADIO-CARBON DATING: PRELIMINARY EXPERIMENTAL RESULTS AT CIRCE CENTRE

MARZAIOLI F.(1)(2), nonnI S.(3), lUbRITTo c.(1)(2), PaSSaRIello I.(2)(1), caPano M.(4)(2), TeRRaSI f.(1)(2)

(1) Dipartimento di Scienze ambientali, Seconda Universita degli Studi di napoli, caSeRTa, ITalY;(2) InnoVa, centre for Isotopic Research on cultural and environmental Heritage, caSeRTa, ITalY;(3) Dipartimento di Scienze della Terra, Universita la Sapienza, RoMa, ITalY;(4) Dipartimento di Studio delle componenti culturali del Territorio, Seconda Universita degli Studi di napoli,, caSeRTa, ITalY

AbstractMortar radiocarbon dating represents one of the main “open issues” involving the radiocarbon community because of the discrepancies observed over the almost 4 decades of experimentations. The technology used for the production of mortars, even if modified over time, preserves the potential to establish the absolute chronology of studied artifacts because the setting process is primarily addressable to the atmospheric CO2 adsorption (carbonatation). This potential was firstly guessed by Delibrias e Labeyrie, in 1965, which began a series of experimental tests to assess the feasibility of the methodology but the clues about the effective accuracy of the mortar dating remain still unclear.Among the different sources of contamination, C of geological origins (primary) has been reported as one of the major sources introducing a sensitive ageing effect. 14C ageing of mortars is due to this source of C introduced when different aliquots of primary carbonate survive to the burning of limestone (calcination) and/or when carbonatic sand is used in the mortar production process.Since more than one year the CIRCE (Centre for Isotopic Research on Cultural and Environmental heritage) 14C group began an intense experimental campaign to develop a protocol able to guarantee a reliable mortar dating.CIRCE proposed methodology (CryoSoniC: Cryobraking, Sincation and Centrifugation) is based on a sequence of physical separations.This contribution aims to propose a definitive preparation pathway of preparation to follow in order to achieve the accurate dating of mortars by means of a validation procedure.First step of the CryoSoniC validation procedure was performed on a series of synthetic laboratory mortars produced without the aggregate addition. Observed results showed an efficient binder C selection allowing unbiased dating for mortars produced at functional calcination temperatures. CryoSoniC selectivity was then tested and implemented on: i) mortar lime lumps commonly addressed as the a feasible alternative to bulk mortar dating and naturally bridging synthetic with archaeological mortars; ii) real mortars coming from a series of chronologically constrained archaeological sites with the aim to check also for the influence of different mortar typologies (i.e. pozzolana mortars) on its effectiveness.

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S03-O-09

PROPOSITION OF A METHODOLOGY FOR THE RADIOCARBON DATING OF ANCIENT IRON ALLOYS

LEROY S.(1)(2), DelQUe-KolIc e.(2), DUMoUlIn J.P.(2), MoReaU c.(2), DIllMann P.(1)

(1) IRaMaT lMc cnRS UMR5060 et SIS2M laPa cea/cnRS UMR3299, GIf / YVeTTe ceDeX, fRance;(2) lMc14, cnRS UMS 2572,, GIf / YVeTTe ceDeX, fRance

AbstractThe dating of archaeological iron objects is a major issue to address questions relative to the history, the technology and the ancient societies. If the iron elements can be sometimes dated by presumptions based on archaeological analysis, a precise dating of iron remains today difficult to obtain for the majority offerrous alloys. An absolute method of dating has yet to be applied.At least until the 19th century, the charcoal was mainly used for iron smelting. During the reduction process, some of the carbon of the charcoal diffused into the metal and was incorporated into the structure of the ferrous alloy in ferrite, as cementite (Fe3C).Given that most smeltings were carried out with charcoal usually produced from freshly cut wood, iron artefacts can be dated by extracting the carbon from the iron. Nevertheless, many limitations for reliable dating were evidenced for this particular material due to:(1) the highly heterogenous distribution of carbon within the matrix of iron alloys. The

average immanent carbon content for each artifact is very low for bloomery steel (mostly <0.5%);

(2) contaminations from modern sources during the preparation of the samples;

(3) possible contaminations from older carbon sources, e.g. coke, reworking of older artifacts, lime and carbonate minerals (siderite FeCO3) as iron ore. Very few studies of 14C-ferrous objects were implemented with good archaeometallurgical constraints and educated guesses based on historical information.

We present here the results of a PNRCC[1]research program on radiocarbon dating of iron alloys. In order to obtain reliable 14C dating, we developed a specialized methodology, based on a specific protocol of sampling to facilitate carbon extraction and minimize contaminations in conjunction with detailed metallurgical studies. To test our methodology, we dated artefacts with known archaeological ages ranging from 0 to 1300 AD, with various carbon concentrations (0.1-2%). To discuss of the possible pollution by geological carbon from carbonate ores, we dated iron alloys produced from several experimental smeltings performed by using contemporary charcoal but siderite (FeCO3). Finally, as part of the problem of the iron use in medieval Gothic buildings, radiocarbon datings were carried out on construction iron of the Beauvais and Bourges cathedrals (France), therefore significantly refine our vision of the iron use in these monuments.

[1] Programme National de Recherche sur la connaissance et la conservation des Matériaux du Patrimoine Culturel

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S03-O-10

IMPROVED SEALED GLASS TUBE COMBUSTION FOR SMALL AEROSOL SAMPLES

GENBERG J., PeRRon n., olSSon M., STenSTRÖM K.

Division of nuclear Physics, lUnD, SWeDen

AbstractRadiocarbon has proven to be a valuable tracer for fossil and moderns sources of atmospheric aerosol. However, being an offline method it uses filters which are limited in time resolution. Shorter sampling time render small samples, thus a system handling large numbers of samples with small amount of carbon is required. At Lund University we have since 2009 employed a graphitization line handling samples as small as 25 µg C (Genberg et al, 2010). The aerosol samples are combusted online which has proven reproducible with the small samples. Our goal is however to be able to utilize sealed glass tube combustion for our aerosol samples because it is more time efficient and the risk of contamination is lower compared to online combustion.Such a method is described in Endo et al. (2004) and they found that the normal amounts of CuO, copper metal and silver had to be significantly increased for combusting aerosol filter samples in sealed glass tubes. However, it is not clear whether the method is optimal for small samples. We have therefore tested the method and optimized it for small scale (<100 µg C) combustion.Using the method described turned out to be inadequate for our needs. The first problem arose when transferring the CO2 in the graphitization system. This proved unsuccessful when aerosol filter samples have been combusted. Pure CO2 and CO2 from combusted biological samples can easily be transferred using cold traps. However residue gasses formed during the combustion of the aerosol samples makes this transfer slow at low pressure. In order to transfer the gas as short distance as possible a modified tube cracker was produced.We also found sources of carbon which made it impossible to use the method as described. To use copper metal was proven impossible. Short time exposure to the atmosphere was enough for it to adsorb some carbon which rendered backgrounds too high for our applications. The same was true for copper oxide powder, although Endo et al. (2004) do not specify the type of CuO used. The required amount of newly cleaned CuO powder (800 mg) rendered a background of 12 µg C, which is unacceptable high for our applications. To avoid the powder, newly cleaned CuO rods (1mm*5mm) ware used. This rendered stable blank values at approximately 2 µg C independent of the amount of CuO used between 400 and 1000 mg. 400 mg CuO was sufficient to give the same yield as online combustion.In conclusion, we will present a modified method for combusting small aerosol samples prior to graphitization using sealed tube combustion.

References1. Endo et al. (2004) atmos. environ. 38, 6263-6267.2. Genberg et al. (2010) Radiocarbon 52, 1270-1276.

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S03-O-11

PRESSED GRAPHITE IS MORE SENSITIVE TO CONTAMINATION THAN GRAPHITE POWDER EXTENSIVE TESTS INTO SHORT-TERM STORAGE OF GRAPHITIZED SAMPLES

MEIJER H.A.J., aeRTS-bIJMa a.T., been H.a., Van ZonneVelD D.

centre for Isotope Research, University of Groningen, GRonInGen, neTHeRlanDS

AbstractIn the process of sample preparation, short-term intermediate storage is inevitable, and sometimes even longer storage of samples along the preparation route is caused by sudden instrument failure. Typically, the stages of the sample along the route of preparation in which a laboratory can choose to store are: pure CO2, graphite powder and fully prepared, pressed targets.Storage as pure CO2 is possible for extended times (even up to years), but only if the sample is stored in a glass tube that is sealed by the «flame off» technique. This, however, requires an extra step in the process that is normally not foreseen. Most laboratories therefore have the choice between storing the produced graphite/catalyst mixture («graphite») as powder, or press this into a target and store this target.On first thought storing the pressed graphite is the best choice: the active surface of the material is significantly reduced, such that contamination (from air CO2 or other sources) is supposed to have minimal influence. However, tests that we performed over the years showed this not to be true: the pressed surface clearly takes up contamination from the surroundings, strange enough quite irrespective of what these surroundings are: storage in open air or in an Argon atmosphere did not make a large difference.In our continuous effort to reduce especially the contamination with «modern» carbon (crucial for the measurement of old samples), we decided recently to perform a systematic investigation into the causes of the contamination, both for pressed and unpressed graphite. In all cases, we used pure CO2 that contains no 14C («Rommenhöller gas», Linde) as sample, and we therefore could observe «modern» carbon contamination only.Treatments of both pressed and unpressed graphite were for example: storage in vacuum, storage in dead or in 14C- enriched CO2, in Argon, or simply in open air. Furthermore, we varied the target preparation pressure, and the atmosphere in which the pressing occurred. Finally, we also investigated possible crossovers in the accelerator’s sample wheel chamber.All results were analysed using a fit function of measurement time (and thus of sample sputter depth), with as result surface activity, activity deeper in the target, and penetration depth of surface contamination. With virtually no exception, all targets had higher 14C contamination on their surface than deeper in the target, and this was (far) worse after pressed graphite storage than after unpressed. The relation, however, between surface activity, in-depth activity and treatment is not straightforward. Moisture plays a key role. At the conference, we will present all details, and give a storage recipe.

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S03-O-12

CHEMISTRY OF RAMPED PYROLYSIS RADIOCARBON DATING

ROSENHEIM B., WIllIaMS e., PenDeRGRafT M.

Tulane University, neW oRleanS, UnITeD STaTeS

AbstractRamped pyrolysis is a technique that aims to exploit differences in thermochemical stability of constituents of organic material mixtures such as particulate organic carbon and soil carbon. The technique employs a slowly increasing temperature ramp (normally 5°C/min) that volatilizes organic matter in a flowing He atmosphere. These volatiles are rapidly oxidized to CO2 downstream of the reactor and CO2 is integrated over temperature intervals of interest for radiocarbon and stable isotope determination. The method has proven effective in both improving sediment chronology and in better constraining aspects of the carbon cycle where mixing of organic carbon can be confounding. By nature, though, the method does not preserve chemistry of the organic matter present in the original sample. Here, we investigate the pyrolysis chemistry of the system through three independent methods – analysis of pyrolysis residues by 13C-NMR and compound specific radiocarbon analysis, chemical pre-treatments of samples, and real time 13C/12C ratio analysis of evolved gases. Analysis of pyrolysis residues allows observation of the disappearance of certain constituents and relationship to bulk and ramped pyrolysis radiocarbon ages. Chemical pretreatments such as acid decarbonation that are typically applied to samples in which organic material is an analytical target often change the shape of the pyrolysis reaction. Finally, use of flow-through CRD spectroscopy allows us to key subsampling on isotope changes that signal decomposition of unique constituents of the mixture. The goal of our use of these methods is to better understand the chemistry of pyrolysis in order to improve early first-order Gaussian reaction models of pyrolysis kinetics.

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S03-O-13

HUMIC ACID AND TEMPERATURE STEPPED-COMBUSTION RADIO-CARBON DATES OF TERRACE SEDIMENTS FROM NANFU, TAIWAN

WANG S.L.(1), bURR G.(1), cHen Y.G.(1), lIn Y.(1), WU T.S.(1), McGeeHIn J.(2)

(1) national Taiwan University, TaIPeI, TaIWan;(2) USGS, ReSTon, Va, UnITeD STaTeS

AbstractTaiwan is tectonically driven by the collision between the Luzon Arc and Eurasian continental margin. Fluvial terraces are well developed along most of the rivers in central Taiwan. Obtaining age control of terraces is difficult for a variety of reasons. Optically stimulated luminescence (OSL) dates may be affected by partial bleaching of the luminescence signal due to short transport distances and episodic fluvial sedimentation from the Taiwan Central Mountain Range. This can result in overestimated ages and unreasonably low uplift rates. Traditional radiocarbon dating is limited by sparse organic remains found in fluvial sediments. Bulk sediments can be used for dating in the absence of charcoal, wood or macrofossils. However, organic material in bulk sediments is well known to contain a mixture of organic carbon sources with varying ages.Previous studies have shown that bulk sediment dates can be improved upon by isolating humic acids from the silt- and clay-sized fraction, and through stepped-combustion of humin from the same material. In this study, we isolated different organic fractions from sediments collected at Nanfu terrace, Central Taiwan. These sediment samples were sieved to <63 μm, and then subjected to an acid-alkali-acid (AAA) pretreatment. The humic acid fraction was collected as alkali-soluble material, and humin (insoluble residue) was collected at the end of the pretreatment. Several approaches were then used to collect the different organic fractions:

1) we combusted the humin fraction in two successive steps, at «low temperature» (LT, <400ºC) and «high temperature» (HT, >1100ºC),

2) we performed an incremental stepped-combustion of the humin with 50ºC increments, from 300ºC to 1100ºC; and

3) we combusted the humic acid fraction at HT.

Previous work from sites with independent age control have shown that in sediments, the LT and humic acid radiocarbon dates are generally closer to the expected ages than bulk dates, and that HT radiocarbon ages are typically much older in comparison. At Nanfu, the humic acid dates give an average age of 2600 14C yrs BP. The LT ages average 3050 14C yrs BP, and the average age of the HT fraction is 7200 years. These ages bracket the age of the Nanfu terrace. The height of Nanfu terrace is about 8 meters above the river bed, and this implies a maximum river incision rate is approximately 1.1 mm/yr. Future work on comparing radiocarbon ages from different organic carbon fractions within sediments will assist us in obtaining ages of fluvial-terrace deposits, and help us understand the active and complex tectonics in Taiwan.

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S03-O-14

14C DATING OF HUMIC ACIDS FROM BRONZE AND IRON AGE PLANT REMAINS FROM THE EASTERN MEDITERRANEAN

WILD E.M.(1), STeIeR P.(1), fIScHeR P.(2), HÖflMaYeR f.(3)

(1) Universtity of Vienna, VeRa-laboratory, VIenna, aUSTRIa;(2) University of Gothenburg, cypriote and near eastern archaeology, GoTHenbURG, SWeDen;(3) German archaeological Institute (DaI), orient Department, beRlIn, GeRManY

AbstractThe VERA laboratory participated over several years in the special research program “The Synchronization of Civilizations in the Eastern Mediterranean in the 2nd Millenium BC” - SCIEM2000. In the course of the project numerous plant remains originating from the Bronze and Early Iron Ages were dated. The 14C samples were collected at various archaeological sites in the Eastern Mediterranean and preferentially short-lived material, for instance, seeds were selected for dating. A problem which we encountered in many cases was the complete dissolution of the samples in the alkaline step of the ABA pretreatment. For these samples only a 14C age determination of the humic acid fraction was possible. It is generally assumed that humic acids present in a sample may partly originate from other (younger) organic material, e.g. from soil horizons located above the sample, and therefore could show divergent 14C ages. Thus humic acids from archaeological samples are/should be always assessed as second-choice material and a verification of their dating results is indispensable. To address this question we started some time ago to date both fractions of seeds and charcoal samples whenever available, i.e. the residue after the ABA treatment and the humic acids extracted from the samples in the alkaline step. This strategy was applied especially for sites from which samples tend to dissolve completely during pretreatment.The results of this comparison showed that for the investigated Near Eastern archaeological sites, the majority of the ~50 humic acid dates were in close agreement (within 2 sigma) with the respective dates of the ABA treated samples. This finding leads to the conclusion that the extracted humic acids originated from the samples themself or from contemporaneous material and were not significantly contaminated by extraneous material of different age. Further this agreement implies that the 14C ages of those samples in the archaeological sequences, which could only be dated via the humic acids may be considered reliable.

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S03-O-15

NON-DESTRUCTIVE PRE-SCREENING METHOD FOR ARCHAEOLOGICAL BONE COLLAGEN PRESERVATION USING ION BEAM ANALYSIS (IBA)

BECK L.(1), PIcHon l.(2), VaUbaIllon S.(1), GaUTHIeR c.(3), VallaDaS H.(3), cUIf J.P.(4), cHIoTTI l.(5), neSPoUleT R.(5)

(1) cea, GIf SUR YVeTTe, fRance;(2) c2RMf, PaRIS, fRance;(3) lSce, GIf SUR YVeTTe, fRance;(4) IDeS, oRSaY, fRance;(5) MnHn, PaRIS, fRance

AbstractRadiocarbon dating of bones depends on the preservation of protein material. One way to quantify the preserved collagen is to measure nitrogen and carbon concentrations (Hedges and Van Klinken, 1992, Bocherens et al, 2005, Tisnerat-Laborde et al, 2003). This procedure is conventionally performed by drilling out a small sample of bone (ca. 5 mg) for analysis with an elemental analyser. This technique is reliable, rapid and cheap, but destructive and could be limited by the size of the sample or in case of precious and rare archaeological remains.In this study, we propose to use ion beam analysis (IBA) techniques to estimate the collagen preservation in bone. These techniques allow direct and non-destructive elemental analysis without any sample preparation. Two experimental configurations were tested:1) Nuclear reaction analysis (NRA) which gives access to C, N and O contents (N. Boscher-Barre and P. Trocellier, 1993), using the IBA system of the JANNUS laboratory (Saclay, France).2) Simultaneous combination of PIXE (Particle induced X-ray emission) and RBS (Rutherford backscattering spectrometry) for measuring light (C, N, O) and heavy elements (Na to U) (Beck et al, 2011), with the external beam of the AGLAE accelerator (Paris, France).Elemental composition has been measured by IBA on reference samples of archaeological bones coming from various Palaeolithic sites. The agreement between these results and the CHN analysis demonstrates the reliability of IBA techniques for determining the C and N contents. Collagen preservation was estimated, only by using IBA, on two rare archaeological samples for which sampling was impossible: a decorated scapula (Abri Pataud, France) and a human skull fragment (Orsang river, Gujarat state, India).IBA is proposed as a non-destructive alternative to conventional CHN method for the collagen preservation estimation prior radiocarbon dating in case of valuable samples, such as museum objects or rare archaeological artifacts. It could be easily implemented in laboratories combining radiocarbon dating and IBA analysis.

References1. L. Beck, L. Pichon, B. Moignard, T. Guillou, Ph. Walter, Nucl. Instr. and Meth.B 269 (2011) 2999-30052. N. Boscher-Barre, P. Trocellier, Nucl. Instr. and Meth. B 73 (1993) 413.3. H. Boscherens, D. Drucker, D. Billiou, I. Moussa, L’anthropologie 109 (2005) 557-567.4. R.E.M Hedges, G. J. Van Klinken, Radiocarbon, 34, 3, (1992) 279-915. N. Tisnérat-Laborde, H. Valladas, E. Kaltnecker, M. Arnold, Radiocarbon, 45, 3 (2003) 409–419

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S03-O-16

RADIOCARBON AND STABLE ISOTOPE INTERCOMPARISON OF ULTRAFILTRATION AND XAD-PURIFICATION PRETREATMENT FOR ARCHAEOLOGICAL BONE

CULLETON B.J.(1), SoUTHon J.R.(2), HanSon D.c.(3), STaffoRD T.W.(4), KenneTT D.J.(1)

(1) The Pennsylvania State University, UnIVeRSITY PaRK, UnITeD STaTeS;(2) Keck carbon cycle aMS laboratory, IRVIne, ca, UnITeD STaTeS;(3) Indiana University, blooMInGTon, In, UnITeD STaTeS;(4) Stafford Research laboratories, lafaYeTTe, co, UnITeD STaTeS

AbstractPretreatment of archaeological and paleontological bone for radiocarbon and stable isotope analyses is technically challenging, but few direct comparisons of pretreatment methods have been made. We processed 6 Pleistocene and Holocene bones for AMS 14C dating using modified Longin (1971) extraction with ultrafiltration (Brown et al. 1988) and an amino acid hydrolysis/XAD-purification method adapted from Stafford et al. (1988, 1991). Samples were selected for their problematic geochemistry and previous characterization in bone pretreatment studies. Results will be discussed highlighting comparability and methodological advantages of each approach with respect to details of depositional context and aspects of bone preservation.Additional stable isotope work on a series of 28 Late Holocene pinniped bones compared the δ13C, δ15N, and C:N between gelatin, ultrafiltered gelatin and XAD amino acids. Results indicate no significant difference between unfiltered and ultrafiltered gelatin in these relatively well preserved bones, but XAD amino acids show systematically higher δ13C values (+0.35‰), lower δ15N values (-0.60‰), and lower C:N ratios (-0.10). While the offsets are not large, they may introduce systematic biases in, for example, regional databases of aggregated stable isotope measurements on archaeological bone.Variations in the abundance of C and N in the processed materials also indicate the need for researchers to specify processing methods when reporting and discussing yields as a measure of bone preservation (e.g,, van Klinken 1999). Hydrolyzed amino acids are roughly 20-25% C, whereas as gelatin is roughly 40-45% C. In addition, yields of ultrafiltered gelatin are inevitably lower than unfiltered gelatin. It is important for researchers to report both yield by weight of gelatin/hydrolyzate and by abundance of final C when evaluating organic preservation in archaeological bone samples.

References1. Brown TA, Nelson DE, Vogel JS, Southon JR. 1988. Improved collagen extraction by modified Longin method.

Radiocarbon 30(2):171–7.2. Longin, R. 1971. New method of collagen extraction for radiocarbon dating. nature 230:241-242.3. StaffordTW, Jr, Brendel K, Duhamel R. 1988. Radiocarbon, 13C and 15N analysis of fossil bone: Removal of

humates with XAD-2 resin. Geochimica et cosmochimica acta 52:2257-2267.4. StaffordTW Jr, Hare PE, Currie LA, Jull AJT, Donahue D. 1991. Accelerator radiocarbon dating at the molecular

level. Journal of archaeological Science 18:35-72.5. van Klinken GJ. 1999. Bone collagen quality indicators for palaeodietary and radiocarbon measurements.

Journal of archaeological Science 26:687–695.

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S03-O-17

DATING GODS: RADIOCARBON DATES FROM THE SANCTUARY OF ZEUS ON MOUNT LYKAION (ARCADIA, GREECE)

STARKOVICH B.(1), HoDGInS G.(2)(1), VoYaTSIS M.(1), GIlMan RoMano D.(1)

(1) School of anthropology, University of arizona, TUcSon, aRIZona, UnITeD STaTeS;(2) nSf-arizona aMS laboratory, University of arizona, TUcSon, aRIZona, UnITeD STaTeS

AbstractGenerally radiocarbon dating bone is difficult in the absence of well-preserved organic collagen. However, in recent years it has become apparent that radiocarbon dating structural carbonate is possible if bones are burned to the point of being calcined. Several calcined bone dating protocols introduced by Van Strydonck, Olsen, De Mulder, and others have yielded reliable results based upon comparisons with radiocarbon dates from other artifact classes (pitch, wood, charcoal, etc.) found in contemporaneous contexts. In this study, a dating protocol developed from the work of these authors has been applied to a stratigraphic sequence of calcined bones. The faunal remains from the Sanctuary of Zeus on Mount Lykaion, in southern Greece, provide an unusual test case for the calcined bone dating method. The depositional context is a mountaintop ash altar, with a meter and a half of anthropogenic sediments rich in calcined bone, ash, ceramics, and botanical remains. These items were burned as part of sacrificial offerings to the god Zeus. Diagnostic ceramics indicate that the altar was used from the Final Neolithic through the Classical periods (about 5,500 to 2,000 years ago). This paper presents a series of 70 radiocarbon dates taken from a 25 x 25 cm sediment column in the deepest part of the altar. The column was excavated in 5 cm cuts, and charcoal, seeds, and calcined bones were collected from each layer. The paired samples were dated in order to assess:

1) the validity of the calcined bone dating method in this particular context,

2) the stratigraphic integrity and post-depositional movement of small artifacts in the altar deposits,

3) the span of time during which the altar was in use.

The application of the method in this context is particularly valuable, as the Sanctuary of Zeus on Mount Lykaion is one of few Greek sacrificial altars to be excavated using modern techniques, and it spans a considerable time depth as compared to other sites.

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SESSION 4

SPECIFIC COMPOUNDS: TOWARDS NEW APPLICATIONS

ConvenersYS Huang (USA), G. mollenhauer (DEU), S. Szidat (CHE)

DescriptionSince its first introduction in 1996, the technique of compound-specific radiocarbon analysis (CSRA) has been applied by a growing number of researchers to a diverse field of topics, including questions regarding carbon cycling in the natural environment and in a changing climate, anthropogenic pollution of the environment, and carbon source apportionment. With the growing number of applications, more and more different compounds and compound-classes are targeted. We invite contributions discussing both the technical challenges associated with preparation of CSRA samples as well as the applications of the technique to all of the above mentioned fields of research.

KeywordsCSRA, sample preparation, carbon cycling, source apportionment

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69

S04-O-01

DATA REDUCTION OF SMALL RADIOCARBON SAMPLES

WACKER L., cHRISTl M., SYnal H.a.


AbstractChemical purification methods such as gas chromatography (GC) or high-pressure liquid chromatography (HPLC) allow radiocarbon analyses on specific organic compounds. However, only small amounts of these substances (i.e. low µg level) can be isolated with commercially available GC and HPLC instruments in a single run. Thus, even very small contaminations will bias any radiocarbon determination of the isolated compound.The propagated uncertainties of the radiocarbon analyses are mostly not the limiting factor anymore.The measured radiocarbon concentration is always a superposition of the radiocarbon concentration of both the sample and the contaminant. The radiocarbon concentration can be extracted applying the model of constant contamination, if the total carbon content and the contaminant mass and radiocarbon concentration of the contaminant are known. We will present possible strategies to access the mass and radiocarbon concentration of the contaminant with their corresponding uncertainties and discuss how they influence the measurements of samples. Methods will be given to derive the “true” radiocarbon concentration of the sample compound from the measured radiocarbon concentration.

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S04-O-02

COMPOUND SPECIFIC RADIOCARBON DATING OF ESSENTIAL AND NON-ESSENTIAL AMINO ACIDS: TOWARDS DETERMINATION OF DIETARY RESERVOIR EFFECTS IN HUMANS

CHAVAN S., MccUllaGH J., HeDGeS R., HIGHaM T.


AbstractWhen multiple carbon reservoirs are present in the diet of humans, inaccuracies in the radiocarbon date of bone collagen can occur. In the Iron Gates of the Danube River in Eastern Europe, human skeletons have shown a reservoir offset of up to ~500 years. This has been demonstrated through direct dating of the human bones and the remains of ungulate bone spear points that were found embedded in them (Cook et al., 2001). This example illustrates how reservoir effects can be responsible for significant errors in estimating the true age of human bone in a wide range of contexts.Here we will present a novel HPLC method for the detection and separation of underivatised amino acids using a water only mobile phase without any type of organic or inorganic modifier, ensuring the lowest carbon backgrounds possible. In addition, the method facilitates separation of less-polar, essential amino acids that are strongly retained using prior methods. We discuss the method development, work on characterization of carbon backgrounds and analytical approaches to minimize their effects. We validate the precision and accuracy of the method by AMS dating relatively modern and radiocarbon dead, known age, bone standards.Finally, we demonstrate application of this method in quantifying reservoir effects from bone collagen known to exhibit a strong reservoir effects including samples from Paleolithic burials at the Iron gates site. We investigate whether differences can be found in AMS dates for essential and non-essential amino acids corresponding to the age offset observed for bulk dates.

ReferencesCook, G.T., Bonsall, C., Hedges, R.E.M., McSweeney, K., Boronean, V. and Pettitt, P.B. (2001) A Freshwater Derived 14C Reservoir Effect at the Stone Age Sites in the Iron Gates Gorge. Radiocarbon 43(2A): 453-460.

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S04-O-03

COMPOUND-SPECIFIC RADIOCARBON ANALYSIS OF DIATOM FRUSTULE BIOMARKERS IN OPAL-RICH MARINE SEDIMENTS

BRIDOUX M.(1), GUIlDeRSon T.(2), anDeRSon R.(3), cRoSTa X.(4), InGallS a.(1)

(1) University of Washington, School of oceanography, SeaTTle, UnITeD STaTeS;(2) center for accelerator Mass Spectrometry, lawrence livermore national laboratory, lIVeRMoRe, UnITeD STaTeS;(3) lamont-Doherty earth observatory and Department of earth and environmental Sciences, columbia University,

PalISaDeS, nY, UnITeD STaTeS;(4) UMR 5805 ePoc, Talence, fRance

AbstractBiogenic carbonate based radiocarbon stratigraphy is an essential tool in paleoceanography and paleoclimatology. However, in regions where production of carbonate is low and/or preservation is poor, such as in the Southern Ocean (SO), the application of 14C dating is limited. In contrast, silicified diatom cell walls (frustules) can comprise up to 90% by weight of SO sediments (Demaster, 1981) and recent studies show that template molecules biosynthesized and incorporated into the frustule during its formation are abundant and physically protected from degradation on geological timescales (Ingalls et al., 2004; Bridoux et al., 2010; 2011). Here, we report the ages of organic compounds released during HF dissolution of pre-cleaned sediments (mycosporine like-amino acids, aliphatic long chain polyamines and uncharacterized chromophores) in opal-rich sediments retrieved from the Atlantic (TNO57-13) and Indian (ELT27-23) sectors of the Southern Ocean as well as near the Adelie Land (MDO3-2601). Radiocarbon dating of HF soluble frustule biomarkers isolated from a SO plankton tow revealed their ages to be consistent with that of the modern dissolved inorganic carbon (DIC) reservoir age (pre-bomb, Δ14C~ -150‰) in this region. In the sediment cores, the 14C ages of these diatom frustule biomarkers gradually increased with depth in the core. Radiocarbon ages were compared to those of foraminifera, humic acids and total organic carbon from the same samples. Overall, there was a good agreement between the foraminifera and compound-specific dates in the three SO sediment cores; although the ages of diatom biomarkers were at times older than those of foraminifera. Possible reasons for the disagreement between the ages of foraminifera and diatom-bound compounds will be discussed in the context of sediment dynamics and reservoir ages. This study highlights the promising potential of diatom frustule-bound organic compounds in paleo-applications in regions where a lack of carbonates hinders progress in the development of late Quaternary paleoceanographic records.

References1. DeMaster D. J. (1981) The supply and accumulation of silica in the marine environment. Geochim. Cosmochim.

Acta 45, 1715-1732.2. Ingalls A.E., Anderson R.F., Pearson A., 2004. Compound-specific radiocarbon dating of diatom-bound

organic compounds. Marine chemistry. 92, 91-105.3. Bridoux, M.C., Ingalls, A.E. 2010. Structural identification of long chain polyamines associated with biosilica

from Antarctic diatomaceous ooze. Geochimica et cosmochimica acta 74, 4044-40574. Bridoux, M.C., Annenkov, V., Menzel, H., Keil, R., Ingalls, A.E. 2011. A new liquid chromatography/electrospray

ionization mass spectrometry method for the analysis of underivatized aliphatic long chain polyamines. Rapid communications in Mass Spectrometry 25, 877-888.

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S04-O-04

CONTRASTING RADIOCARBON AGE OF LIGNIN PHENOLS IN THE DISSOLVED AND PARTICULATE MATTER IN MAJOR RIVER SYSTEMS

fenG X.(1)(2), VonK J.e.(1), bao H.(3), GalY V.(2), VoSS b.(2), Mann P.(4), WU Y.(3), PeUcKeR-eHRenbRInK b.(2), RePeTa D.J.(2), HolMeS R.M.(4), MonTlUcon D.(1)(2), eGlInTon T.I.(1)(2)

(1) eTH Zurich, ZURIcH, SWITZeRlanD;(2) Woods Hole oceanographic Institution, WooDS Hole, Ma, UnITeD STaTeS;(3) State Key laboratory of estuarine and coastal Research, east china normal University, SHanGHaI, cHIna;(4) Woods Hole Research center, WooDS Hole, Ma, UnITeD STaTeS

AbstractAs an important and ubiquitous component of vascular plants, lignin is widely dispersed as both dissolved and particulate organic carbon in river systems. While the distribution and composition of lignin-derived phenols in dissolved and particulate phases have been extensively investigated and compared, little is known about their radiocarbon ages, which carry information on their residence time within drainage basins and the relationships between lignin components carried in either phase. These characteristics may differ depending on transport processes and organic matter sources. Here we employed a recently modified high pressure liquid chromatography method of isolating individual lignin phenols and assessed its efficiency and accuracy for radiocarbon dating dissolved lignin phenols from standard phenol solutions and plant leaf leachates. We then extracted dissolved lignin phenols from 60-500 L of river water and employed compound-specific radiocarbon analysis to compare the provenance and transport of lignin in the dissolved and particulate phases from six major river systems (Mackenzie, Kolyma, Fraser, Yangtze, Ganges-Brahmaputra, and Congo). The radiocarbon age of lignin phenols in fluvial particles ranged from modern in tropical/subtropical rivers (Congo and Ganges-Brahmaputra) to approximately 4000 years in the Arctic (Kolyma and Mackenzie). The latter, while clearly reflecting protracted storage of lignin within Arctic river drainage basins, is markedly younger than higher plant wax lipids isolated from the same sediments. This observation indicates that lignin in the particulate phase is a relatively rapidly cycling component of the terrestrial organic matter transported by rivers. In sharp contrast, dissolved lignin phenols exhibited significantly older ages than particulate lignin in the same river system, spanning from ~4000 to 10,000 years in the Fraser, Ganges-Brahmaputra, and Congo rivers. This observation suggests substantial pre-aging of dissolved lignin in the environment (presumably soils) before its delivery into rivers and/or contrasting sources of particulate and dissolved organic matter during land-ocean transfer. Overall, the radiocarbon age of dissolved lignin versus particle-associated lignin provides novel insights on the processing and fate of lignin during fluvial transport and on the parameters controlling the stabilization of terrestrial organic matter in river systems.

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SESSION 5

STATISTICAL TOOLS

Convenersm. Blaauw (GBR), A. millard (GBR), m. Scott (GBR)

DescriptionStatistical tools are increasingly used to synthesize elements of radiocarbon science with other scientific information, for example:- chronological models incorporating stratigraphic and depositional processes- spatial modelling of radiocarbon measurements- statistical analysis for quality control- representations of laboratory processes- uses of calibration curve data for purposes other than calibration, e.g. palaeoclimate or forensic studies

This session will bring together this broad field of applications, to encourage discussion and cross-fertilisation.

Keywordsmodels, statistics, calibration, synthesis

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S05-O-01

RECENT AND PLANNED DEVELOPMENTS OF THE PROGRAM OXCAL

BRONK RAMSEY C., lee S.


AbstractOxCal is a widely used software package for the calibration of radiocarbon dates and the statistical analysis of radiocarbon and other chronological information. The program aims to make statistical methods easily available to researchers and students working in a range of different disciplines. This paper will look at the recent and planned developments of the package.The recent additions to the statistical methods are primarily aimed at providing more robust models, in particular through model averaging for deposition models and through different multi-phase models. The paper will look at how these new models have been implemented and explore the implications for researchers who might benefit from their use. In addition a new approach to the evaluation of marine reservoirs will be presented.As the quantity and complexity of chronological data increases it is also important to have efficient methods for the visualisation of extensive data-sets and methods for the presentation of spatial and geographical data embedded within planned future versions of OxCal will also be discussed.

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S05-O-02

BACON AND CLAM: NOUVELLE CUISINE AGE-DEPTH MODELLING

BLAAUW M.(1), cHRISTen J.a.(2)

(1) Queen’s University belfast, belfaST, UnITeD KInGDoM;(2) centro de Investigacion en Matematicas, GUanaJUaTo, MeXIco

AbstractTwo recent developments in age-depth modelling of cores dated by radiocarbon and/or other dates will be discussed.The first one, clam (Blaauw 2010), aims to provide a more transparent, consistent and reproducible approach to producing basic age-depth models based on “classical” approaches. Age-depth curves are drawn through calibrated radiocarbon or other dates based on importance sampling. The impacts of user decisions such as rejecting “outlying” dates, choice of age-depth model (e.g., linear interpolation, polynomial regression or smooth spline), extrapolation, excising sections of abrupt accumulation (slumps), or hiatuses, can easily and rapidly be visualised.The second approach, Bacon (Blaauw and Christen 2011), uses a Bayesian framework to simulate the accumulation of deposits/sediments while taking into account assumptions, or prior information, on accumulation rate and its variability. The autoregressive semiparametric age-depth models are flexible, deal efficiently with outlying dates, and prove robust for a large range of tested sites. Different prior settings have a clear impact on the resulting age-depth models, and we will discuss that this should actually be the case, both for high-resolution and low-resolution dated fossil proxy cores.Both approaches have been tested on hundreds of cores and are open-source, cross-platform and implemented within a popular, free statistics environment called R.

References1. Blaauw, M., 2010. Methods and code for ‘classical’ age-modelling of radiocarbon sequences. Quaternary

Geochronology 5: 512-5182. Blaauw, M., Christen, J.A., 2011. Flexible paleoclimate age-depth models using an autoregressive gamma

process. bayesian analysis 6: 457-474

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S05-O-03

qUANTIFYING FRESHWATER RESERVOIR EFFECTS AT THE BRONZE AGE NECROPOLIS OF OLMO DI NOGARA, ITALY: A BAYESIAN MODELLING APPROACH

MEADOWS J.(1)(2), ValZolGHeR e.(3), SalZanI l.(4), De MaRInIS R.c.(5)(6)

(1) Zentrum für baltische und Skandinavische archäologie, Stiftung Schleswig-Holsteinische landesmuseen, Schloss Gottorf, ScHleSWIG, GeRManY;

(2) leibniz-labor für altersbestimmung und Isotopenforschung, christian-albrechts-Universität zu Kiel, KIel, GeRManY; (3) Ricerche archeologiche snc/archäologische Untersuchungen oHG, bReSSanone/bRIXen, ITalY;(4) Soprintendenza per i beni archeologici per il Veneto - nucleo operativo di Verona, VeRona, ITalY;(5) Dipartimento di Scienze dell’antichità, Università degli Studi di Milano, MIlan, ITalY;(6) Istituto Italiano di Preistoria e Protostoria, floRence, ITalY

AbstractOlmo di Nogara, near Verona, is one of the largest Bronze Age burial ground in Italy (~500 inhumations, many with grave goods, and ~60 cremations). Bones from 11 inhumations (10 with bronze grave goods) were dated at CEDAD, Lecce, in 2011, and in all cases the results are earlier than expected on the basis of grave-good typology. Fourteen more samples were then dated at Kiel, to validate the initial results and to confirm that they reflect freshwater dietary reservoir effects, rather than a misunderstanding of the chronology of the grave goods.The second series of samples was chosen using a Bayesian simulation model, based on the CEDAD results, stratigraphic relationships between burials, typological attributions of grave goods and the expected dates of potential samples that should not be subject to reservoir effects (cremations, charcoal and herbivore bone). Bayesian modelling of the combined radiocarbon results allows us to estimate the calendar dates of death of 17 individuals, and thus to quantify apparent radiocarbon age offsets in these cases.In parallel, stable isotope measurements are being undertaken on both the dated human bones and contemporary local herbivore bones, to investigate the relationship between diet and radiocarbon age offsets. Previous stable isotope research, on different individuals (Tafuri et al. 2009), attributed δ13C enrichment at Olmo di Nogara to millet consumption, by humans and domestic herbivores. Although millet consumption probably masks the δ13C signature of fish consumption to some degree, we expect δ15N and/or δ34S in human bone collagen to be correlated with the radiocarbon age offsets, confirming that these offsets are due to dietary reservoir effects.

ReferencesMary Anne Tafuri, Oliver E. Craig, and Alessandro Canci (2009) Stable isotope evidence for the consumption of millet and other plants in Bronze Age Italy, american Journal of Physical anthropology, 139: 146-153

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S05-O-04

qUANTITATIVE APPROACH TO ANCIENT DIET RECONSTRUCTION AND RESERVOIR EFFECT CORRECTION

FERNANDES R.(1)(2), MeIJlInK b.(3), neHlIcH o.(4), MIllaRD a.R.(5), bRabec M.(6), naDeaU M.J.(1), GRooTeS P.M.(1)

(1) leibniz-laboratory for Radiometric Dating and Isotope Research, KIel, GeRManY;(2) Graduate School Human Development in landscapes, KIel, GeRManY;(3) Walcherse archeologische Dienst, MIDDelbURG, neTHeRlanDS;(4) Department of Human evolution, Max-Planck Institute for evolutionary anthropology, leIPZIG, GeRManY;(5) Department of archaeology, Durham University, DURHaM, UnITeD KInGDoM;(6) Institute of computer Science, academy of Sciences of the czech Republic, PRaGUe, cZecH RePUblIc

AbstractStable isotope analysis is one of the main analytical tools used within archaeological research for ancient human diet reconstruction. However, several issues need to be addressed so that a truly quantitative diet reconstruction becomes possible. A three step approach is hereby proposed:1) Characterization of the isotopic baseline, i.e., identifying possible food sources and characterizing corresponding isotopic signals.

2) Use of multiple isotopic signals for which dietary routing mechanisms have been well established. This implies knowledge of the dietary routing of food macronutrients (carbohydrates, lipids, and proteins) and biochemical components (e.g. amino acids).

3) Use of statistical models that allow integration of all sources of data variability (including uncertainty in isotopic enrichment and isotopic variability in the food source).

An illustrative example of a quantitative approach to ancient diet reconstruction is hereby presented. Individual human remains, in an excellent state of preservation, were collected from the medieval cemetery of Oude Markt in Vlissingen (The Netherlands). Stratigraphically associated fish and animal material located in an ancient cesspit permitted a characterisation of the isotopic baseline. Archaeological data was complemented with historical information on dietary habits of medieval Dutch coastal populations. Compiled information was used to define food groups (e.g. cereals, land animals, freshwater fish, and marine fish). Estimates of food nutrient composition and isotopic variability relied on previously published data.A Bayesian mixing model was designed to take into account the dietary contribution of different food nutrients and components to the organic and inorganic carbon in bones. For each measured isotopic signal (δ13C and δ15N in bone collagen, δ34S in collagen’s methionine, and δ13C in bioapatite) weight contributions of the different food nutrients and/or components were determined from an analysis of compiled results of controlled animal feeding experiments (e.g. Warinner and Tuross 2009, Froehle et al. 2010).Model output provided, for each individual, probability distributions and confidence intervals on the consumption of each food group. These results were used to provide an estimate of each individual’s reservoir effect. The reliability of such an estimate was assessed by comparison with age offsets observed between collagen radiocarbon dates and the dating (dendro and radiocarbon) of wooden caskets in which the individuals were buried.

References1. Warinner, C., and Tuross, N., 2009, Alkaline cooking and stable isotope tissue-diet spacing in swine:

archaeological implications, Journal of archaeological Science 36(8), 1690-1697.2. Froehle, A.W., Kellner, C.M., and Schoeninger, M.J., 2010, FOCUS: effect of diet and protein source on

carbon stable isotope ratios in collagen: follow up to Warinner and Tuross (2009), Journal of archaeological Science 37(10), 2662-2670.

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S05-O-05

MODELLING CHARCOAL DATES FOR HIGH-PRECISION CHRONOLOGIES

DEE M., bRonK RaMSeY c.


AbstractCharcoal is one of the most common materials selected for radiocarbon dating. Its inertness and durability mean it is often the only organic material available in some archaeological and environmental deposits. Furthermore, in contexts such as destruction layers or hearths, charcoal may provide the only directly datable evidence for anthropogenic activity. However, charcoal samples are often considered unsuitable for chronological studies where the levels of precision and accuracy required are close to the limits of the radiocarbon method. The most significant problem is usually the magnitude of the inbuilt age associated with each sample. Indeed, in most undisturbed contexts, charcoal dates are just treated as termini post quos. Designating the results in this way, however, diminishes their use for high-precision modelling and renders the enormous resource of published charcoal dates essentially redundant. Here we propose and test methods for tackling the problem of inbuilt age in charcoal samples. Firstly, best practices for sampling charcoal are discussed and then different approaches to modelling charcoal dates are evaluated. Examples are drawn from ancient Egyptian contexts, where the true ages of events are well established on historical grounds. Simulated results provide additional insight into the suitability of dates for high-precision work, based on the patterning within a given data set. The overall goal of this study is to circumscribe the employment of charcoal data for high-precision chronological modelling.

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S05-O-06

WORKING TOWARDS AN IMPROVED UNDERSTANDING OF DEEP-SEA SEDIMENT CHRONOLOGIES USING POST-DEPOSITIONAL REMANENCE MAGNETIZATION (PDRM) MODELING

STRANO S., SToneR J., MaRcoTT S.

oregon State University, college of earth, oceanic and atmospheric Science, coRVallIS, UnITeD STaTeS

AbstractFor years, the paleo community has used both relative and absolute dating (e.g. paleomagnetic stratigraphy and radiocarbon dating) in an attempt to understand past environmental events and processes. This study specifically addresses the need to account for and reconcile paleomagnetic age offsets that result from post-depositional remanence magnetization (pDRM) and how this might address radiocarbon uncertainties in the future. Here we use seven high-resolution (~10-65 cm/kyr) deep-sea sediment cores taken from the western (KN158-04-2GC, KN158-04-22GC and IODP Site U1305) and eastern North Atlantic (KN158-04-53GC, KN158-04-46GC, KN158-04-57GC and ODP Site 984). All output records contain robust independent chronologies based on a large quantity of radiocarbon dates on planktic foraminifera with a constant 400-year reservoir correction. Accurately dated geomagnetic inputs are derived from multiple archeomagnetic and ultra-high resolution regional paleomagnetic secular variation records where pDRM in terms of minimal delta-T.To account for chronologic errors associated with radiocarbon age uncertainty, we applied a Monte Carlo based approach that perturbed each of the records’ age models 10,000 times following a random draw from a normal distribution (Marcott et al., in prep). The uncertainty between the age control points was modeled as a random walk, after Huybers and Wunch (2004), and chronologic uncertainty was assumed to be autocorrelated through time and modeled as a first order autoregressive process.By eliminating radiocarbon error as the reason for apparent age differences, this analysis allows us to show that paleomagnetic features in deep-sea sediment cores are «locked-in» at some depth due to a pDRM process, and therefore, appear artificially older than the same features in absolutely dated records. Through modeling the pDRM processes we can begin to account for temporal offsets within paleomagnetic correlations. These show that changes in sedimentation rate and lithology influence pDRM. Here we quantify these changes and use them to correctly date the age of the magnetic features that will allow us to assess uncertainties in other dating methods including, variable reservoir ages and radiocarbon production rates.

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SESSION 6

VARIATIONS IN RADIOCARBON RESERVOIR EFFECTS

ConvenersW. Beck (USA), Q. Hua (AUS), G. Quarta (ITA), G. Siani (FRA)

DescriptionContributions are welcome on the investigation of radiocarbon reservoir effects and their temporal variations over the past 50 ka for various materials including marine and coastal (estuarine, lagoonal) samples, speleothems, terrestrial shells, lake sediments, and freshwater plants and shells. This investigation is not only important for improving the radiocarbon dating method but also gives useful information on climatic and environmental changes and the carbon cycle (ie, ocean circulation changes associated with climate change, and soil-to-speleothem carbon transfer dynamics through the cave system). Modelling studies of temporal variations in the reservoir effects associated with changes in climatic and/or environmental factors (ie, trace elements and stable isotopes) are also encouraged.

KeywordsRadiocarbon reservoir effect, speleothem dead carbon fraction, marine reservoir ages, hard-water effect, climatic and environmental changes.

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S06-O-01

LATE-GLACIAL AND EARLY HOLOCENE MARINE 14C RESERVOIR AGES OFF NORTH ICELAND (16-9 CAL KYR BP)

OLSEN J.(1)(2), KnUDSen K.l.(1), eIRÍKSSon J.(3), ReIMeR P.J.(2)

(1) aarhus University, aaRHUS, DenMaRK;(2) Queen’s University belfast, belfaST, UnITeD KInGDoM;(3) University of Iceland, ReYKJaVIK, IcelanD

AbstractTephrochronological age models and 48 14C age determinations on molluscs and foraminifera (planktonic and benthic) are applied for the calculation of marine 14C reservoir age variability during a time period covering the Heinrich event H1 to early Holocene (16–9 cal kyr BP). Our data source consists of four high-resolution marine sediment cores (HM107-04, HM107-05, MD99-2271, MD99-2275) from the North Icelandic shelf. The marine reservoir age (ΔR) is found to be extremely variable, ranging from 385 to 1065 14C years. Extreme ΔR values occur at the end of H1, with values around 1000 14C years (~15 cal kyr BP), probably due to reduced northward flow of well-ventilated subtropical surface waters and a southward expansion of polar waters, as well as an expansion of sea ice limiting air-sea gas exchange. With the onset of the Bølling-Allerød interstadial, the ΔR values decrease towards 0 14C years suggesting a more vigorous North Atlantic Current and an active meridional overturning circulation system. During the Younger Dryas stadial, ΔR values are consistently around 700 14C years suggesting a renewed expansion of polar waters and a weakened meridional overtuning circulation. Interestingly, ΔR values remain high (~200 14C years) at the onset of the Holocene suggesting continued high influence of polar waters. Subsequently, ΔR values rapidly decrease to ~- 250 14C years around 11 cal kyr BP, indicating increased air-sea CO2 exchange with the coeval atmosphere. The ΔR values average around 0 14C years from around 10.5 to 9.0 cal kyr BP.

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S06-O-02

MARINE RADIOCARBON RESERVOIR EFFECT IN SOUTHERN IBERIAN ATLANTIC COAST

MATOS MARTINS J.M.(1)(2), MonGe SoaReS a.M.(1)

(1) Instituto Tecnológico e nuclear, SacaVÉM, PoRTUGal;(2) Universidade do algarve, cIMa, faculdade de ciências e Tecnologia, faRo, PoRTUGal

AbstractThe quantification of the marine radiocarbon reservoir effect (ΔR) is essential not only to calibrate conventional radiocarbon dates from marine shell samples but also to get information concerning the spatial and temporal variability of coastal upwelling in marine regions influenced by this phenomenon.Previous research concerning the southern Iberian Atlantic coast, i.e. the northern region of Gulf of Cadiz, has shown the existence of different oceanographic conditions (Fiúza, 1983) with the corresponding ΔR values (Soares and Dias, 2006): the western part of the southern Portuguese coast is influenced by the Northeastern Atlantic circulation (positive ΔR values) and the southwestern Andalusian coast, due to its configuration, does not present any wind-driven coastal upwelling (negative ΔR values). Nevertheless, regarding the oceano-graphic conditions, the southern Portuguese coast can be divided into two zones: Barlavento (Winward), from Cape S. Vicente to Cape Santa Maria, where the coastal waters are influenced by the prolongation to the east of the western coastal upwelling system, and Sotavento (Leeward), from Cape Santa Maria to the mouth of the Guadiana river, where a minor upwelling area occurs to the east of Cape Santa Maria when the prevailing winds in the Gulf of Cadiz are from west. So, concerning the coastal upwelling regime, the Sotavento can be considered as a transition zone between the Barlavento and the Andalusian coast. This work focuses on the southern Portuguese coast. For the first time ΔR values were determined for the Sotavento coastal region and also new ΔR values were added to the data already known for the Barlavento coastal region.Taking into account the last 3000 yr weighted mean values for ΔR can be calculated for the three coastal regions of the northern area of Gulf of Cadiz: Barlavento ΔR = + 65 ± 20 14C yr, Sotavento ΔR = - 65 ± 30 14C yr, and Andalusian coast ΔR = -135 ± 20 14C yr. These values are in accordance with the oceanographic conditions present in Gulf of Cadiz, and must be used in association with the marine calibration curve (MARINE09) in order to get accurate and reliable calendar dates from calibration of conventional radiocarbon dates obtained with marine shell samples collected in these regions.

AcknowledgementsThis work was partially supported by FCT research project PTDC/MAR/68932/2006. J.Martins acknowledges the PhD grant SFRH/BD/45528/2008 from the same institution.

References1. Fiúza, AFG 1983. Upwelling Patterns off Portugal. In: Suess E, Thiede J (eds.). Coastal Upwelling. Its Sediment

Record. Plenum: New York, 85-98.2. Soares AMM, Dias JMA 2006. Coastal Upwelling and Radiocarbon – Evidence for Temporal Fluctuations in

Ocean Reservoir Effect off Portugal during the Holocene. Radiocarbon 48(1):45–60.

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S06-O-03

IMPACT OF SURFACE RESERVOIR 14C CHANGES ON DEGLACIATION TIMING AND DEEP WATER VENTILATION IN THE SOUTH-EASTERN PACIFIC

SIANI G.(1), MIcHel e.(2), De-Pol HolZ R.(3), laMY f.(4), caRel M.(1), PaTeRne M.(2)

(1) laboratoire des Interactions et Dynamique des environnements de Surface (IDeS), UMR 8148, cnRS-Université de Paris-Sud, bât. 504, 91405 orsay cedex, france, oRSaY, fRance;

(2) laboratoire des Sciences du climat et de l’environnement (lSce), laboratoire mixte cnRS-cea, GIf-SUR-YVeTTe, fRance;(3) Department of oceanography, University of concepcion, chile, concePTIon, cHIle;(4) alfred Wegener Institut fur Polar- und Meeresforschung, am alten Hafen 26, 27568 bremerhaven, bReMeRHaVen,

GeRManY

AbstractAccuracy of timing of millennian-scale climatic events recorded in marine and continental archives are crucial for a better understanding of the mechanisms, temporal frequency and the geographical repercussion that govern ocean-climate interactions. A robust benchmark to solve this issue bears on the knowledge of present and past quantitative estimates of marine radiocarbon reservoir ages (sea surface - atmosphere 14C differences) that still remain poorly constrained. Alongside, accurate estimates of the past sea surface reservoir 14C age changes are essential for reconstructing ocean 14C ventilation history of the ocean. However, deep-sea 14C variability reconstructions based on paired benthic and planktonic 14C ages often miss a precise sea surface reservoir age estimate.Here we present independent estimates of surface and deep-water reservoir ages by radiocarbon (14C) dates of contemporaneous planktonic and benthic foraminifera and volcanic tephra, contemporaneously deposited over the South-Eastern Pacific marine and terrestrial regions in Northern Patagonia. For this study, we have selected a long CALYPSO high sedimentation piston core MD07-3088 collected off the south Chilean margin between the northern Chonos archipelago and southern Taitao peninsula at about 46°S during the IMAGES R/V Marion Dufresne cruise Pachiderme (February 2007).Results reveal that sea surface reservoir 14C age is at ~ 1300 years during the deglacial warming, decrease to ~ 1000 years during the Antarctic Cold Reversal and 900 to 800 years at the Early and Upper Holocene respectively. These findings are consistent with Benthic-Planktic (B-P age difference) 14C ages reconstructions suggesting a vertical mixing with radiocarbon depleted deep waters since the onset of deglacial time. Our conclusions are substantiated from the exact synchronism between the marine and Antarctic ice core record providing as well new insight on deep-water ventilation in the South-Eastern Pacific Ocean.

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S06-O-04

RADIOCARBON SURFACE OCEAN RESERVOIR AGES OVER THE PAST 5,000 YEARS FROM PORITES MICROATOLLS, CHRISTMAS (KIRITIMATI) ISLAND, CENTRAL PACIFIC OCEAN

FINK D.(1), caRRIllI J.(1), McGReGoR H.(2), WooDRoffe c.(2), ZHao J.X.(3), fallon S.(4)

(1) Institute for environmental Research, anSTo, SYDneY, aUSTRalIa;(2) School of earth and environmental Sciences, UnIVeRSITY of WollonGonG, WollonGonG, aUSTRalIa;(3) Radiogenic Isotope laboratory, centre for Microscopy and Microanalysis, University of Queensland, ST. lUcIa QUeenSlanD, aUSTRalIa;(4) RSeS, The australian national University, canbeRRa, aUSTRalIa

AbstractWe present radiocarbon reservoir (ΔR) values over the past 5,000 years based on high-precision paired U-series and AMS 14C in modern and fossil Porites coral micro-atolls from Christmas Island (2N, 157W). The data set (n~25) allows temporal reconstruction of ΔR with ~250 year spacing. Christmas Island lies within the Equatorial Counter Current and the NINO3.4 region with a climate frequently punctuated by higher precipitation and warmer SSTs during El-Nino. Along its coastal perimeter, and throughout the internal network of tidal flats and lagoons, which in the late Holocene were flourishing reefal environments, fossil and modern microatolls abound. Microatolls are large discoid colonies with horizontal radial growth axes constrained in upwards vertical growth by spring tide low-water level. Consequently, a single microatoll can extend to ~9 m in diameter representing an exceptional ~300 years of continuous growth. Sr/Ca and δ18O in modern microatolls faithfully replicate instrumental climate records (SSTs, rainfall). Results from numerous multi-decadel and centennial fossil cores (1,500-5,500 years BP) shows distinct variability in ENSO variance both in frequency and amplitude domains compared to modern microatolls. These fossil populations are used to generate a temporal pattern of ΔR variability. Strict criteria were followed with respect to secondary calcite (via quantitative XRD), unaltered microstructure (via thin sections) and ensuring splits of identical coral chips for dual U-series and AMS 14C. Preliminary results shows a ΔR decrease at about 2,000 BP. Further analyses of correlations of ΔR deviations from the long term average with changes in regional ocean surface currents and in paleo-ENSO variance are in progress.

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S06-O-05

AN ATTEMPT TO RECONSTRUCT SOIL AIR pCO2 WITH C ISOTOPES IN STALAGMITES

FOHLMEISTER J.(1), ScHolZ D.(2), KRoMeR b.(1), ManGInI a.(1)

(1) Heidelberg acedemy of Sciences, HeIDelbeRG, GeRManY;(2) Institute for Geosciences, University of Mainz, MaInZ, GeRManY

AbstractCarbon isotope composition and pCO2 of soil air is influenced by vegetation density, which is driven by climate variations. Here we apply the stable and radiogenic carbon isotope composition of speleothems for the reconstruction of the soil pCO2 above the cave during the Holocene.In a first step a numerical model that describes the isotope composition of drip water upon reaction with the calcite of the karst was developed. The model allows for open and closed carbonate dissolution systems as well as intermediate dissolution conditions computed by contributions of the both extreme cases. Furthermore the model accounts for isotope fractionation processes occurring during degassing of CO2 and precipitation of CaCO3 inside the cave is accounted for.The reconstruction of recent and past soil pCO2 is performed by inverse modelling of the 14C and δ13C composition of monthly collected cave drip water and of a well dated stalagmite. The model is assessed by the comparison of the calculated soil pCO2 and of the monthly measured soil pCO2. The reconstruction delivers a probable range of recent soil pCO2, although the solution is not unique, due to the uncertainties originating in the unknown degree of open and closed system conditions during the carbonate dissolution. The convincing model performance for the present day situation allows to apply the model to a Holocene stalagmite. The reconstruction of past soil conditions reveals an increasing soil pCO2 within the last 5,000 years in the soil above the cave.

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S06-O-06

UNDERSTANDING VARIABILITY IN DEAD CARBON FRACTION IN HESHANG CAVE, CHINA

NORONHA A.(1), JoHnSon K.(1), RUan J.(2), HU c.(2)

(1) University of california, Irvine, IRVIne, UnITeD STaTeS;(2) china University of Geosciences, WUHan, cHIna

AbstractSpeleothems are calcite cave deposits, which have recently been identified as valuable terrestrial 14C archives. They have long been used in paleoclimate reconstructions, because they can be independently dated using 234U-230Th series (U-Th) measurements. Some speleothems display annual banding, and they can grow continuously for tens of thousands of years. Speleothem calcite carbon is derived from both soil CO2, and dissolution of the 14C free cave host bedrock. The incorporation of 14C free carbon creates a dead carbon fraction (DCF) in speleothem calcite, which could potentially vary over climate transitions. Some records of 14C from speleothems display stable DCF, but the mechanism for this apparently constant DCF is not well understood (Southon et. al., 2012; Hoffman et. al. 2011). In order to interpret speleothem 14C records as records of atmospheric 14C, studies of controls of DCF in speleothems are required.We will present the initial results of a study at Heshang Cave, Hubei Province, China (30.44°N, 110.42°E), the site of ongoing, extensive modern calibration and paleoclimate reconstruction efforts. Field trips were made to Heshang Cave in March and September of 2010, and June and July of 2011 to conduct detailed studies of carbon cycling in the modern cave system through collection and analysis of the δ13C and Δ14C composition of soil CO2. Monthly field trips are made to collect dripwater and modern calcite samples to investigate how seasonal environmental changes impact speleothem DCF and δ13C. A ~20 year section of a Chinese Pine was collected in July 2011 and is being analyzed to reconstruct a local record of Δ14C for comparison with monitoring data and a high resolution Δ14C record through the bomb peak based on a speleothem that was actively growing when it was collected in 2001. In addition, we have investigated climatic controls on DCF on longer timescales through Δ14C analysis of this annually laminated, U-Th dated stalagmite covering the Holocene, as well as preliminary work on another stalagmite which extends through the last glacial cycle.Modern calcite results show significant seasonal Δ14C variability of ~20‰, which may reflect exchange with cave atmospheric CO2 prior to crystallization. Despite a large range in the Δ14C values of dripwater DIC samples collected from throughout the cave, individual speleothem DCF appears quite constant over the Holocene, at 10 ± 2%, with an average age offset of 840 ± 190 years. Minor DCF variations may reflect climatic variability though and could introduce age uncertainties on the order of a few hundred years. We therefore argue that despite minor variations in speleothem DCF that operate on seasonal and longer timescales, DCF remains remarkably constant over the wide range of climates, so that speleothems from this and other locations may be well suited for use in improving the radiocarbon calibration curve beyond the tree ring record.

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S06-O-07

DATING SPELEOTHEMS WITH RADIOCARBON EXAMPLES OF DEAD CARBON PROPORTION VARIATION DURING THE HOLOCENE, LATE GLACIAL AND PART OF MIS 2-3 IN STALAGMITES FROM THE CHAUVET CAVE (S-FRANCE)

GENTY D.(1), MoReaU c.(2), DUMoUlIn J.P.(2), blaMaRT D.(3), boURDIn c.(1), DoUVIlle e.(3), GHaleb b.(4), HellSTRoM J.(5)

(1) lSce, UMR cea/cnRS/UVSQ 8212, l’orme des Merisiers, GIf-SUR-YVeTTe, fRance;(2) laboratoire de Mesure du carbone 14, UMS 2572, cea, SaclaY, fRance;(3) lSce, UMR cea/cnRS/UVSQ 8212, GIf-SUR-YVeTTe, fRance;(4) GeoToP, Université du Québec à Montréal, MonTRÉal, canaDa;(5) School of earth Sciences, The University of Melbourne, VIc 3010, MelboURne, fRance

AbstractSpeleothems are extensively used for past climate reconstructions mainly because they give, in addition to a climatic signal extracted from stable isotopes, a precise chronology thanks to uranium-thorium (U-Th) dating (i.e. error typically <1% to 5% and age up to ~450 ka). However, in some cases, the U-Th method does not give expected results because of low [U] content, low 234U/238U ratio or high detrital component (low 230Th/232Th). A few attempts have been made in the past to use radiocarbon dating on the calcite speleothem, but results were uncertain due to the unknown proportion of the carbon coming from the rock formation dissolution (the dead carbon proportion, or dcp) and the ignorance of its variability in the past. Moreover, the atmospheric radiocarbon calibration curve was not well known at that time. We present here the dcp results obtained on five stalagmites from the same cave (Chauvet Cave, South-France) that cover the last 30 ka.

We observe the following:

1) a low dcp value during most part of the Holocene (0-8 ka) (5.5 % ± 1.5);

2) a slightly higher dcp for the early Holocene, between 9 and 10.5 ka (10.5 % ± 2.5);

3) a large dcp decrease between ~15 ka and ~10.5 ka of an amplitude from 15 to 20 %;

4) extremely high dcp values during part of the glacial period (up to 50%) with very large variations (> 30%).

Thus, it appears that only stalagmites that grew during the most recent part of the Holocene can be dated with radiocarbon assuming a constant dcp. The later can be found by comparing one U-Th with one 14C analyse of the same aliquot, or by the detection of the 14C pre-bomb peak level in a modern stalagmite. Such a method can be very helpful when U-Th method does not work well or/and when we require only a small quantity of calcite in order to get the most accurate spatial resolution (few mg). Dating older speleothems implies calibrating the dcp with, for example, trace elements, which will be discussed here too.

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S06-O-08

RADIOCARBON RESERVOIR EFFECT IN THE FORMATION OF STROMATOLITES IN NAMIBIA

BROOK G.A., cHeRKInSKY a.

University of Georgia, aTHenS, UnITeD STaTeS

AbstractLacustrine stromatolites are layered accretionary structures formed in shallow water by blue-green algae. They are a precise indicator of high lake limits and their morphology and structure provide an insight into paleoenvironments of the time (Casanova, 1992).Previous research on lacustrine stromatolites from Etosha Pan in Namibia based on 14C ages of carbonates were close to the limit of the method. These ages suggested that the basin was not extensively flooded during the last 40 ka.We have investigated the radiocarbon ages of a stromatolite by dating both carbonates and organic sediments deposited during growth after extensive flooding of Etosha Pan. The stromatolite, about 15 cm in diameter, was separated in 12 zones from the center to the edge and samples were collected from each zone. Each sample was dated on carbonate and organic sediment material. All but two of the samples closely fit a linear regression of decreasing radiocarbon age from the center to the edge of the stromatolite. The 14C ages of the carbonate samples were in the range 34.7-24.7 ka and the 14C age of organic material was much younger ranging from 9.9-2.5 ka. The oldest dates for organic material 15.7 and 13.6 ka could be explained by contamination with old carbon, possibly from other organic rich deposits, which were eroded and washed into the lake by flooding. The δ13C values for these two samples (about -25‰) are also very different from the others (between -20 and -22‰) which are typical for algae organic compounds. The apparent old carbonate age is a result of the hard water effect from the closest springs which are saturated with the old dissolved inorganic carbon.Thus the ages based on the dating of organic carbon, along with petrographic and stable isotopic date for the stromatolite, have provided important new information on past flooding of Etosha Pan including evidence of prolonged lacustrine conditions during the Holocene Climatic Optimum.

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89

S06-O-09

CHARACTERIZATION OF RESERVOIR EFFECTS IN THE MECKLENBURG LAKE DISTRICT

FERNANDES R.(1)(2), DReVeS a.(1), GRooTeS P.M.(1), naDeaU M.J.(1)

(1) leibniz-laboratory for Radiometric Dating and Isotope Research, KIel, GeRManY;(2) Graduate School Human Development in landscapes, KIel, GeRManY

AbstractThe Mecklenburg lake district is located approximately 40 km inland from the Mecklenburg Bay (Baltic Sea, Germany) and is characterized by the larger Lake Schwerin and several smaller lakes such as Lake Ostorf. The region is of great archaeological importance for the study of neolithisation with many megalith monuments. Recently published radiocarbon data from Lake Ostorf demonstrate, however, the presence of large reservoir effects in Neolithic humans (Olsen et al. 2010). Isotopic analysis of human bone collagen showed low δ13C values overlapping the range from terrestrial food sources. Elevated δ15N values indicated freshwater fish consumption, though with no clear relationship between δ15N values and individual reservoir effect. A possible explanation lies in the variability of both isotopic signals and reservoir effects in freshwater species, associated with trophic level and feeding habits.A study was undertaken to characterize present day reservoir effects and isotopic signals in different faunal species, collected from Lake Schwerin and Lake Ostorf, including predators (eel and pike), bottom feeders (bream), and filter feeders (zebra mussels). Given the prevalence in the archaeological record of mussel shells, both mussel tissue and shell were analysed. The study was extended to include radiocarbon dating of aquatic plants (potamogeton) and algae (chara). Finally, radiocarbon was measured in dissolved inorganic carbon in water (DIC), dissolved organic mater (DOC), defined as having a grain size smaller than 0.45 µm, and particulate organic mater (POC). Such an integrated description of reservoir effects provides a great insight in the sourcing and routing of carbon along an aquatic food chain. It also provides useful information to define optimal strategies in establishing the variability of a local reservoir effect within the context of a glacially formed landscape of the southern Baltic coast in order to provide more accurate archaeological dates.

ReferencesOlsen, J., Heinemeier, J., Lübke, H., Lüth, F., and Terberger, T., 2010, Dietary Habits and Freshwater Reservoir Effects in Bones from a Neolithic NE German Cemetery, Radiocarbon 52(2), 635-644.

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90

S06-O-10

AMS DATING AND STABLE ISOTOPE MEASUREMENTS OF HUMAN REMAINS FROM THE AD 79 ERUPTION OF VESUVIUS

CRAIG O.E.(1), bonDIolI l.(2), faTToRe l.(2), HIGHaM T.(3), HeDGeS R.e.M.(4)

(1) bioarch, Department of archaeology, University of York, YoRK, UnITeD KInGDoM;(2) Soprintendenza al Museo nazionale Preistorico etnografico ‘luigi Pigorini’, RoMe, ITalY;(3) oxford Radiocarbon accelerator Unit, oXfoRD, UnITeD KInGDoM;(4) Research laboratory for archaeology and the History of art, oXfoRD, UnITeD KInGDoM

AbstractHuman bone collagen is a problematic medium for dating when there is a possibility that marine foods were consumed, as the 14C label will reflect the ocean reservoir to an unknown extent. One way around this has been to estimate the contribution of marine resources by independently measuring the δ13C value of bone collagen, and then to derive a corresponding marine reservoir correction to the measured date. A problem with this approach is that the relationship between δ13C and the reservoir effect is unknown and has to be estimated. To clarify this relationship, we have determined the δ13C values and radiocarbon dates of 9 human and 2 terrestrial faunal bones from Herculaneum. Crucially, the samples are from different individuals who perished during the AD 79 eruption of Vesuvius. We found a significant difference in the radiocarbon dates between some of the humans and the terrestrial animals. We compared this difference with the corresponding δ13C values. From these data we have derived i) an accurate assessment of the degree of marine consumption by each individual, using the best estimate of the maximum marine reservoir from this region, and ii) a regression equation which enables accurate calibration of radiocarbon dates based on δ13C. We also determined the δ15N values of each sample to examine the degree of marine consumption and increasing human collagen δ15N.

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91

SESSION 7

RADIOCARBON DATING AND THE PALAEOLITHIC

ConvenersC. Barshay-Szmidt (CA), N Conard (DEU), T. Higham (GBR), H. Valladas (FRA)

DescriptionRadiocarbon dating of material covering the Middle and early Upper Palaeolithic is very challenging. Even small amounts of contamination affect dating reliability. Dating is, however, crucially important if we are to understand important issues relating to modern human dispersals. How can we improve this situation? This session will be concerned with developments in the reliable dating of material from MOIS3 in Eurasia, the sub-continent and Africa (Middle and Late Stone Age). This will include improvements in laboratory and archaeological/field methodology (pre-screening, pre-treatment, methods to select samples from the least disturbed zones and well linked to human activity) and the interpretation of results, laboratory intercomparison issues, background corrections and the development of novel sample types that offer improvements in reliability. Papers could also embrace the question of previous results and their reliability. Papers discussing recent results from the period and their archaeological significance will also be welcomed. For instance, including such improvements may have had an impact on the dates of a particular site, affected a regional chronological framework or had implications as to potential interaction, dispersals or links between industries.

KeywordsPalaeolithic, MOIS 3, pretreatment chemistry, background corrections, contamination, measurement reliability, sample selection criteria for radiocarbon dating, Eurasia, Africa.

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92

S07-O-01

RADIOCARBON DATING THE EXTINCTION OF EUROPEAN NEANDERTHALS

HIGHAM T.(1), DoUKa K.(1), WooD R.(2), bRonK RaMSeY c.(1), JacobI R.(3)

(1) oxford Radiocarbon accelerator Unit, oXfoRD, UnITeD KInGDoM;(2) Research School of earth Sciences, canbeRRa, aUSTRalIa;(3) The british Museum, lonDon, UnITeD KInGDoM

AbstractTo understand the disappearance of the Neanderthals, a reliable chronology is required. This has largely eluded science thus far; despite many radiocarbon determinations being obtained from sites dating to the Middle to Upper Palaeolithic transition, our knowledge of the timing of this is opaque. The western European archaeological record constitutes the best evidence there is for the replacement of one species of human by another, so deciphering the signals of this transition assumes importance in understanding what happened. For example, exploring the dates of the disappearance of Neanderthals and the arrival of modern humans might help us to understand the possibilities for overlap between the two groups, and therefore whether there was any genetic or genetic exchange between the two populations.Dating material <2-3fMC is challenging, but work undertaken in Oxford over the last decade has improved the dating of material from this period. We have developed aspects of our pre-treatment chemistry, particularly the purification of bone collagen using ultrafiltration and in the dating of single amino acids from bone as well quantifying our background limits and corrections.Within a large project funded by the NERC in the UK, we have dated over 400 samples of bone, shell and charcoal from more than 50 key Palaeolithic sites in 10 countries. The main focus has been on sites with a succession of contexts containing lithic industries attributed to the Mousterian, Châtelperronian (all seemingly associated with Neanderthals), Uluzzian (now thought to be anatomically modern humans (AMH)), Aurignacian and Gravettian (associated with AMHs).In this paper we will discuss the emerging chronology for the disappearance of the Neanderthals by presenting results from some of the key sites in France, Germany, Italy, Spain and Belgium. We use Bayesian modelling to derive posterior density estimates for the final disappearance data of Neanderthals in each geographic location we have studied.

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93

S07-O-02

COMPARISON OF MIDDLE TO UPPER PALAEOLITHIC TRANSITION SITES IN SOUTHWEST FRANCE. AN ACCURATE CHRONOLOGY.

TALAMO S.(1), McPHeRRon S.(1), RIcHaRDS M.(1)(2), RoUSSel M.(1)(3), SoReSSI M.(3)(4)(1), HUblIn J.J.(1)

(1) Max Planck Institute for evolutionary anthropology, leIPZIG, GeRManY;(2) Department of anthropology, University of british columbia, 6303 nW MaRIne DRIVe, VancoUVeR, canaDa;(3) UMR 7041 cnRS, arScan, anTeT, 21 allée de l’Université,, 92023 nanTeRRe ceDeX, fRance;(4) Institut national de recherches archéologiques préventives centre archéologique d’orléans 525, 45590 SaInT-cYR-en-Val,

fRance

AbstractThe nature and duration of the Middle to Upper Palaeolithic transition (MUP) in Western Europe is one of the key ongoing debates in Palaeoanthropology. Central to this debate is the biological nature of the makers of the different lithic assemblages (Neanderthals and modern humans), and contradictory models have been proposed to explain the cultural evolution of these hominids. Common to all these questions is chronology, and Radiocarbon dating is the backbone of the time frame during this period, even though it is close to the limit of the method.We undertook an extensive radiocarbon dating program mainly on bones modified by human which allows us to propose a chronological framework of different sites dating to the Middle to Upper Palaeolithic transition in Southwest France. The main objectives were to remove contamination from the organic bone fraction, which generally results in younger ages, and to avoid the incorporation of exogenous carbon in the laboratory by careful cleaning of the equipment.We present chronologies of several sites in Southwest France spanning Mousterian to Aurignacian phases, using radiocarbon dates combined with stratigraphy in OxCal models (Bronk Ramsey, 2009). We conclude that with refinement of AMS 14C bone dating methods, including ultrafiltration, and the IntCal09 calibration dataset (Reimer et al., 2009), which resolved doubts about the reliability of 14C in the this time period (Talamo et al., 2012), more accurate chronologies for late Middle and Upper Palaeolithic sites in Europe are now emerging.

References1. Bronk Ramsey, C., 2009. Bayesian analysis of radiocarbon dates, Radiocarbon 51, 337-360.2. Reimer, P.J., et al., 2009. IntCal09 and Marine09 radiocarbon age calibration curves, 0 – 50 cal kBP, Radiocarbon

51, 1111-1150.3. T alamo et al., 2012. Debates over Palaeolithic chronology – the reliability of 14C is confirmed. Accepted for

publication in JAS

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S07-O-03

COMBINING ARCHAEOLOGICAL AND LABORATORY IMPROVEMENTS TO INCREASE ACCURACY AND PRECISION IN RADIOCARBON DATING: THE CASE OF GATZARRIA CAVE, FRANCE

BARSHAY-SZMIDT C.(1)(2), eIZenbeRG l.(3), DeScHaMPS M.(3)

(1) University of Pennsylvania, PHIlaDelPHIa, UnITeD STaTeS;(2) University of Toronto, ToRonTo, canaDa;(3) Universite de Toulouse-le Mirail UMR 5608 TRaceS, ToUloUSe, fRance

AbstractIn recent years there have been significant developments in the laboratory methods used to date MOIS3 samples, such as in pre-treatment and background corrections. These have led to improved precision and accuracy. It is clear, though, that combining these with careful archaeological considerations, such as sampling context, stratigraphic integrity and sample type including the strength of its link to hominin involvement, can only improve the reliability of the dating. These considerations are beginning to form a standard part of sampling decisions from recent excavations, but attention to these has usually been lacking in the past and when sampling from museum collections.In this paper we present the dating we carried out on animal bones from the 1960s and 1970s excavations carried out at Gatzarria Cave, Pyrenean France. This site is important for many reasons; it is among the rare sites to contain a stratified sequence of Proto-Aurignacian and Classic Aurignacian levels. It is also one of the few sites to contain a Vasconian Mousterian industry, a facies often thought to represent a late stage in the Mousterian and thereby potentially associated with the recent Neanderthals. Thus, it can help us to appreciate the chronological and taxonomic relationships between the various Early Upper Palaeolithic industries and between these and the late Mousterian, issues which are greatly debated currently.Although the excavation and recovery methods used at the time were advanced, (including three-dimensional plotting of many artifacts), the sloping topography of the cave, the homogeneous nature of the sediments, combined with horizontal excavation, meant that much of the material was incorrectly attributed in terms of layer. We established this by conducting an assessment of the stratigraphic integrity of the excavation through lithic analysis, including some refitting work. This helped us determine the most appropriate zones from which to sample.This paper focuses on the work we have done to date the Classic Aurignacian, Proto-Aurignacian and Vasconian Mousterian levels at the site, through the integration of this archaeological work with good laboratory methods. This site serves as a case-study into how to approach the dating of collections of excavations carried out before the benefit of taphonomic analyses. It also demonstrates that many published dated sites likely need to be redated by including these types of archaeological, as well as laboratory, methodological advances.The dates obtained at Gatzarria are stratigraphically coherent, with an overlap in dates between the Classic and Proto-Aurignacian. The Vasconian Mousterian is older here than has been argued at other sites. Gatzarria also contributes to the emerging pattern of a longer lasting Proto-Aurignacian than initially envisaged. We discuss these results within some of the larger technological, chronological and human behavioural issues of the Middle to Upper Palaeolithic transition.

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95

S07-O-04

DATING THE SWABIAN AURIGNACIAN

CONARD N.(1), HIGHaM T.(2)

(1) University of Tübingen, TÜbInGen, GeRManY;(2) University of oxford, oXfoRD, UnITeD KInGDoM

AbstractThe caves of the Swabian Jura of southwestern Germany provide one of the best archaeological records of the Aurignacian. Sites in both the Ach and Lone Valleys document a radical discontinuity in the material culture between the end of the Middle Paleolithic and the Aurignacian, which is often associated with the arrival of modern humans in the region. Here we summarize the results from recent excavations by the University of Tübingen and present new dates from Oxford Radiocarbon Accelerator Unit. The newest sequence of dates using ultra-filtration confirm the early age of the Swabian Aurignacian and provides important insights into the patterns of cultural evolution and population dynamics in Europe.

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96

S07-O-05

BAYESIAN MODELLING OF THE CHAUVET CAVE DATING

QUILES A.(1), VallaDaS H.(1), GeneSTe J.M.(2), GenTY D.(1), elaloUf J.M.(3), SaDIeR b.(4)

(1) lSce, GIf SUR YVeTTe, fRance;(2) cnP, PÉRIGUeUX, fRance;(3) cea Saclay, GIf-SUR-YVeTTe, fRance;(4) eDYTeM, UnIVeRSITÉ De SaVoIe, fRance

AbstractSince 1998, the Chauvet Cave (Ardèche, France) and its famous paintings have been studied by a multi-disciplinary scientific team who has performed research including climatic, geological, paleontological and biological studies, as well as archaeological context studies. The cave appears today as one of the most important for the study of the earliest manifestations and the development of prehistoric art at the beginning of the upper Paleolithic. In particular, different dating techniques like AMS-14C on organic material, U/Th TIMS on speleothems, 36Cl on rock collapse at the entrance of the cave, were carried out. Thus, more than 150 dates have been obtained from charcoal (soil and wall drawings), animal bones and calcite, in order to get thorough and relevant chronological information for the Chauvet Cave.The 14C dates so far obtained show that the cave was occupied during the Aurignacian period (32-30 ka 14C BP) and a few millennia later during the Gravettian period (28-25 ka 14C BP). Then, to further assess the accuracy of the 14C dates, an intercomparison program involving several international radiocarbon laboratories was carried out under the initiative of the LSCE. The successful result was published in (Cuzange et al, 2007).In the current study, we calibrated the set of radiocarbon dates with Intcal09. We also undertook a Bayesian approach to constrain the 14C dates (Valladas et al, 2004) using U/Th (Genty et al, 2004), 36Cl analyses (Sadier et al, 2012) as well as the archaeological, stratigraphic, and geological results obtained in situ. This statistical modelling, based on OxCal 4.1 software (Bronk Ramsey, 2009), will be used to specify the chronological framework of the Chauvet Cave occupations.

References1. Bronk Ramsey, 2009, Bayesian Analysis of radiocarbon dates, Radiocarbon 51(1), 2009, p. 337-360.2. Cuzange et al, 2007, Radiocarbon intercomparison program for Chauvet Cave, Radiocarbon 49 (2), p. 339-347.3. Genty et al, 2004, Datations U/Th (TIMS) et 14C (AMS) des stalagmites de la grotte Chauvet (Ardèche, France):

intérêt pour la chronologie des événements naturels et anthropiques de la grotte, C. R. Palevol 3, p. 629-642.4. Valladas et al, 2004, Chauvet, la grotte ornée la mieux datée du monde, Dossier Le Temps des Datations, Pour

la Science, p. 82-87.5. Sadier et al., 2012, New constraints on the Chauvet cave artwork elaboration, Proc natl Acad Sciences USA,

submitted

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97

S07-O-06

PRECISION RADIOCARBON DATING OF THE PALAEOLITHIC: THE CHRONOLOGY OF THE ABRI PATAUD, FRANCE

DOUKA K.(1), HIGHaM T.(1), DInnIS R.(2), neSPoUleT R.(3), cHIoTTI l.(3), bRonK RaMSeY c.(1)

(1) oRaU, RlaHa, University of oxford, oXfoRD, UnITeD KInGDoM;(2) Department of Prehistory and europe, The british Museum, lonDon, UnITeD KInGDoM;(3) Département de Préhistoire du Muséum national d’Histoire naturelle, UMR 7194, Musée de l’abri Pataud,

leS eYZIeS-De-TaYac, fRance

AbstractThe Abri Pataud is a key archaeological sequence in Les Eyzies-de-Tayac, in the French Dordogne. It is often used as a reference section for comparing Aurignacian and Gravettian cultural sequences against other sites in widely disparate regions. This is because the excavation of H. Movius in the 1960s was carefully undertaken and mixing of material seems rare due to the deposition of sterile layers between the successive archaeological horizons. In 2009, we worked on the radiocarbon chronology of the Aurignacian sections of the site, levels 14-9 (Early Aurignacian), and 8-6 (Evolved Aurignacian) and also produced a small number of dates from the Early Gravettian layer 5 (Higham et al., 2011). We showed that the previous chronology, established between the 1960s-1980s, was dominated by determinations that underestimated the real age of these layers, probably because of unremoved contamination and improved modern methods of estimating background subtractions for dating modern bone using AMS.Here we will present the results of further work on the site. Within the framework of AHOB3 (www.ahobproject.org), a new dating programme was undertaken in 2011-2012, focusing this time on the upper part of the Pataud sequence. We selected carefully identified cut-marked bone from layer 5 (Early Gravettian), layer 4 (Middle Gravettian, with Noailles and Raysse burins), layer 3 (Recent Gravettian) and layer 2 (Final Gravettian). Direct dating of all four stages of the French Gravettian –Abri Pataud is the only site to preserve this succession- was crucial in the re-assessment of the Gravettian chronological framework. Additionally, in our previous study (Higham et al., 2011), we emphasized the need to obtain more dates from layer 5 in order to understand the complexity of this major occupational phase of the site.We used the Oxford ultrafiltration procedure to extract datable collagen and we built a Bayesian statistical model to analyse the new dates. We compare this against climatic proxies to consider the wider implications of our results for the presence/absence of human groups at the site and in the wider region during MIOS3. The new chrono-stratigraphic model from Abri Pataud is an impressive example demonstrating how advanced radiocarbon pretreatment methods and modern statistical tools have revolutionized our understanding of the European Upper Palaeolithic.

ReferencesHigham, T.F.G., Jacobi, R.M., Basell, L., Bronk Ramsey, C., Chiotti, L. and Nespoulet, R. 2011. Precision dating of the Palaeolithic: A new radiocarbon chronology for the Abri Pataud (France), a key Aurignacian sequence. Journal of Human evolution 61(5): 549-563.

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98

S07-O-07

NEW AMS RADIOCARBON DATING OF THE TRANSITION FROM THE MIDDLE TO THE LATE STONE AGE IN TAFORALT CAVE, MOROCCO.

baRTon R.n.e.(1), boUZoUGGaR a.(2), HoGUe J.(3), lee S.(4)

(1) University of oxford, oXfoRD, UnITeD KInGDoM;(2) 2Institut national des Sciences de l’archéologie et du Patrimoine, RabaT, MoRocco;(3) Institute of archaeology, University of oxford, oXfoRD, UnITeD KInGDoM;(4) Research laboratory for archaeology & the History of art, University of oxford, oXfoRD, UnITeD KInGDoM

AbstractThis paper outlines the results of excavations of a long sequence of archaeological deposits at Grotte des Pigeons at Taforalt. The upper part of this sequence consists of a four-metre thickness of grey ashy sediments overlying yellow silty sands that contain a rich succession of Iberomaurusian microlithic backed bladelet industries. Below the base of the Iberomaurusian and separated by a thin sterile layer are a series of artefact layers containing flakes and side scrapers with affinities to Middle Stone Age/Middle Palaeolithic technologies. The sequence is dated by around 50 AMS dates on cut marked bone, charcoals and ostrich eggshell. These ages have been modelled using Bayesian analysis and suggest that the oldest Iberomaurusian lies at ~20-21 ka Cal BP. The nature of the age gap between this and the underlying flake industries will be discussed and we present new ideas on the Middle to Late Stone Age transition in the Maghreb.

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99

S07-O-08

THE EARLY TO LATE PALEOLITHIC TRANSITION IN KOREA: A CLOSER LOOK

BAE C.J.(1), bae K.(2), KIM J.(3)

(1) University of Hawai’i at Manoa, HonolUlU, UnITeD STaTeS;(2) Hanyang University, HanYanG, SoUTH KoRea;(3) Seoul national University, SeoUl, SoUTH KoRea

AbstractTraditionally, understanding the nature of hominin migrations in and around the Korean Peninsula during the Late Pleistocene has often been difficult due to the lack of syntheses of the archaeological and radiocarbon records. In a continuation of our recent research dedicated to trying to develop a clearer picture of the transition from the Early to Late Paleolithic in the region, we present new data and re-evaluations of old data on a series of previously excavated and newly identified sites in South Korea, with particular emphasis on changes to our knowledge of the Korean Paleolithic record since 2009. In the present study, we use calibrated radiocarbon dates to better understand the timing of the appearance of certain archaeological indicators (e.g., blades and microblades) of the Late Paleolithic in the region. Based on a more inclusive array of calibrated ages from Korean Paleolithic sites, it now appears that blade and microblade technologies may have diffused directly from Siberia rather than northern China as previously thought. In particular, multiple dates from Hopyeongdong (ranging from 31,950 ± 700 cal. years BP to 28,700 ± 850 cal. years BP), best known for the presence of blades and blade cores, predate recent calibrated AMS dates derived from Shuidonggou (ranging from 29,520 ± 230 cal. years BP to 23,790 ± 180 cal. years BP), the type site of the Chinese Late Paleolithic blade technology. It should be noted that other Korean Late Paleolithic sites (e.g., Hwadaeri, Hahwagaeri) also have dates between 40,000 to 30,000 cal. years BP, including an isolated date from Yonghodong (42,950 ± 1,500 cal. years BP), where a tanged point was excavated. At least some of these “early” ages have to some extent been tentatively accepted by specialists of the Korean Paleolithic. In addition, microblades and microblade cores were excavated from Jangheungri, with some of the earliest dates in eastern Asia for this type of lithic technology (29,500 ± 800 cal. years BP and 29,200 ± 1,250 cal. years BP). Clearly, the migration model of Late Paleolithic foragers moving from Central Asia to Shuidonggou (northern China) and then on to the Korean Peninsula and the Japanese Archipelago is too simplistic and needs to be revisited. In our view, it is also highly unlikely that blade and microblade technology evolved in situ in Korea without interactions with foraging groups from regions adjacent to the Korean Peninsula. In light of these Korean data, we present a revised model of Late Pleistocene hominin migration into the region that in turn triggered the transition from the Early to Late Paleolithic in Korea and possibly broader eastern Asia.Grant Sponsor: Korean Studies Promotion Service Grant, Academy of Korean Studies Grant (AKS-2010-DZZ-3102)

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SESSION 8

ARCHAEOLOGY - EURASIA AND AFRICA

ConvenersC.J. Bae (USA), H. Bocoum (SEN), m. Fontugne (FRA), Y. Kuzmin (RUS)

DescriptionDue to major advances in the application of radiocarbon dating methods and new archaeological discoveries in the past few decades, a number of significant changes have occurred in the Old World Holocene archaeological record. For instance, the meaning of the term “Neolithic” in archaeology has become more obscure. Pottery is now known in East Asia from the Terminal Pleistocene (ca. 14,800–13,300 BP) and associated with complex of hunter-fisher-gatherers. However, in the Levant it is generally accepted that agriculture preceded pottery-making. Other major contributions radiocarbon dating has provided prehistoric archaeology is a deeper understanding of the timing and nature of behavioral transitions (e.g., Neolithic-Bronze Age, Bronze Age-Iron Age, etc.), the spread of new technologies (e.g., diffusion of agriculture technologies across Europe, diffusion of iron metallurgy across Africa, both events that likely accompanied large scale human population movements), and the complex relationship between past climatic conditions, various ecological processes, and human activities.Our session aims to bring together archaeologists, radiocarbon specialists, palaeogeographers, and geoarchaeologists, to discuss recent findings in chronology and palaeoeconomy of a number of different topics currently being debated in Terminal Pleistocene-Holocene archaeology. For instance, presenters will discuss the earliest Neolithic (both pottery- and agriculture-bearing) complexes in Eurasia, in order to understand spatio-temporal patterns of the emergence of two key Neolithic phenomena (pottery and agriculture) and to understand the influence (or not) of climatic changes on these cultural transitions. Other speakers will present recent findings from other spatio-temporal points and topics (e.g., spread of plant and animal domesticates across regions like Africa and Europe and Oceania).

KeywordsOld World (Europe , Africa, Asia); Pleistocene-Holocene Transition; Marine Isotope Stages 2-1 Transition; Neolithic; Bronze Age; Iron Age; Plant and Animal Domestication

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S08-O-01

RADIOCARBON DATING THE CASTING CORES OF THE “CAPITOLINE SHE-WOLF”

CALCAGNILE L., QUaRTa G., D’elIa M., Gaballo V., coRVaGlIa e., MaRUccIo l.

ceDaD,, DePT. of enGIneeRInG of InnoVaTIon, UnIVeRSITY of SalenTo, lecce, ITalY

AbstractThe possibility offered by AMS to analyze samples of mass in the sub-mg range allows the extraction of suitable material for radiocarbon dating also from complex, inorganic matrixes containing only traces of organic residues such as the casting cores of ancient bronze statues. By this approach the dating of objects with a high cultural or religious value is possible with a high degree of accuracy which allows to solve historical controversies, often difficult to solve by alternative approaches. In this paper we present the results of the radiocarbon dating analyses carried out on organic residues extracted from the inner cores of the “Capitoline She-Wolf”, a bronze statue housed in a dedicated room in the “Capitolini” museums in Rome, Italy. The statue, of an extraordinary cultural and symbolic value, represents a she-wolf feeding two infants and it is inspired by the legendary founding of the city of Rome by the two twins Romulus and Remus. Although traditionally and almost unanimously considered Etruscan and dated to the 5th century BC, the dating of the statue has been subject, more recently, to large controversies among scholars. In fact considerations about the casting technology have suggested a possible dating of this artefact to the Middle Ages. In this study different samples of the casting cores, extracted from different areas of the statue were selected to be submitted to 14C dating. All the samples were screened and organic residues handpicked at the optical microscope and submitted to standard AAA chemical processing. It was possible to extract twenty-eight organic samples such as charcoal, vegetal remains and seeds in quantities suitable to allow their radiocarbon dating by AMS. All the analyzed samples gave consistent radiocarbon ages. Statistical tests showed a normal distribution of the data and allowed the combination of the measurements to a calibrated date in the 11th-12th centuries AD range, with a the two sigma confidence level. This study has thus given a fundamental contributions to the solution of this long-lasting controversy among archaeologists and art historians.

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S08-O-02

14C-DATING OF SO-CALLED “BRANDGRUBENGRäBER” IN THE LATE IRON AGE AND ROMAN PERIOD IN WESTERN FLANDERS (BELGIUM)

DE MULDER G.(1), De cleRcQ W.(1), Van STRYDoncK M.(2)

(1) Ghent University, GenT, belGIUM;(2) Royal Institute for cultural Heritage, bRUSSelS, belGIUM

AbstractA ‘Brandgrubengrab’ is a specific way of deposition of human remains whereby the cremated remains of the deceased and other remains of the pyre such as charcoal and burnt objects are jointly deposited on the bottom of a pit without any structured distinction, resulting during excavation in a homogenous black, lenticular layer sealed by soil which was thrown in the grave after depositing the pyre-remains. Typical for this type of cremation grave is that only a limited number of the cremated bones are deposited in the burial pit, probably as a pars pro toto for the deceased. This burial-type becomes predominantly popular during the Late Iron Age and the Roman period, when it was the main funerary structure used in western Flanders.These burials are traditionally dated by the funerary objects accompanying the deceased. In the last years however, more attention has been paid to develop a chronology for these funerary structures independent from material-culture by using the 14C method. In view of the mostly very limited amount as well as the heavily fragmented nature of the cremated bone present in the graves, most radiocarbon dates are obtained from charcoal found in the bottom-layer of the graves originating from the pyre. In the funerary rite, oak clearly was the preferred combustible and samples for radiocarbon dating hence predominantly originate from carbonized oakwood.We have a set of 37 14C-dates coming from a few small cemeteries and isolated cremations. Most of these sites cluster in the Ghent-Bruges area. The results of the radiocarbon analysis applied to the burials are fourfold. Firstly, 14C-dating based on a good prior selection of charcoal samples proves to be a valuable tool for establishing funerary chronology in the region during the period 2,200-1,750 BP. All dates fall within the expected broad timeframes, suggested by material culture found in the graves. Secondly however, existing chronologies based on pottery finds are refined and adjusted within the periods concerned, notably the Roman period, and graves without grave goods can now also be placed chronologically. This is over more of importance since many grave-goods consist of typo-chronologically less datable hand-made ceramics of local provenance which can now be dated more precise. Thirdly, the distribution of dates ranges clearly demonstrates a peak in the first two centuries AD. This seems to be a historic fact since Iron Age and post-3th century AD Roman occupation are considerably less well documented in settlement research too. Fourthly and of great importance for the understanding of the funerary rite, the 14C-results indicate an important change in the structure of these cremation graves in the transition from the Late Iron Age to the Early Roman period, ca. 2,100-2,000 BP. The small irregular shaped cremations of the Late Iron Age become replaced by more uniformly structured Brandgrubengräber which have a rectangular or quadrangular form in plan.

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S08-O-03

BOOM AND BUST IN EUROPE’S EARLY FARMING POPULATIONS

EDINBOROUGH K., SHennan S., TIMPSon a., DoWneY S., THoMaS M.

University college london, lonDon, UnITeD KInGDoM

AbstractWe present summed calibrated radiocarbon date distributions from a number of regions across the western half of Europe as a demographic proxy (6,000-2,000 CalBC). We develop a new set of statistical tools that allow for the identification of significant features in summed calibrated date distributions, as well as correlations with other temporal processes, whilst dealing with concerns regarding sample sizes and sampling error, taphonomic losses, long term population trends, multiple samples from sites, and potentially unjustified features in the calibration curve. Our results indicate that West European populations grew rapidly in many regions with the onset of farming, but that these growth rates were not sustained. The new subsistence system, despite its potential for supporting increased populations in any suitable area, did not bring long-term stability. The characteristic regional pattern indicated by changing population densities is one of instability; of boom and bust. We demonstrate the existence and quantify the scale of these instabilities and discuss the possibility that they have endogenous or exogenous causes.

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S08-O-04

RADIOCARBON CHRONOLOGY OF THE EARLY IRON AGE AND MEDIEVAL SITES IN SUZDAL LAND, CENTRAL RUSSIA

ZAITSEVA G.(1), MaKaRoV n.(2), a feDoRIna a.(2), GRooTS P.(3)

(1) Institute for the history of Material culture, Russian academy of Sciences, SaInT-PeTeRSbURG, RUSSIan feDeRaTIon; (2) The Institute of archaeology of Russian academy of Sciences, MoScoW, RUSSIan feDeRaTIon;(3) christian-albrecht University, KIel, GeRManY

AbstractThe chronology of the Iron Age and Medieval sites located in Suzdal Land up to the recent time was based exclusively on the archaeological evidences. Corpus of archeological materials from this important medieval region increased significantly during the last decades after large-scale field projects were conducted by the Institute of Archaeology (Moscow). These materials provide opportunity to determine chronological positions of the majority of the sites and to outline the basic stages of colonization and cultural changes in the region (Makarov, 2009). However, many aspects of settlement history in the region remain controversial and need more thorough examination. Radiocarbon dating is important in this context as it can check and correct some archaeological conceptions. Radiocarbon dates have a special relevance due to the specific character of the cultural landscape of Suzdal land where medieval sites with the stratified occupational deposits are rare exceptions. At present more than 100 14C dates have been produced from 11 settlements in the Suzdal Land. A new chronological horizon of antiquities has been identified on the sites of the region which is dating to the first half and the middle of the 1st millennium AD. Some of the sites yielded the antiquities from the horizon of the 9th – first half of the 10th centuries AD. One can assume that the new settlements network and new material culture reflecting integration of Suzdal Land into the system of international trade and the Baltic cultural relation began to develop in the second half of the 9th century at the latest.The large series of 14C dates that fall into the range of the 10th -12th centuries AD confirm earlier observations that this period was the time of the intensive colonization and settlement growth. The series of radiocarbon dates which indicate the period from the middle of the 13th to the middle of the 14th centuries AD confirms that some rural settlements founded in the 10th -12th centuries AD survived the Mongolian invasion and continued to exist in the second half of the 13th AD. Radiocarbon dates were produced in the radiocarbon laboratory of the Institute for the History of material culture (St.-Petersburg) and Kiel laboratory.

ReferencesMakarov N.A. 2009. Archaeological study of the North- East Russia: colonization and the cultural traditions.// Herald of the Academy of Sciences #12, pp. 1068-1077.

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S08-O-05

CENTERS OF THE NEOLITHIZATION OF THE STEPPE ZONES IN EUROPEAN RUSSIA

VYBORNOV A.(1), ZaITSeVa G.(2), KUlKoVa M.(3)

(1) Samara State academy of Social Sciences and Humanities, SaMaRa, RUSSIan feDeRaTIon;(2) Institute for History of Material culture, ST.PeTeRSbURG, RUSSIan feDeRaTIon;(3) Herzen State Pedagogical University, ST.PeTeRSbURG, RUSSIan feDeRaTIon

AbstractThis research is supported by Russian Humanitarian Foundation, grant 10-01-00-393 and grant 10-01-00553a/B, Russian Foundation for Basic Research, grant 10-06-00096a.The steppes between the Volga and the Don are the key to the understanding the process of neolithization of vaster territories. The Early Neolithic in Lower Podonye is presented by Rakushechny Yar culture, and by Kairshak and Yelshanskaya ones on Volga-Urals interfluve. 14С dates proved their early age. But there are still a number of questions. In the cultural layers of Rakushechny Yar were found poorly ornamented flat bottom pottery, with no microlith in lower layer. There are domestic animals, stone vessels. The food crust of ceramic from lower layers is dated to 7,930-7,680 BP. All these features let us suppose that the origin of this culture is the result of the infiltration from Anatolia. Prototypes could be assemblages of Hallan Cemi type with flat bottom drilled stone vessels dated to VIII millennium BP. Pointed bottom pottery was found in the 13th layer dated to 7,250 ± 150 BP 6,930 ± 130 BP. Its origin is connected with Sura culture 7,250 ± 95 BP, 7,125 ± 60 BP (on bones). This group favours the neolithization up to the Oka, where the similar vessels were found (6,870 ± 100 BP).Kairshak culture of the Northern Caspian Sea area is characterized by flat bottom scratched silt pottery, proper of Mesolithic microlith, wild animals. It is dated to 7,800 - 7,200 BP on pottery and food crusts. The centre of neolithization, that influenced on the steppe Pvolzhye, was forming here. Thus assemblages dated to 7,760 - 6,544 BP and similar to the Caspian Sea area ones were found at Varfolomeevskaya site.Yelshanskaya culture is presented in the north of the Volga-Urals by poorly ornamented pointed bottom pottery made of silty clay. This centre is dated to 8,000 - 6,900 BP. All the features denote its Central Asian origin. The eastern trend is confirmed. Yelshanskaya culture centre influenced the neolithization of the Middle Volga, the Vyatka, the Sura, the Middle Don, Upper part of Western Dvina where the similar assemblages are dated to 7,300-6,900 BP.

References1. Dolbounova E., Kulkova M., Mazourkevitch A. 2011. The results of comprehensive research of clay vessels

from Rakushechny Yar /Neolithic of Middle Povolzhye in Eurasian context. Samara2. Dolukhanov P., Shukurov A., Vybornov A., Kovaliukh N., SkripkinV., Zaitseva G. 2009. The spread of the

Neolithic in the south east European plain. Radiocarbon V51, №23. Zaitseva G., Timofeev V., Sementsov A. 1999. Radiocarbon dating in the Institute for the History of Material

Culture, Russian Academy of Sciences//RA №44. Zaitseva G., Skripkin V., Kovaliukh N., Possnert G., Dolukhanov P., Vybornov A. 2009. Radiocarbon dating of

Neolithic pottery/ Radiocarbon V 51 №2.5. Vybornov A., Vasilieva I. 2011. On the earliest pottery in the Middle Povolzhye/Oslo6. Vybornov A., Kulkova M. 2012. New dates on Yelshanskaya culture. SSC RAS. Samara

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S08-O-06

TWO TRAJECTORIES IN THE NEOLITHISATION OF EURASIA: POTTERY VERSUS AGRICULTURE (SPATIOTEMPORAL PATTERNS)

KUZMIN Y.

Institute of Geology and Mineralogy, noVoSIbIRSK, RUSSIan feDeRaTIon

AbstractThe term “Neolithic” originally meant the presence of polished tools and pottery, and since the 1920s the ‘agricultural’ definition of the Neolithic became prevalent. It is obvious that no worldwide universal definition of the term “Neolithic” exists today.In order to understand the spatiotemporal relationship between pottery and agriculture, information about the timing of their appearance in key regions of Eurasia [in calendar ages for the appearance of pottery (Apot) and the invention/introduction of agriculture (Aagr)] was taken from published sources. The difference between them is therefore ΔApot–agr.In East Asia, the ΔApot–agr varies from ca. +13,000 yr to ca. +2,000 yr. In mainland Southeast Asia it is about +200–2,100 yr, while in island Southeast Asia it is ca. +1,500–0 yr. This is the so-called ‘East Asian’ trajectory with positive ΔApot–agr values. Here pottery is the main criterion for determination of the Neolithic complexes. In different parts of Siberia, it varies from +10,200 yr (Transbaikal) to +4,700 yr (Trans-Urals and Western Siberia). A similar trend is common for some parts of Central Asia (Kazakhstan, +2,000 yr) and southern India (+1,000 yr).However, in the Near and Middle East the ΔApot–agr values are always negative indicating that the emergence of agriculture is the criterion of the Neolithic. In the Levant it is ca. -3,500 yr, in Syria -4,000 yr, and on Cyprus -4,300 yr. Further west (and sometimes northeast), it is almost zero, because agriculture and pottery were brought together as a “Neolithic package”. These regions include western Anatolia; Turkmenistan; the Mediterranean and Iberian coasts; the region of LBK pottery (primarily Hungary, Croatia, Serbia, Austria, southern and central Germany, and the Czech Republic); and the British Isles. There are slightly positive ΔApot–agr values for the Low Countries (northern France, Belgium, and the Netherlands; +1,000 yr); and Ukraine and Moldavia (+400 yr). The situation in Northern Europe (northern Germany, Denmark, Fennoscandia, and the Baltic coast) is more complicated, without a clear trend.In Eastern Europe the ΔApot–agr values are closer to East Asia rather than to the Near East; for the southern Russian Plain it is +3,100 yr; for the southern Urals +5,000 yr; for the eastern Russian Plain (middle and lower courses of the Volga River) +4,900–4,000 yr; and for the central Russian Plain +4,000 yr.It seems that the ‘agricultural’ Neolithic has its origin in Levantine societies of early cultivators at ca. 11,500–12,500 cal BP, with a subsequent spread after ca. 9,000 cal BP toward Central/Western Europe, and some parts of Central and South Asia. The ‘pottery’ Neolithic is to a major extent an independent invention, with several centres of the emergence of pottery-making technologies after ca. 18,300 cal BP throughout Eurasia.

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S08-O-07

14C CHRONOLOGY OF TWO BURIED EPIPALAEOLITHIC/PPN (?) SITES IN ANATOLIA. ITS SIGNIFICANCE FOR EASTERN MEDITERRANEAN CULTURAL CONTINUITY AND DOMESTICATION PRACTICES DURING THE YOUNGER DRYAS AND THE ONSET OF HOLOCENE

KUZUCUOGLU C.(1), fonTUGne M.(2), baSaRan M.(3), eMeRY-baRbIeR a.(4), RobeRT V.(1), DeGeaI J.P.(1), GaUTHIeR a.(1), le DReZen Y.(5)

(1) lGP, UMR 8591, cnRS.Universités Paris 1 and Paris 12, MeUDon, fRance;(2) lSce, UMR 1572 cnRS/cea/UVSQ, GIf-SUR-YVeTTe, fRance;(3) Prehistory Department, Istanbul University, ISTanbUl, TURKeY;(4) aRScan, UMR 7041, cnRS/Universités Paris 1 and Paris 10, nanTeRRe, fRance;(5) PRoDIG, UMR 8586, Université Paris 1 (cnRS/Paris 1 and Paris 7), PaRIS, fRance

AbstractAMS 14C dates obtained from two sedimentary sequences cored in Anatolia allow to identify clearly two buried epipalaeolithic/Pre-Pottery Neolithic (PPN) sites. Together with many 14C dating, pollen, mineralogy and sedimentology analyses have been performed on these sequences. These preliminary results will be discussed on the light of our knowledge and interpretation of human cultural developments in Eastern Mediterranean at the turn of Late Glacial/Holocene.The Öküzini site (Antalya) on the Mediterranean coast of Anatolia facing Cyprus, is formed by marshes fed by a karstic spring. Here, the hard water effect has been traced and measured by cross-dating (at LSCE-Gif/Artemis-Saclay) different materials from the same samples: organic matter in sediment bulk, and/or plant remains, and/or wood charcoals. Results show a spatial variation of apparent 14C age oldering in relation to two different aquifers feeding two distinct springs. Buried at a -400-494 cm depth, archaeological layers have been identified and dated Younger Dryas (YD) and Early Holocene. This chronology is firmly controlled, thanks to the richness of sediments in charcoal pieces. Out of the main results from the analyses of the Öküzini marsh sediments, the pollen content will be discussed in more details, as it shows the gathering and storage of cereals as early as during the Younger Dryas and the YD/Early Holocene boundary.At Asikli site in western Cappadocia (central Anatolia), a core performed next to a PPN tell went through a YD and Holocene-onset sediment accumulation of archaeological layers, the age of which points to a possible first epipalaeolithic site identified in Cappadocia. This attribution to Epipalaeolithic will be either rejected or confirmed when a test trench will be excavated in next July. Buried below 2 m of recent slope deposits, this sequence may record the continuity of human occupation and cultural development in the region since the beginning of the YD, thus providing crucial information on the possible genuine development of plant-predomestication and domestication practices as well as sedentarisation in central Anatolia.In conclusion, the data obtained from both Öküzini and Asikli cored sequences will be compared to available data from excavated epipalaeolithic and early PPN sites in the Eastern Mediterranean, mainly in the mid-Euphrates valley, but also and especially in central Anatolia (Pinarbasi, Boncuklu) and in Cyprus (Shillourokambos). Comparison suggests that both sequences presented here are very important for the understanding of the spatial distribution of early sedentary communities and the local neolithization process in favour of the hypothesis of multi-regional centers, as well as for the timing of plant-domestication processes in the Eastern Mediterranean.

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S08-O-08

CULTURE CHANGE THROUGH THE LENS OF SUPRA-REGIONAL TEMPORAL DYNAMICS. CASE OF THE PRE-POTTERY NEOLITHIC

JACOBSSON P.

University of edinburgh, eDInbURGH, UnITeD KInGDoM

AbstractAnthropology has long appreciated that the timing of events is the key to understanding the meaning of cultural processes. While the detailed resolution of such studies in a living society is in most cases beyond the reach of archaeological research, questions remain as to whether difference in cultural praxis leaves a trace on the greater scales of supra-regional radiocarbon sequences. The paper explores this problem with reference to the process of the first neolithization in the Near East, beginning in the Epipalaeolithic and ending with the onset of sixth millennium BC.A simple procedure for visualisation is proposed. The extents of calibrated radiocarbon date sequences from the period have been placed against a centennial axis. For each century a count of discontinuities has been conducted (onsets, terminations and stratigraphic divisions supported by absolute dates), producing a graph of instability within the cultural networks during the neolithization process. This graph was subsequently folded onto its previous values, so as to produce a two-dimensional map of instability patterns throughout the period. Finer temporal division demonstrated marked transformation to the instability patterns with the onset of the PPNB at c. 8,600 BC, as well as a complex set of transformations during the seventh millennium BC. This information supports general observations from material culture studies of the PPN and makes a case for use of radiocarbon sequences not only as a chronometer of cultural process in prehistory, but also as a means of describing such processes.

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S08-O-09

IRON AGE IN ISRAEL – A NEW BAYESIAN CHRONOLOGY

LEE S., bRonK RaMSeY c.


AbstractThe Iron Age chronology in the Levant has been a hotly debated issue. Scholars have been trying to establish a chronology for the period between the collapse of the Egypto-Canaanite system in the twelfth century BCE (1,140/1,130 BCE) and the Assyrian conquests in the eight century BCE (between 732 and 701 BCE). Establishing a consensus on the Iron Age chronology has far reaching implications on relative chronologies in other regions around the Mediterranean, Israelite history, historiography and on biblical history. The debate has centred around the Conventional (or High) chronology and the Low chronology. These chronologies are based on data from pottery typology, stratigraphic analyses and attempted correlations to historical sources across different sites.Bayesian methods have been widely used to address the Iron Age chronological debate but a consensus has not been reached. This is largely because radiocarbon dates of materials in this period lie on an oscillation in the calibration curve. This presentation focuses on the modelling of radiocarbon dates from the Iron I and Iron II periods, discusses the underlying assumptions and limitations of existing comprehensive Bayesian chronologies and proposes the use of a more appropriate model which allows for the transition not being instantaneous. The new model sheds light on the probably duration of the transition between the two periods.

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110

S08-O-10

WEST CENTRAL AFRICAN PEOPLES: SURVEY OF RADIOCARBON DATES OVER THE PAST 5000 YEARS

OSLISLY R.(1), faVIeR c.(2), fonTUGne M.(3), benTaleb I.(2), GIlleT J.f.(4)

(1) Institut de recherche pour le Développement, YaoUnDÉ, caMeRoon;(2) University Montpellier 2, MonTPellIeR, fRance;(3) lSce IPSl, GIf SUR YVeTTe, fRance;(4) University Gembloux, lIÈGe, belGIUM

AbstractTracing human history in West Central Africa run up against the scarcity of historical data and archeological remains. In order to provide new insight into this question, we performed a review of 931 radiocarbon dates of archaeological sites from Late Stone Age, Neolithic Stage, Early and Late Iron Age in Cameroon, Gabon, Central African Republic, Republic of Congo and West Democratic Republic of Congo. Maps of human occupancy were the derived from 4,000 cal BP to present at 100 year time step. This synthesis first emphasizes the regions with low sampling intensity, namely South East Cameroon, Adamawa Plateau, Sangha Interval. Then, it provides a spatiotemporal framework of history of human settlement in the forest area. Beyond the well-known initial spread of iron-age population through the forest ca. 2,500 cal BP, it depicts the geographical patterns and the links with cultural evolution of the successive phases of human expansion from 5,000 BP to 3,000 BP and then from 3,000 BP to 1,500 BP, of hinterland depopulation until 1,000 BP, of recolonization until 500 BP and slight fall after.

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S08-O-11

FIRST DIRECT RADIOCARBON DATING OF TWO UNDISCOVERED DECORA-TED CAVES IN LOWER CONGO (DEMOCRATIC REPUBLIC OF THE CONGO)

HEIMLICH G.(1), GanDolfo n.(2), laVal e.(2), MenU M.(2), RIcHaRDIn P.(2)

(1) Université de Paris I Panthéon-Sorbonne, Université libre de bruxelles, PaRIS, bRUXelleS, fRance;(2) centre de Recherche et de Restauration des Musées de france, c2RMf, PaRIS, fRance

AbstractLower Congo rock art is concentrated in a region that stretches from Kinshasa to the Atlantic coast and from Northern Angola to Southern Congo-Brazzaville. In Central Africa, Lower Congo has one of the richest concentrations of rock art. Although Lower Congo rock art was identified as far back as the XIXth century by James Tuckey in the course of his exploration of the Congo River, it had never been a subject of thorough investigation.Now inhabited by the Ndibu, one of the Kongo sub-groups, the Lovo Massif is situated north of the ancient Kongo kingdom. Although the Kongo kingdom after 1,500 is one of the best-documented kingdoms in all Central Africa, from historical as well as both ethnographic and anthropological sources for more recent periods, it remains unknown archaeologically. The little archaeological research done in the Lower Congo region so far shows the high density of prehistoric inhabited sites and the presence of sedentary populations with pottery, polished stones, and probably villages around 500 BC. There is a gap in the archaeological record between AD 250 and 1,000. After that date, several ceramic traditions related to the kingdom have been discovered. Their dispersion corresponds to complex trading networks.With 93 sites (including 59 decorated caves), the Lovo Massif has the largest concentration of rock art in the entire region. Hundreds of limestone outcrops with carved surfaces, punctuated by numerous caves and rocky overhangs, rise up over an area of about 400 square kilometers. The inventory comprises mostly geometric designs that can be related to anthropomorphs and zoomorphs (lizard-like shapes, antelopes). There are also a very few therianthropes (human/animal figures), alphabetical inscriptions and positive hands or plant shapes.In 2010 and 2011, we were able to take pigment samples in two undiscovered decorated caves in Lower Congo, the westernmost region of the present-day Democratic Republic of Congo. Unlike the Sahara and Southern Africa, both extensively prospected, rock art of Central Africa is still widely unknown and is still not dated. Dating rock art in Africa using radiocarbon is a real challenge and only a few direct datings have been yet obtained. After verifying that the pigment samples were indeed charcoal, it was obvious to rely to date them on carbon-14 in accelerator mass spectrometry (AMS).For the first time, we were thus able to directly date the occupation of two caves of Lower Congo. This communication will allow us to specify the chronology and interpretation of these rock images.

ReferencesHeimlich, G. (2010) Lower Congo revisited. Nyame Akuma. bulletin of the Society of africanist archaeologists 74, 42-50

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S08-O-12

HOW TO CHOOSE OUR BANTU BRIDE: RADIOCARBON DATING TO RECONSTRUCT THE SOCIAL DYNAMICS OF THE FIRST VILLAGERS AND IRON SMELTERS EXPANSION THROUGH CENTRAL AFRICA

CLIST B.

Gent University, GenT, belGIUM

AbstractFollowing the early villagers’ expansion through Central Africa from Cameroon to northern Angola, the help of radiocarbon dating has let us identify their presence north of the Equatorial forest between Yaoundé and Kribi in Cameroon before 3,000 BP in a degraded forest environment, and pinpoint the earliest villages in bas-Congo and probably in northern Angola south of the evergreen forest around 2,300 BP at the latest. Already some data from recent field and lab work suggest two waves of advance for these villages, one along the Atlantic coast, the other one further inland, each following a rough north to south axis.A critical synthesis of our knowledge about early metallurgy chronology in West, Central, and East Africa, pinpoints the earliest iron production between 800-400 cal BC in West Africa, around 800 cal BC in Central Africa, and around 800 cal BC in the Great Lakes area of East Africa. Iron smelting techniques are transmitted fast along the network of neolithic social ties which were layed down for the few last centuries in Central Africa helped by a dry climatic period opening up corridors through the forest .Two phases are suggested: the first one with iron smelting centres in Cameroon and Gabon trading iron tools to still neolithic villages, a second one with locally crafted iron products by more widespread smelters.A critical attitude to radiocarbon evidence by archaeologists is again recommended using several test cases, like the proposal of a demographic crash in at least some parts of the region during several periods of the last 2,000 years using only the number of radiocarbon dates processed.

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S08-O-13

THE LATE PALEOLITHIC TO NEOLITHIC TRANSITION IN KOREA: EXTRINSIC OR INTRINSIC FACTORS?

BAE K.(1), bae c.J.(2), KIM J.(3)

(1) Hanyang University, anSan, SoUTH KoRea;(2) University of Hawai’i at Manoa, HonolUlU, UnITeD STaTeS;(3) Seoul national University, SeoUl, SoUTH KoRea

AbstractBased on current archaeological and radiocarbon data, the Late Paleolithic to Neolithic transition in East Asia occurs between the post Last Glacial Maximum (LGM; ~15,000 years BP) and the Early Holocene (~8,000 years BP). During this time interval, evidence for full scale plant and animal domestication appears in China, but does not appear until much later in Korea and Japan. Pottery appears early in China and Japan, but later in Korea. Microliths, which appear during the Late Paleolithic (c. 25,000 years BP) in Korea, displays a great deal of variability during the Late Paleolithic to Neolithic transition. This stone tool variability may be explained by stylistic preferences specific to either the region or foraging communities and/or functional variation. Evidence from this time period suggests that the Korean peninsula may have been less densely populated vis-à-vis China and Japan. Different reasons may exist to explain variation in population density between these different regions. In the case of central China where many of these archaeological traces initially appear the region is relatively more open plains and less mountainous facilitating human interactions. In Japan, the reliance on anadromous fish, particularly around areas where the seasonal fish congregated in large numbers, contributed to higher population densities. The Korean peninsula is ~70% mountainous leading to pockets of communities that may have been somewhat isolated, though certainly not completely. These reasons are likely to have contributed to higher population densities in China and Japan, while at the same time indirectly suggestive of lower population densities in coeval Korea. This paper explores these patterns in the archaeological data comparing the Korean record with the coeval Chinese Neolithic and Japanese Jomon records. We also review the current hypotheses being proposed by researchers to explain the nature of the transition from the Late Paleolithic to Neolithic transition in Korea, particularly in its regional context and more robust radiocarbon dating analyses. With rising sea levels after the peak of the LGM, there would have been an increase in territorial circumscription in the region. The rising sea levels could have contributed to foraging groups being less mobile at the end of the Paleolithic, eventually leading to full scale sedentary villages during the Neolithic in Korea.Grant Sponsor: Korean Studies Promotion Service Grant, Academy of Korean Studies Grant (AKS-2010-DZZ-3102)

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S08-O-14

ARCHAEOLOGICAL RESEARCH IN THE HIMALAYA REGION BY 14C AMS DATING 0F WOODEN DRILL CORES FROM HISTORIC BUILDINGS

SCHARF A.(1), KReTScHMeR W.(1), bRÄUnInG a.(2), DaRaGon f.(2)

(1) erlangen University, eRlanGen, GeRManY;(2) Geographical Institute, erlangen University, eRlanGen, GeRManY

AbstractIn recent years, the Geographical Institute of the University Erlangen could sample numerous wooden drill cores from historic buildings in four regions of High Asia and could evaluate them dendrochronologically. Part of the drill cores were collected from monasteries and temples in the Dolpo region of western Nepal, a barely studied region in the Inner Himalaya and situated in the rain shadow of the main Himalayan crest line. Another major part came from temples in Central Tibet. In many cases tree-ring dating of these drill cores was not possible, indicating that the sample woods exhibit a higher age than the present range of the existing tree-ring chronologies which only reach back to the 11th century. So these samples can be used to extend the tree-ring chronologies of this region, which could help to detect suggested monsoon variations during the Middle Ages. The historic tower buildings of Tibet and Sichuan are a special cultural heritage which has been rarely studied up to now. The knowledge of their exact age could help to better understand the cultural and historical context of their development and their function, and could support the effort to declare them a UNESCO World Heritage site. The Erlangen AMS laboratory has performed 14C - AMS datings on 200 samples of 74 of these drill cores. Using wiggle-matching these drill cores could be dated with enhanced precision, and in many cases important information about the time of construction of these important historic buildings could be obtained for the first time.

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S08-O-15

AN EXPANDED SET OF CALENDAR AGES FOR BRONZE-IRON AGE TRANSITION IN CENTRAL ASIA DRAWN FROM ARCHAEOLOGICAL TREE RINGS WITH RADIOCARBON

PANYUSHKINA I.(1), GoRYacHeV a.(2), GRIGoRIeV f.(3), MaR’YaSHeV a.(2), cHanG c.(4)

(1) Tree-Ring Research lab, University of arizona, TUScon, UnITeD STaTeS;(2) a. Kh. Margulan Institute of archaeology, alMaTY, KaZaKHSTan;(3) central State Museum of Kazakhstan, alMaTY, KaZaKHSTan;(4) Department of anthropology, Sweet briar college, SWeeT bRIaR, UnITeD STaTeS

AbstractAs early as the 1960s, Saka kurgans of the Ili Valley in a large agro-pastoral hub of the semi-desert Semirechye region lying just north of the Tian Shan Mountains (Kazakhstan) underwent a vigorous excavation program led by prominent archaeologist- Kemal A. Akishev and his progeny. The cultural uplift of this region during the Iron Age (800 BC - AD 400) is exemplified by the pyramid-like kurgans built by Tigrahauda-Saka on the eastern outskirts of the Saka homeland – Fergana Valley. Archaeological surveys and site excavations identified manifold clusters of kurgans and cemeteries throughout the region, linked to the remains of ancient settlements dated to few transitional periods between the Bronze and Iron Ages (1600-800 BC) and the Early Iron Age (400 BC). Socio-cultural transformations of this region during the transition involved development of horse-riding pastoralism, the combination of farming and herding economies, and in some cases subsequent sedentism. The existing incomplete chronology of Bronze-Iron Age in Semirechye does not permit to develop a coherent explanation for the observed diversity of economic strategies in the region (1, 2).The collection of Bronze and Iron Age timbers from Semirechye and the adjacent upland Turgen Valley from local archaeological teams has resulted in the tree-ring study of a new set of 17 AMS radiocarbon dates from crossdated tree rings of seven archaeological occurrences, including two Saka sites (Besshatyr-3 kurgan and Turgen II settlement) and three Andronovo sites (Kyzyl Bulak 1 and Asi-7 cemeteries, and Asi I settlement). The new set of calendar dates ranging from 1,200 to 400 cal BC was compared with existing radiocarbon dates of Semirechye archeology derived from carbonized soils, bones, seeds and bulk wood. To accurately date the onset of sedentism due to increased agricultural development and the increase in mobility due to the spread of pastoralism in the region, site stratigraphy and archaeological context at dated cemeteries were compared with radiocarbon dates from multi-component settlements. Spatial and temporal distribution of a large number of radiocarbon dates from the Semirechye attributed to population dynamics, cultural development and environmental change of the transition is discussed. Although the new 14C-set determines the calendar age of Saka tsars’ kurgans in the Ili Valley and significantly improves the Bronze-Iron Age chronology of Semirechye, the question of whether sedentism is a subsequent independent phenomenon or part of an agro-pastoralist economy can only be answered through continued refinement of a regional chronological framework.

References1. Frachetti M., A. Mar’yashev, 2007. Long-term occupation and seasonal settlement of Eastern Eurasian

pastoralists at Begash, Kazakhstan. Field Archaeology 32: 221-42.2. Chang C., Benecke N., Grigoriev F., Rosen A.M., P.A. Tourtellotte, 2003. Iron Age society and chronology in

south-east Kazakhstan. Antiquity 77: 298–312.

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SESSION 9

RADIOCARBON AND ARCHAEOLOGY OF THE AMERICAS AND OCEANIA: IMPROVING

CHRONOLOGIES AND THEORETICAL INSIGHTS

ConvenersN. Beavan (NZL), T. Dillehay (USA), N. Sanz (UNESCo)

DescriptionThe session calls for papers on radiocarbon applications to improve chronologies or contribute to current theoretical debates. The symposium will focus on several major themes related to the Americas (North America, Mesoamerica, South America, the Caribbean) and to Oceania (Australia, New Zealand, Micronesia, Melanesia, and Polynesia):1) the establishment or re-evaluation of regional chronologies via conventional and/or AMS 14C dating, especially in South America;2) correlating radiocarbon dated archaeological patterns and environmental events;3) recent research on human migrations, dispersal of commensal animals or culturally significant floras, and4) the timing of cross-cultural contacts and cultural transitions.

Keywordscultural history, migration, chronologies, contexts

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S09-INV-01

THE WORLD HERITAGE THEMATIC PROGRAMME, HUMAN EVOLUTION: ADAPTATIONS, DISPERSALS AND SOCIAL DEVELOPMENTS (HEADS)

SANZ N.

UneSco, PaRIS, fRance

AbstractThe World Heritage Thematic Programme, Human evolution: adaptations, Dispersals and Social Developments (HEADS) was initiated in the framework of the Global Strategy for a Representative, balanced and credible World Heritage list, in recognizing that sites related to early human origins are under-represented on the World Heritage List. As UNESCO HEADS programme coordinator I would like to present the results of the Action Plan focused on the early prehistoric sites in Latin America and Caribbean region.Its focus lies in defining and establishing a solid strategy of cooperation and implementation to ensure the future recognition, conservation and study of these vulnerable sites. Tracing back to the earliest ancestors of human lineage 2.6 million years ago, the sites offer insight to the foundations and diversity of human life, experience, and social behaviour, and can include various types of properties such as burial, tool-making, rock art, mining, trade and human settlement, among others.Since its inception in 2008, HEAD’s activities have embodied a strong overarching cooperation between the fields of both culture and science, and have included more than 15 international meetings and the participation of over 80 Member States, 120 international experts, 80 site managers and the Advisory Bodies to the World Heritage convention. HEADS is financed by the Spanish Funds-in-Trust for World Heritage.

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S09-O-02

TOMB 7 AT MONTE ALBAN

TUROSS N.(1), RobleS GaRcIa n.(2)

(1) Harvard University, caMbRIDGe, UnITeD STaTeS;(2) Instituto nacional antropologia e Historia, MeXIco cITY, MeXIco

AbstractIn 1932, Alfonso Caso and coworkers excavated Tomb 7 at Monte Alban, Oaxaca, Mexico. The site of Monte Alban contains one of the early cities of Mexico, and this Zapotec location has been the focus of significant archaeological research since the 1930’s. The material wealth removed from Tomb 7 was substantial, including multiple objects made of gold, jade, turquoise, and obsidian that are now housed in the ex-convent of Santo Domingo in Oaxaca City, Mexico. Based largely on comparisons of the architectural style of Tomb 7 and the material culture of items found in the tomb, including the iconography, it has been assumed that later Mixtec peoples who reused Tomb 7 removed the earlier Zapotec burials.As part of a reexamination of Tomb 7 by INAH, we undertook the first radiocarbon dating of this important New World site, and obtained more than fifty radiocarbon dates from Tomb 7 skeletal material. The picture emerging from both the radiocarbon chronology and associated stable isotopic data present a more complicated picture of tomb use than has been previously assumed.

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S09-O-03

HOW LONG DID PEOPLE AND MEGAFAUNA CO-EXIST IN NEW ZEALAND? RE-DATING THE OCCUPATION OF WAIRAU BAR AND THE EXTINCTION OF MOA (AVES: DINORNITHIFORMES)

HOLDAWAY R.(1), JacoMb c.(2), allenTofT M.(3)(4), oSKaM c.(4), bUnce M.(4), WalTeR R.(2)

(1) Palaecol Research ltd, cHRISTcHURcH, neW ZealanD;(2) University of otago, DUneDIn, neW ZealanD;(3) natural History Museum, coPenHaGen, DenMaRK;(4) Murdoch University, PeRTH, aUSTRalIa

AbstractNew Zealand was the scene of the most recent extinction of a megafauna, for which evidence exists from hundreds of well-dated natural deposits of well-preserved bones and other materials. These confirm the survival of the major megafaunal group, the moa (Aves: Dinornithiformes) into the 14th century CE. Despite the comparative brevity of its human settlement, New Zealand also boasts a copious archaeological record, including sites such as that at Wairau Bar, at the northern end of the South Island, which contain artefacts and evidence of human traditions matching those of the source populations in the central South Pacific. The earliest dated sites contain significant evidence for a period of intense exploitation of moa and other megafauna (primarily pinnipeds), in association with artefacts of the ‘Archaic’ phaseof east Polynesian prehistory. Palynological, macrofossil, and biological evidence points to large-scale deforestation of the drier areas of both main islands during the first century or so of Polynesian settlement of New Zealand.Despite the advantages of low geologic age, abundance and state of preservation of natural and archaeological materials, and a history of application of radiocarbon and other dating technologies, the chronologies of both Polynesian settlement and moa extinction remain controversial. The controversy results partly from the ambiguity of most if not all of the 14C ages for the period of moa hunting which coincided with the major fluctuation in the terrestrial calibration curves in the 14th century CE, but also because of the dependence of the ‘Archaic’ chronology on marine-sourced materials.We provide a new integrated chronology for the period of interaction of Polynesian settlers and moa in New Zealand. This revised chronology is based on Bayesian analyses of >250 AMS 14C ages on bone gelatin from moa from natural sites, and of suites of AMS 14C ages on moa eggshell (including recalibration of previously published data) from Wairau Bar, South Island, a first settlement site on the South Island, using the SHcal04 calibration curve. We underpin the chronology with a revised date for the Kaharoa tephra, which pre-dates all known archaeology in New Zealand, based also on the SHcal04 curve. The evidence supports a more recent settlement of New Zealand in the first half of the 14th century CE rather than the late 13th century or earlier, followed by extinction of all South Island moa populations before 1,450 CE. Polynesians enjoyed moa as an abundant source of food and fresh material for tools for at most 60 years, and the total period of co-existence of human settlers and terrestrial megafauna, at a maximum of 120 years, is the briefest known.

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S09-O-04

RADIOCARBON DATING OF OLD SITES IN BRAZIL: A DISCUSSION ABOUT THEIR VALIDITY?

FONTUGNE M.

laboratoire des Sciences du climat et de l’environnement, UMR1572 cnRS, cea, UVSQ, GIf SUR YVeTTe, fRance

AbstractPrehistory of Brazil offers a wide variety of cultures spread across its vast territory. Using technological convergences with old world lithic or bone tools, as well as some apparent similarities of graphic shapes in rock art would be misleading. Then, a lot of questions remain unanswered: where and when did the first settlements in the New World occur? Are the cultural phases due to local migration or arrival of new populations. Thus, one of the first priority was the establishment of an absolute radiocarbon chronology for these settlements and the different stages of development of these cultures. Since more than forty years, French/Brazilian teams point out to the existence of early settlements in Brazil: in Piaui the sites in Parque Nacional Serra da Capivara, Toca do sitio do Meio (12-14 ka) Caldirao dos Rodriguez (18.6 ka) Toca do Sitio do Meio (8-25.2 ka) and Barra do Antoniao with human remains at around 10ka, Boqueiro do sitio da Pedra Furada (5 to ≥52 ka) and recently at the site of Vale da Pedra (20 ka); in Mato Grosso, Santa Elina site (2-10 and 25 ka) and in Minas Gereis the site of Lapa Vermelha IV (3 to 15.3 ka) with the Luiza woman skeleton. These results are presented and discussed taking in account their archaeological context.

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SESSION 10

OCEANIC PALAEOCLIMATOLOGY AND PALAEOCEANOGRAPHY

ConvenersN. Frank (FRA), H. Haflidason (NoR), A. Ingalls (USA)

DescriptionThe distribution of 14C both in the ocean and in the atmosphere has fluctuated on decadal to millennial time scales. A better understanding of the behavior, variability, processes and occurrence of 14C in both the present and the past ocean is important for using 14C as an instrument for radiometric dating or as a tracer for reconstructing the past ocean circulation. Over the last decade increasing attention has been drawn to the spatial and temporal variability of marine radiocarbon reservoir ages and their implications for the correction and calibration of marine sediments. The need for new and more accurate estimates of marine radiocarbon reservoir effects and a better understanding of the processes influencing them has been heightened by the increasing number of very high-resolution marine records from various oceanographic regions. Improvements in instrumentation and analytical technique have resulted in an increasing interest in and application of 14C as a circulation tracer. The issues we propose to address in this session include geological and oceanographic processes related to the exchange of atmospheric radiocarbon with the surface and deep-ocean, application of 14C as a tracer for paleocirculation and the application of 14C in association with trace elements. The session intents to bring together paleoceanographers, oceanographers, atmospheric scientists, physicists and biologists using radiocarbon for a wide range of studies regarding mixing and exchange processes between the atmosphere and ocean and within the ocean.

Keywords14C as a chronometer, 14C tracer of past circulation (more than 1000 yrs), 14C associated with trace elements

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S10-O-01

INTERHEMISPHERIC GRADIENT OF ATMOSPHERIC RADIOCARBON REVEALS NATURAL VARIABILITY OF SOUTHERN OCEAN WINDS

RODGERS K.

Princeton University, aoS Program, PRInceTon, nJ, UnITeD STaTeS

AbstractTree ring Δ14C data (Reimer et al., 2004; McCormac et al., 2004) indicate that atmospheric Δ14C varied on multi-decadal to centennial timescales, in both hemispheres, over the period between AD 950 and 1830. The Northern and Southern Hemispheric Δ14C records display similar variability, but from the data alone it is not clear whether these variations are driven by the production of 14C in the stratosphere (Stuiver and Quay, 1980) or by perturbations to exchanges between carbon reservoirs (Siegenthaler et al., 1980). As the sea-air flux of 14CO2 has a clear maximum in the open ocean regions of the Southern Ocean, relatively modest perturbations to the winds over this region drive significant perturbations to the interhemispheric gradient. In this study, model simulations are used to show that Southern Ocean winds are likely a main driver of the observed variability in the interhemispheric gradient over AD 950–1830, and further, that this variability may be larger than the Southern Ocean wind trends that have been reported for recent decades (notably 1980–2004). This interpretation also implies that there may have been a significant weakening of the winds over the Southern Ocean within a few decades of AD1375, associated with the transition between the Medieval Climate Anomaly and the Little Ice Age. The driving forces that could have produced such a shift in the winds at the Medieval Climate Anomaly to Little Ice Age transition remain unknown. Our process-focused suite of perturbation experiments with models raises the possibility that the current generation of coupled climate and earth system models may underestimate the natural background multi-decadal- to centennial-timescale variations in the winds over the Southern Ocean.

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S10-O-02

BOMB RADIOCARBON AT THE SOURCE: CORAL Δ14C FROM ENEWETAK ATOLL

FALLON S., noRMan R.

The australian national University, acTon, aUSTRalIa

AbstractThe seasonal Δ14C history of surface waters in and around Enewetak Atoll (RMI) in the tropical western Pacific has been reconstructed from radiocarbon measurements on a Porites coral. Enewetak Atoll was a major nuclear test-site during the 1940-50s and this is the first coral-radiocarbon record produced in such proximity to a nuclear test site. We will present Δ14C data from the pre-bomb (-60‰) to 1984 encompassing the bomb testing period. Individual bomb tests can be differentiated as well as the cumulative effect of multiple tests. The largest Δ14C value in the coral came from the 1957 Oak test (34,840‰). The Oak test site was located ~2km west from the coral site. The coral did not display any growth effects from the nuclear bomb tests.

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S10-O-03

LAST DEGLACIATION CHANGES IN Δ14Catm AND ATMOSPHERIC PCO2 AND THE DEEP GLACIAL CARBON OCEAN RESERVOIR

MARIOTTI V.(1), PaIllaRD D.(1), boUTTeS n.(1)(2), RocHe D.M.(1)(3), boPP l.(1)

(1) laboratoire des Sciences du climat et de l’environnement, GIf-SUR-YVeTTe, fRance;(2) ncaS-climate, Department of Meteorology, University of Reading, ReaDInG, UnITeD KInGDoM;(3) earth & climate Department, faculty of earth and life Sciences, Vrije Universiteit, aMSTeRDaM, neTHeRlanDS

AbstractΔ14Catm has changed during the last deglaciation, decreasing from 420±80‰ at the Last Glacial Maximum (LGM) to 0‰ at modern times (INTCAL09). How can we explain such a decrease? Δ14Catm is a function of two terms: the cosmogenic production term and a term linked to the carbon cycle - the exchange of carbon atoms between the atmosphere and the other superficial carbon reservoirs, ocean and continental biosphere. 10Be-based reconstructions show a contribution of the cosmogenic production term of only 200±200‰ at the LGM. The remaining 220‰ of Δ14Catm variation between the LGM and modern times have thus to be explained by changes in the carbon cycle. Containing around 90% of the carbon of the superficial reservoirs, the ocean seems to be the best reservoir to induce such a decrease of Δ14Catm on millennial time scales.Recently, Bouttes et al (2010) proposed the “sinking of brines” mechanism to explain most of the difference in atmospheric pCO2 between glacial and interglacial times. The sinking of brines induces the formation of very saline water masses that store Dissolved Inorganic Carbon (DIC) in the deep ocean. During glacial times, this sinking of brines is enhanced and more DIC is buried in the deep ocean, lowering the atmospheric pCO2. This mechanism could also explain the reduction of Δ14Catm through the deglaciation, as the deep saline waters from the sinking of brines are very old, thus with a low signature in Δ14C. Evidence of such 14C-depleted deep waters during the LGM has recently been found in the Southern Ocean (Skinner et al., 2010). The degassing of this carbon with low Δ14C would then reduce the Δ14Catm during the deglaciation.We have further developed the CLIMBER-2 model to include the cosmogenic production term of 14C as well as an interactive atmospheric 14C reservoir. We investigate the role of both the sinking of brine mechanism and the cosmogenic production rate at explaining the changes in Δ14Catm during the last deglaciation.

References1. .J. Reimer et al., IntCal09 and Marine09 Calibration Curves, 0-50,000 Years cal BP, Radiocarbon, Vol. 51, Nr.

4, p.1111-1150, 2009.2. Bouttes et al., Impact of brine-induced stratification on the glacial carbon cycle, Climate of the Past, 6, p.575-

589, 2010.3. Skinner et al., Ventilation of the Deep Southern Ocean and Deglacial CO2 Rise, Science, Vol. 328, 2010.

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S10-O-04

VARIATIONS OF RADIOCARBON IN THE EASTERN ATLANTIC SECTOR OF THE SOUTHERN OCEAN OVER THE LAST 40 YEARS

TISNÉRAT-LABORDE N.(1), DelIlle b.(2), boRDIeR l.(1), HaTTÉ c.(3), MoReaU c.(4), PaTeRne M.(1), boYÉ M.(5), SPeIcH S.(6)

(1) laboratoire des Sciences du climat et de l’environnement/IPSl, cea-cnRS-UVSQ, GIf-SUR-YVeTTe, fRance;(2) Unité d’océanographie chimique, Interfacultary for Marine Research, Université of liège, lIÈGe, belGIUM;(3) laboratoire des Sciences de l’environnement Marin, UMR 6539, Institut européen de la Mer, GIf-SUR-YVeTTe, fRance;(4) laboratoire de Mesure du carbone 14, UMS 2572, cea Saclay, GIf-SUR-YVeTTe, fRance;(5) laboratoire des Sciences de l’environnement Marin, UMR 6539, Institut européen de la Mer, PloUZanÉ, fRance;(6) laboratoire de Physique des océans, UMR 6523, Université de bretagne occidentale, bReST, fRance

AbstractThe Southern Ocean plays an important role in the Earth’s climate system with its large productivity belt and vigorous circum Antarctic circulation patterns. However, our knowledge of temporal evolution of the Southern Ocean circulation including its carbon redistribution is poorly constrained by in situ observations in this vast remote region. Here, we used radiocarbon measurements of Dissolved oceanic Inorganic Carbon (DIC) in order to provide powerful means to describe and quantify the movement of the water masses as well as the uptake of anthropogenic CO2. We investigated the spatio-temporal variability of radiocarbon in the Southern Ocean during the last 40 years.Recent radiocarbon measurements were performed on DIC of five depth profiles off the Southwestern of Africa coast between 33.58°S 17.14°E towards 57.33°S 00.02°W obtained during Bonus-Goodhope cruise in 2008. We compare these results with those obtained from earlier cruises, GEOSECS and WOCE-France CIVA1. Within surface waters, observed 14C gradients between north and south are consistent with previous observations. However, the absolute values of Δ14C are slightly depleted compared to previous studies most likely reflecting the decrease of bomb 14C in the atmosphere, the northward displacement of surface waters and replacement by old deep waters upwelled at the Antarctic Divergence. Our observation of arrival of deep waters is consistent with the observed oversaturation in CO2 of subsurface waters compared to the atmosphere and the depleted δ13C signature of DIC. In contrast, within the deep ocean, we observe a basin scale dramatic fall of Δ14C values since the early 1970s, which may reflect strong invasion of 14C depleted Pacific Deep Waters into the Circumpolar Deep Water (CDW). The origin of this remarkable replacement of water masses may be attributed to atmospheric climate dynamics over the last 40 years or may reflect other ocean interior processes.

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S10-O-05

IS THE ATMOSPHERIC RADIOCARBON ANOMALY DURING THE MYSTERY INTERVAL (17.5 TO 14.5 KYR BP) AN ARTIFACT OF CALIBRATION? EVIDENCE FROM BARBADOS CORALS

MORTLOCK R.(1), abDUl n.(1), WRIGHT J.(1), cao l.(2), faIRbanKS R.(1)

(1) Rutgers University, PIScaTaWaY, UnITeD STaTeS;(2) Morehouse School of Medicine, aTlanTa, UnITeD STaTeS

AbstractA reconstruction of atmospheric radiocarbon (IntCal09) from various archives records a 190‰ decrease in Δ14C during the Mystery Interval (17.5 to 14.5 kyr BP). It has been suggested that the decrease results from the injection of 14C depleted waters during the deglacial. Supporting evidence comes from benthic foraminifera in sediment cores off Baja, CA that record a 300‰ decrease in the 14C content of intermediate waters at the same time ice core records display an increase in atmospheric CO2 and from the Arabian Sea where records suggest the release of 14C depleted deep waters during the last deglaciation.We have generated a record of atmospheric Δ14C for the period 7.3 to 27 kyr BP using 190-paired radiocarbon and U-series dated surface corals from Barbados Drill Cores. A unique advantage to using the fossil coral archive is that both radiocarbon and calendar ages are obtained from the same sample, whereas atmospheric 14C reconstructions generated from deep sea core microfossils require assigned calendar ages which are based on proxies correlated to ice cores or speleothems and are subject to proxy interpretations, correlation errors, and uncertainties in the imported chronologies. Unfortunately, small inaccuracies in the estimated calendar ages lead to large Δ14C errors. Our coral record adds 40 new 14C and U-series calibration data to the Mystery Interval, previously constrained by only 4 data between 15 and 17.5 ka. The resulting coral radiocarbon calibration record permits an independent estimate as to the timing, duration, and magnitude of the decrease in Δ14C during the Mystery Interval.We observe a break in the decreasing trend of Δ14C around 20 ka. From 20 to 18.5 kyr BP Δ14C values increases by about 100‰ to a maximum value of about 430‰. Δ14C decreases to 300‰ by about 17 ka at which time the long-term decreasing trend in Δ14C is re-established and continues to about 14.5 ka to values of ~ 230‰. Thus, the rapid decrease in atmospheric Δ14C recorded by Barbados corals precedes the Mystery Interval and coincides with only a very small (< 10 ppmv) rise in atmospheric CO2.When compared with the Marine09 curve, Barbados data are offset by as much as 800 years from 17.5 to 15 kyr BP. These age differences are too large to be attributed to reservoir age changes. We attribute the offsets in age (and calculated Δ14C) to inaccuracies in the transferred time scale (Hulu Cave) to the non-varved Cariaco Basin sedimentary (reflectance) record. While precisely dated, high-resolution records from deep-sea cores provide significant contributions to consensus calibration curves, the Barbados record argues that only independently dated records provide the necessary tests of accuracy. Regrettably, much of what has been published or debated about the Mystery Interval may have been based on inaccurate radiocarbon calibration.

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S10-O-06

ASSESSING WITH RADIOCARBON THE U-TH DATING METHOD APPLIED TO SEDIMENTARY ARAGONITE

SEPULCRE S.(1)(2), DeScHaMPS P.(1), baRD e.(1)

(1) centre européen de Recherche et d enseignement en Géosciences de l environnement ceReGe, UMR 6635, Université aix-Marseille, cnRS, collège de france, IRD europôle arbois, bP80, 13545 aIX-en-PRoVence, fRance;

(2) now at laboratoire des Interactions et Dynamique des environnements de Surface IDeS, UMR 8148, cnRS, Université de Paris Sud 11, bat 504, 91405 oRSaY, fRance

AbstractAbsolute chronologies of past climate changes are a clue to understand the processes involved in glacial-interglacial cycles. In paleoclimatic research, the chronological framework is often given by the radiocarbon 14C method. Uranium-thorium (U/Th) dating can extend the 14C chronologies and has enabled accurate and precise dating of past sea-level highstands (corals: [1]; speleothems: [2]).In this work, we are testing an approach based on aragonite-rich sediments from a tropical carbonate platform [3]. These sediments (core MD032628, 17°21N, 77°42W, 846m water depth, Caribbean Sea) are suitable for 14C and U/Th dating (high calcium carbonate CaCO3 content and fine aragonite percent). Moreover, regional paleoclimatic changes have been previously studied over the last 1 Ma [4]. However, U/Th dating of such material is complex because there is some initial 230Th which needs corrections by using isochrons and a possible open-system behavior for the U/Th system [3]. For the most recent time period (≈50 ka),14C dating is useful to check the U/Th ages and to test if the sub-samples are cogenetic and consequently suitable for the isochron method.To obtain cogenetic sub-samples, we separated the CaCO3 minerals (calcite, magnesian calcite Mg-calcite and aragonite) by using heavy liquids on samples from the Holocene, the last deglaciation and the Last Glacial Maximum. The efficiency of the mineralogical extraction was checked by X-Ray diffraction. For each sample, a pure aragonite fraction is obtained in the > 2.85 g.cm-3 density range, and we obtained a Mg-calcite-enriched and a Calcite-enriched sub-samples in the 2.75-2.85 and 2.65-2.75 g.cm-3 ranges, respectively. 14C and U/Th dating were performed on each sub-sample.The most suitable results were obtained for the Holocene pure aragonite sub-sample (H-Arag.). H-Arag. has the highest and lowest 238U and 232Th concentrations, respectively, compared to all other samples and sub-samples for which Th values attest for a contamination (detrital fraction or scavenging). H-Arag. provided an U/Th age of 9.7 ±0.2 (2σ) and of 5.2 ±1.7 (2σ) when corrected from the initial (230Th/232Th). This result is in good agreement with a 14C calendar age of 5.8 ±0.12 cal ka BP (2σ) for H-Arag. It is also close to the bulk fine fraction 14C calendar age of 5.9 ±0.2 cal ka BP (2σ). The difference between a corrected U/Th age lower than the calendar age gives evidence for an α-recoil effect that has to be corrected by modeling [3; 5].The coupling between 14C and U/Th dating was required to test this approach before dating paleoclimatic events from older samples for which only U/Th can be applied (e.g., MIS 5 or 11).

References[1] Bard E. et al., Nature, 346, 456-458, 1990.[2] Bard et al., Earth Planet. Sci. Lett., 196, 135-146, 2002.[3] Henderson G. et al., Geochim. Cosmochim. Acta, 65, 2757-2770, 2001.[4] Sepulcre S. et al., Geochem. Geophys. Geosyst., 10, Q11013, 2009.[5] Thompson et al., Earth Planet. Sci. Lett., 210, 365-381, 2003.

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SESSION 11

CONTINENTAL PALAEOCLIMATOLOGY AND PALAEOHYDROLOGY

ConvenersD. Genty (FRA), L.C.R Pessenda (BRA), H. Wang (USA)

DescriptionThis session addresses multiple issues related to time series for continental palaeoclimatic records and palaeohydrological responses. It focuses on precisely dated continental records that shed light on climatic variability on all continents and its impact on hydrology and vegetation changes. Palaeoclimatic reconstructions from continental carbonates (speleo-thems, travertine, gastropods, ostracods, soils carbonates, calcified roots, etc.), from continental and coastal organic matter (peat, sediment, soil, vegetation, etc.) are welcome. Besides climatic reconstruction, processes involving carbon isotopes (12C, 13C, 14C) and bio indicators (pollen, diatoms, sponge spicules, phytolits, etc.) in above organic archives are welcome.

Keywordsdating, paleoclimatic series, continental carbonates, speleothem, travertine, gastropod, ostracods, calcified roots, rhizoliths, organic matter, soil, vegetation, (paleo) climate, (paleo) hydrology

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S11-O-01

POSSIBLE CORRELATIO BETWEEN RADIOCARBON REGIONAL OFFSET IN JAPAN AND EAST ASIAN MONSOON

IMAMURA M.(1), oZaKI H.(1)(2), SaKaMoTo M.(1), IToH S.(3), MITSUTanI T.(4)

(1) national Museum of Japanese History, SaKURa, JaPan;(2) The University of Tokyo Museum, ToKYo, JaPan;(3) Paleo-labo Inc. ltd., KIRYU, JaPan; (4) national Research Institute for cultural Properties, nara, naRa, JaPan

AbstractRadiocarbon dates measured for Japanese tree-rings have been demonstrated to be consistent with the INTCAL datasets within quoted errors in most periods of 10c. BC to 8c. AD (Sakamoto et al., 2003; Ozaki et al., this conference). However, deviations from INTCAL or regional offsets up to ~70 14C years have also been identified for tree-rings in the period of 1~3 centuries AD (Ozaki et al., this conference) .In this paper, we discuss the 14C regional offsets between 245 BC to AD 400 obtained for dendro-dated Japanese trees (cedar and cypress from central Japan), and point out that a close relationship exists between the 14C regional offsets in Japan (138~139°E 35°N) and the climatic proxy data from Shihua Cave (116°E, 39°N) near Beijing by Tan et al. (2003) who reported a 2650-years Beijing warm season (MJJA) climatic proxies using annually resolved thickness variations of stalagmite. When two time-series curves are compared between 240 BC to AD 400, a general correlation of wiggles is found between two curves. Large offsets tend to occur when proxy data (temperature and/or precipitation) is substantially high, particularly in the periods of 1~AD200. On the other hand, smaller offsets in order of ~20 14C-years seem to persist when the proxy data is lower than some threshold value.These observations may be explained if increased East Asian summer monsoon contributed to the increase of regional offsets in Japanese trees as well as the Beijing summer temperature and/or precipitation. We discuss possible causes of the observed regional offsets in relation to climatic changes in East Asia.

References1. Sakamoto et al., Radiocarbon, 45, 81-89, 2003.2. Tan et al., Geophys. Res. Letters, 30, 1617-1620, 2003.3. Tan et al., 2003, IGBP PAGES/World Data Center for Paleoclimatology Data Contribution Series # 2003-050.

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S11-O-02

USING REPORTED δ13C VALUES FROM RADIOCARBON DATES TO CALCULATE Δ13Cp RATES FOR TERRESTRIAL PALEOCLIMATE ANALYSIS

DRAKE B.L.

University of new Mexico, albUQUeRQUe, UnITeD STaTeS

AbstractC3 plants are characterized by highly variable δ13C values. A model for photosynthetic discrimination in C3 plants was developed by Farquhar and colleagues (1982) to analyze whole plant processes in the same terms as chemical processes:

Δ13Cp = ap + (bp - ap) ci/ca = (δ13Ca - δ13Cp)/(1+ δ13Cp/1,000)

where δ13Ca defines atmospheric δ13C values, δ13Cp defines the isotopic carbon product of photosynthesis, ap is change brought by diffusion of δ13C (4.4‰), bp is the effect of Ribulose-1,5 -biphosphate carboxylase oxygenase (RuP2) (27‰), and ci/ca the ratio between the CO2 partial pressure in the intercellular leave space and atmosphere, respectively. The fractionation process is driven in part by changes of the carbon source (δ13Ca) and limitations in water availability. The resulting discrimination value (Δ13Cp) directly expresses the results of plant photosynthesis, whereas raw δ13Cp records source (atmospheric) concentration and plant biological processes. Just as stomatal closure reduces carbon intake and increases the incorporation of 13CO2 in plant tissues, it will also increase the incorporation of 14CO2 in the same tissues; Farquhar and colleagues estimate that this rate can be calculated by doubling the value ap and multiplying the value bp by 1.9, in addition to factoring in the lower concentrations of 14CO2.Recent research has shown that Δ13Cp rates in C3 plants vary due to mean annual precipitation (Diefendorf et al. 2010). C3 plants in arid regions are more conservative with water; this is reflected in Δ13Cp rates. When many samples are aggregated together, they can produce a representative Δ13Cp value that demonstrates changes in regional water availability. A radiocarbon-dated pollen sequence from Lake Voulkaria in Greece had Δ13Cp rates calculated from reported δ13Cp values. This sequence corresponded well with a record of paleo-rainfall from Soreq Cave in Israel, with a decline in precipitation and Δ13Cp rates at the end of the Bronze Age and increases in both during the Roman Warm Period (Drake 2012).As δ13Cp values from radiocarbon dated charcoal and pollen samples are normally reported with dates (Stuiver and Polach 1977), they have the potential to provide a valuable paleoclimate record when calculated as Δ13Cp rates. This data can be useful to archaeologists and other professionals.

References1. Diefendorf, A., Mueller, K., Wing, S., Koch, P, and Freeman, K., (2010) Global patterns in leaf δ13C

discrimination and implications for studies of past and future climate. Proceedings of the national academy of Sciences 13, 5738-5743

2. Drake, B.L. (2012) The influence of climatic change on the late Bronze Age Collapse and the Greek Dark Ages, Journal of archaeological Science, In Press

3. Farquhar, G., O’Leary, M. and Berry, J. 1982. On the relationship between carbon isotope discrimination and intercellular carbon dioxide concentration in leaves. australian Journal of Plant Physiology 9, 121-137

4. Stuiver, M., Polach, H.A., (1977) Reporting of 14C data, Radiocarbon 19(3), 355 - 363

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S11-O-03

PALAEOCLIMATIC RECONSTRUCTION BASED ON STATISTICAL ANALYSIS OF RADIOCARBON DATES - AN EXAMPLE FROM POLAND

MICHCZYNSKA D.J.(1), STaRKel l.(2), MIcHcZYnSKI a.(1), PaZDUR a.(1), KRaPIec M.(3), MaRGIeleWSKI W.(4), nalePKa D.(5)

(1) Silesian University of Technology, Institute of Physics - cSe, GlIWIce, PolanD;(2) Institute of Geography and Spatial organization PaS, KRaKoW, PolanD;(3) aGH, University of Science and Technology, faculty of Geology, Geophysics and environmental Protection, KRaKoW, PolanD;(4) Institute of nature conservation PaS, KRaKoW, PolanD; (5) W. Szafer Institute of botany PaS, KRaKoW, PolanD

AbstractOur research shows that analysis of frequency distributions of big sets of calibrated dates is helpful in reconstruction of palaeoclimatic changes, especially in estimation of chrono-stratigraphic boundaries. It is based on a few thousand of radiocarbon dates for samples from the Late Glacial and Holocene (dated mainly in Gliwice Radiocarbon Laboratory).Samples were divided into the following subsets:- Samples connected with changes in the fluvial regime (mainly floods)- Samples from landslides and minerogenic horizons- Peat, mud or gyttja samples from tops and bottoms of layers with taking into account different orders of layers and types of sediments (lake, alluvial etc.)For each set probability density functions (PDFs) were constructed by calibration of individual dates and summing up received distributions (Bronk Ramsey, 2010; Reimer et al., 2009).Received results have been compared with available global and regional palaeoenvironmental records. Characteristic feature is that changes in hydrological regime are especially well expressed by sharp begin. Among the most discussed problems are where to put the two boundaries: Eo-Mesoholocene and Meso-Neoholocene considering both factors: temperature and humidity.The first chrono-climatostratigraphic limit was put at about 9600 cal BP. In reality it is two-fold limit. At about 9600 cal BP together with a rapid melting of Laurentide ice sheet was created a free way for westerlies and humid air masses expanded over Europe and Siberia with heavy rains and floods as well with Atlantic forest species. But the real start of warm period reflected in calcareous precipitation and reign of Quercetum mixtum followed one millennium later.The border between Meso- and Neoholocene has also a complex character. It was put at about 4850 cal BP. But earlier, about 5600 cal BP it followed a first distinct cooling and wetter phase, reflected in avulsions of river channels, formation of new landslides – being synchronous with first post-optimum phase of glacial advances in the Alps. However several centuries later started a general rebuilding of ecosystems initiated by rise of humidity and cooling registered in rise of groundwater level and transitional descend of Picea excelsa to lower elevations, later followed be expansion of fagus and abies.The research project is financially supported by the grant N° N306 034040.

References1. Bronk Ramsey C et al., 2010. Radiocarbon 52(3): 953-961.2. Margielewski W, 2006. folia Quaternaria 76: 144pp.3. Michczynska DJ, Pazdur A, 2004. Radiocarbon 46(2): 733-744.4. Michczynska DJ, Michczynski A, Pazdur A, 2007. Radiocarbon 49(2): 799-806.5. Reimer PJ et al., 2009. Radiocarbon 51: 1111-1150.6. Starkel L. Soja R, MichczyСska DJ, 2006. caTena 66: 24-33.7. Starkel L, Michcznska DJ, Krapiec M, Margielewski W, Nalepka D, Pazdur A, 2012. Geochronometria, in print

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S11-O-04

HOLOCENE VEGETATION DYNAMICS TROPICAL ATLANTIC FOREST - GRASSLAND ECOTONE AT NORTHERN ESPIRITO SANTO STATE, SOUTHEASTERN BRAZILIAN COAST

PESSENDA L.C.R.(1), bUSo JR a.a.(1), boRoTTI fIlHo M.a.(1), PaSSaRInI JR J.R.(1), SIQUeIRa G.(2), ScHIaVo J.a.(3), lIMa f.T.W.(1), cHeRKInSKY a.(4)

(1) cena/USP, PIRacIcaba, bRaZIl;(2) Vale natural Reserve, lInHaReS, bRaZIl;(3) Mato Grosso do Sul State University, aQUIDaUana, bRaZIl;(4) University of Georgia, aTHenS, UnITeD STaTeS

AbstractBased on an interdisciplinary study, the objectives of the present work were to study the vegetation dynamics among tropical Atlantic forest and grassland (nativo) vegetation and to infer climate changes during the Holocene, at Vale Natural Reserve (19°00’S - 19°15’S and 39°50’W-40°05’W), northeastern region of Espirito Santo State, southeastern Brazil. The materials and respective analyses were:

(i) modern vegetation (botanic identification, δ13C);

(ii) soil organic matter (total organic carbon, δ13C and 14C dating of the humin fraction).

The sampling points are located at tropical rainforest vegetation dominance, with trees of up to ~50 meters height and growing in not flooded terrains (“Terra Firme” trees) and covering the Ultisols, a clayey, nutrient poor and well drained soils. In the natural grassland fragments there is an association with the Spodosols, sandy and poorly drained soils due to the presence of a cementation layer, generally flooding during the rainy season. The δ13C of native plants in grassland sites indicate ~95 % predominance of C3 grasses and herbs and ~5% of C4 grasses. The C isotope values in the soil organic matter at forest and grassland sites suggest a general predominance of C3 plants since at least ~8000 cal yr BP. The main conclusions were:

(i) forest retreatment and grassland expansion were not observed during the late to mid Holocene dry period, aspects recorded in southeastern, northeastern and in the southern Brazilian Amazonia regions

ii) The soil (Spodosol), associated to the humidity in the studied period, was a significant factor for the maintenance of the grassland-tropical Atlantic Forest ecotone equilibrium.

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S11-O-05

RECOVERING NOVEL ∂13C AND RADIOCARBON RECORDS FROM ORGANIC MATTER PRESERVED IN SPELEOTHEMS

BLYTH A.(1), SMITH c.(2), HUa Q.(3)

(1) curtin University, PeRTH, aUSTRalIa;(2) la Trobe University, MelboURne, aUSTRalIa;(3) anSTo, SYDneY, aUSTRalIa

AbstractSpeleothems form excellent archives of environmental change as they are easy to date and preserve multiple environmental records. However, although the stable isotopic composition of speleothem calcite is well characterised, the potential of the isotopic composition of organic molecules preserved in speleothems has not been investigated in depth. The approach has considerable potential value in providing isotopic records directly linked to particular parts of the overlying ecosystem. For stable carbon isotopes, this will provide records independent of those in calcite records, and enable identification of the primary controls (vegetation type, climate, soil conditions) on the bulk signal. Radiocarbon analysis of the different fractions of organic matter in speleothems has the potential to provide data about relative lags, and OM turnover, especially when used in conjunction with U-Th dating of the calcite. The detailed measurement of isotopic records in speleothem organic matter has previously been hindered by methodological constraints, including extraction of sufficient material, and recovery without adding unquantifiable carbon contamination. However, here we are able to present methodological and time-series data demonstrating how these obstacles may be overcome.A primary analytical need is a rapid and efficient technique to analyse stable carbon isotopes on speleothem organic matter in order to assess relationships between inorganic and organic 13C records, and identify areas of interest for more detailed radiocarbon and compound specific organic analysis. To address this we have developed a new approach utilising liquid chromatography – mass spectrometry (LC-IR-MS), which provides precise organic stable carbon isotope measurements at calcite sample sizes of under 100 mg. This has the added advantage of enabling organic matter analysis in speleothems to match the temporal resolution provided by inorganic analyses for the first time.Radiocarbon analysis of bulk stalagmite material is an increasingly established technique, and here we demonstrate how this utility can be extended by dating of isolated organic matter, and especially specific organic matter fractions. By comparing dates from specific fractions with the bulk radiocarbon dates, and with the dates of calcite precipitation as derived from U-Th dating, it becomes possible to investigate more detailed lags in the system, especially with reference to vegetation and soil driven palaeoenvironmental records. This is of considerable importance if multi-proxy organic and inorganic records are to be combined into a single intergrated palaeoenvironmental record, and will contribute significantly to understanding any differences in response to climate between carbon and organic records, and those, such as oxygen isotopes, derived directly from the drip water and the stalagmite calcite.

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S11-O-06

THE GEOLOGICAL RECORDS OF “MYSTERY INTERVAL” IN MONSOON CHINA SINCE THE LAST 21KA

ZHOU W.(1)(2)(3), XIan f.(1)(2), lIU Z.(1)(4), ZHU Y.(1)

(1) State Key laboratory of loess and Quaternary Geology, Institute of earth environment, chinese academy of Sciences, XI’an, cHIna;

(2) Xi’an aMS center, XI’an, cHIna;(3) Xi’an Jiaotong University, XI’an, cHIna;(4) Graduate University of chinese academy of Sciences, beIJInG, cHIna

AbstractAs Denton et al. (2006) proposed the “Mystery Interval”(MI)(17.5-14.5 ka), which appeared to be contradictory to the climate shift of the last 100-kaglacial cycle. Broecker et al.(2009, 2010) further documented that the deglacial MI has two distinct hydrologic parts in the western USA and suggested the possible forcing mechanism. Here, we present the multi-proxy climatic records of MI from the Chinese Loess Plateau and its comparison with the Chinese cave records (e.g., Wang et al., 2001,2008; Cheng et al., 2009), the climatic archives from the Northern high latitude and (e.g., Johnson et al., 2001; McManus et al., 2004) the Southern high latitude (e.g., Monnin et al., 2001), the most striking features of the “Mystery Interval” can be broadly summarized as, the asynchronous structure of Northern high latitudes climatic changes such as the decreased North Atlantic meridional over turning circulation (e.g., McManus et al., 2004) and the extensive glacier recession in Swiss Alps (e.g., Denton et al., 2006), the weakening monsoon in mid-latitude China (e.g., Wang et al., 2001) and the rapid warming in Antarctic (e.g., Monnin et al., 2001).The Asian Monsoon intensity derived from the studied records is characterized by severe cold and dry features (e.g., Wang et al., 2001; Zhou et al., 2007), which is apparently different with the continued strengthening temperature or CO2 increase in the Southern high latitudes. After detailed comparison analysis on longer time-scales, it clearly shows that the Asian Monsoon records closely follow the insolation changes, if without the Mystery Interval(MI) and the Younger Dryas (YD) events. Although the MI and YD were similarly linked to the expansion of North Atlantic sea ice (e.g., Broecker et al., 2010), they are possibly in response to the strengthened insolation changes and Bipolar see-saw process (e.g., Broecker,1998; Chylek et al., 2010). As the MI was within the Termination I, its climatic change is more sensitive than YD. The general similarity of the Terminations I and III presented by Asian Monsoon cave records (e.g., Cheng et al., 2009) left us with question that what is mechanism of MI, though the insolation amount during the Terminations I was higher than Terminations III (Berger & Louter., 1991), but why the shutdown from the Heinrich 1 iceberg armada could have had a greater impact than those associated with the five earlier Heinrich armadas. Therefore, the arguments on the MI climatic changes are still debated. It seems that the changes of Asian Monsoon over the MI may basically reflect the teleconnection between the cold air activity of the Northern high-latitude and hydrological cycle from the Southern low latitude. Further studies should be focused on the dynamics of this interval.

AcknowledgementsThis work is jointly supported by the the National Basic Research Program of China and National Science Foundation of China.

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S11-O-07

APPLICATION OF IMPROVED VERSIONS OF 14C AND 230TH/U METHODS FOR DEVELOPMENT OF THE LATE PLEISTOCENE INTERGLACIAL AND INTERSTADIAL CHRONOLOGY OF WESTERN SIBERIA

ARSLANOV K.(1), MaKSIMoV f.(1), KUZneTSoV V.(1), cHeRnoV S.(1), laUKHIn S.(2)

(1) Saint-Petersburg State University, SaInT-PeTeRSbURG, RUSSIan feDeRaTIon;(2) Institute of Problems of Development of the Russian north, Siberian Division Russian academy of Siences, TYUMen,

RUSSIan feDeRaTIon

AbstractThe limiting factor in dating of the Late Pleistocene organic sediments by 14C method is sharp influence of the younger carbon brought to the sample by roots of plants, mobile forms of humic acids, bacteria and fungi. The samples for dating were taken from the deep clearings to except or at least reduce the influence of the younger carbon. More complete extraction of humic acids from organic samples was carried out in laboratory processing of samples. Synthesis of benzene were carried out on the same installation from a series of ancient samples to except of the influence of the memory-effect. Application of the above enumerated measures has allowed us to extend a 14C dating range of the wood and peat samples up to 60 ka BP. We have applied the 230Th/U method for dating of Middle and Late Pleistocene peatbogs. We applied the improved 14C and 230Th/U methods for dating of interglacial peatbog in outerop located close to village Bedoba in the Angara river basin. These sediments have been assignited to Middle Wurm Karginskian Interglacial on the based of series finite 14C dates of peat samples in the range of 29,6-47,0 ka BP. These dates were received in the 1960s-1970s. Our researches haven’t confirmed former underestimated 14C dates: we have received the 14C dates ≥53500 BP and ≥56900 BP for upper- and middle layers of the peatbog in the same exposure. The 230Th/U ages of the middle peatbog layers is equal 120±11 ka. Thus, this peatbog was formed during Kazantsovian Interglacial. We also dated by 230Th/U method the peatbog formed during Kazantsovian Interglacial in the section Shuryshkary in the lower reaches of the river Ob (age 133±14 ka and 141.1±11.7 ka) and in the section Chembakchino in the lower reaches of the river Irtysh (age 114.2+22.1/-14.7 and 110.1+6.7/-8.3 ka). The dates of Kazantsovian Interglacial of Western Siberia can be correlated with the 230Th/U date of Mikulinscian Interglacial on the Russian Plain (age 113±10 ka) and with chronology of substage MIS-5e. The authors also have studied the true Middle Wurm deposits of Western Siberia. We have dated the peatbog thickness 1,8 m, formed during 14C ages range 40,0-48,9 ka BP in an exposure Golden Cape in the lower reaches of the river Ob. Three stages of warming (a condition of northern taiga) and two stage of cooling are revealed according to pollen data on this section. We have dated peat lenses in loams and received 4 dates in the range from 27800±210 BP to 46350±1590 BP in an exposure of Kiryas in the middle reaches of the river Ob. Three stages of warming and two ones of cooling are fixed in this age range according pollen data. Landscapes of forest-tundra and northern taiga existed during the warming periods and conditions of grassy tundra during a cooling stages in this region. Nowadays the Kiryas section is situated in an area of middle taiga.

AcknowledgementsThis research was supported by RFBR (grant № 10-05-01070) and by Government of Russian Federation (grant N° 11.G34.31.0025).

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S11-O-08

WOOD FROM THE SHELTON MASTODON SITE (MICHIGAN): RADIOCARBON AND TREE-RING DATING

LEAVITT S.(1), PanYUSHKIna I.(1), ZaWISKIe J.(2), WIeDenHoefT a.(3)

(1) University of arizona, TUcSon, UnITeD STaTeS;(2) cranbrook Institute of Science, blooMfIelD HIllS, MIcHIGan, UnITeD STaTeS;(3) USDa forest Products laboratory, MaDISon, WISconSIn, UnITeD STaTeS

AbstractCultural history of the Great Lakes region extends back at least 12,000 years, to about the time of North American megafauna extinction. Event chronologies at this time are based heavily on radiocarbon dating of microfossil and macrofossil remains preserved in a variety of different post-glacial environments, but tree rings offer potential to provide dating and assessment of environmental conditions at much finer resolution. Our investigation focused on the Shelton mastodon site (Shoshani et al., 1989) located in Oakland County, Michigan. The primary excavation was conducted between 1984 and 1987 with the recovery of 12 vertebrate species, including the American mastodon and Scott’s moose megafauna. The bone-bearing Shelton forest bed occurs at the base of a well-defined spruce macrofloral zone, containing abundant wood, charcoal fragments, and several in situ tree stumps. Originally reported dates bracket the forest bed between 12,320 ±110 to 11,740 ± 175 14C years BP (Two Creeks age to slightly older). The transition to an overlying pine-dominated zone at the site occurs in bog soils originally dated at 10,020 ± 80 to 9,640 ± 120 14C years BP. The environmental setting for the megafauna was an intermorainal lake with oscillating levels that developed by ponding in glacial channel. Charcoal layers with clastic influx indicate sporadic wildfires occurred in the surrounding spruce forest during transition to the Holocene.We subsampled more than 50 spruce specimens collected from the 1980s excavations. A floating 218-year tree-ring width chronology was constructed with high replication and tree-ring sample depth (35 trees). This tree-ring set appears to be further suitable for a dendroclimatic study. In order to determine precise calendar age of the tree-ring series, 10 AMS radiocarbon dates were obtained from a sequence of 10 decadal groups of crossdated tree rings. Results using several statistical techniques of 14C-wiggling matching of the developed 14C sequence with the calibration curve are compared to identify the best-fit calendar age, and various inferences about timing of events at the site including Clovis culture are discussed.

AcknowledgementsThis work is supported by NSF grant #P2C2-1003483.

References1. Shoshani, J., Fisher, D.C., Zawiskie, J.M., Thurlow, S.J., Shoshani, S.L., Benninghoff, W.S., Zoch, F.H., 1989. The Shelton Mastodon Site: Multidisciplinary study of a Late Pleistocene (Twocreekan) locality in southeastern Michigan. Contributions from the Museum of Paleontology The University of Michigan 27(14): 393-436.

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S11-O-09

VARIABILITY OF RADIOCARBON DATES AND DENDROCHRONO-LOGICAL CYCLICITY OF SPRUCE WOOD FROM MIDDLE PLENIGLACIAL DEPOSITS AT KURTAK (CENTRAL SIBERIA)

DAMBLON F.(1), HaeSaeRTS P.(1), DRoZDoV n.I.(2), cHeKHa V.P.(2), oRloVa l.a.(3), Van DeR PlIcHT J.(4)(5)

(1) Royal belgian Institute of natural Sciences, bRUXelleS, belGIUM;(2) laboratory of archaeology and Palaeogeography of central Siberia, KRaSnoYaRSK, RUSSIan feDeRaTIon;(3) United Institute of Geology, Geophysics and Mineralogy, noVoSIbIRSK, RUSSIan feDeRaTIon;(4) centre for Isotope Research, University of Groningen, GRonInGen, neTHeRlanDS;(5) faculty of archaeology, leIDen, neTHeRlanDS

AbstractWell preserved spruce wood pieces with numerous rings were recovered from a Middle Pleniglacial loess-loam sequence investigated in the site of Kurtak (Central Siberia), close to the Yenisei River. Nice wood remains were found in some 15 successive layers and collected for radiocarbon dating. When combined with pedostratigraphy and palynology they allowed framing 9 positive climatic events between 39 and 27 uncal ka BP on the basis of parallel dates from the Novosibirsk and Groningen laboratories. The concordance of the results was remarkable despite some minor differences for the older dates (Haesaerts et al., 2005, 2010). Five wood pieces from 3 successive layers dated respectivly around 30.0, 30.8 and 32.5 ka BP, show up to 150 narrow tree rings which were counted and measured. The results show strong variations of the rings with a cyclicity of about 10-15 years. In order to control the stability or variability of the radiocarbon dates from each of the pleniglacial wood piece, series of dating have been performed on successive sets of rings (between 12 and 18 samples of about 10 rings) precisely positioned in the ring succession of the five spruce wood pieces. For most of the wood pieces the distribution of the radiocarbon ages shows some wiggles which may be put in relation with the cyclicity of the corresponding tree rings. The reproducibility of such variations has been investigated by a second set of complementary dating performed on a series of 14 samples of adjacent rings taken from one of the best wood sample dated around 32.5 ka BP. The results show the same trend in the dates. The interpretation of such variations in the 14C content of the rings will be discussed.

AcknowledgmentsThe loess research in Kurtak is a contribution to the MO/36/021 research projects of the Belgian Science Policy, with complementary funding from the INTAS 2000-879 research project.

References1. Haesaerts, P., Chekha, V.P., Damblon, F., Drozdov, N.I., Orlova, L.A., van der Plicht, J., 2005. The loess-palaosol succession of Kurtak (Yenisei Basin, Siberia): a reference recor for the Karga Stage (MIS 3). Quaternaire, Paris, 16 (1), 3-24. 2. Haesaerts, P., Borziac, I., Chekha, V.P., Chirica, V., Drozdov, N.I., Koulakovska L., Orlova, L.A., van der Plicht, J., Damblon, F., 2010. Charcoal and wood remains for radiocarbon dating Upper Pleistocene loess sequences in Eastern Europe and Central Siberia. Palaeogeography, Palaeoclimatology, Palaeoecology, 291, 106-127.

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SESSION 12

INSIGHTS INTO THE OCEAN CARBON CYCLE FROM RADIOCARBON MEASUREMENTS

ConvenersE. Druffel (USA), A. mcNichol (USA) , K. Tedesco (UNESCo), N. Tisnérat-Laborde (FRA)

DescriptionRadiocarbon measurements on carbon isolated from all of the reservoirs in the ocean-from bulk pools such as dissolved inorganic (DIC) and dissolved organic (DOC) carbon to individual biomarkers isolated from complex matrices-adds important time and source information to studies of the carbon cycle in the natural environment. The addition of radiocarbon measurements to carbon cycle studies brings critical information for understanding and quantifying the impact of human activity and climate change on the environment. Sensitive environments such as coastal and high latitude regions have complex carbon cycle processes with organic matter inputs from a variety of sources and ages-direct input from primary production, modern and pre-aged terrestrial matter, as well as ancient material. The combination of bulk and compound specific measurements can help sort out the history of carbon deposition in these environments and permit us to make insightful predictions for the future. In the open ocean, tracing the bomb pulse in specific compounds can help to understand the synthesis, degradation and reactivity of complex materials such as DOC. We invite contributions describing studies using radiocarbon to investigate the modern carbon cycle.

Keywordsocean carbon cycle, dissolved inorganic carbon cycling, dissolved organic carbon cycling, compound specific radiocarbon analyses, coastal ocean carbon cycling, pre-aged terrestrial carbon

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S12-O-01

ORIGIN AND SPATIAL DISTRIBUTION OF THE RHôNE RIVER PARTICU-LATE INPUTS IN THE MEDITERRANEAN SEA: NEW EVIDENCES FROM RADIOCARBON MEASUREMENT

CATHALOT C.(1), RaboUIlle c.(1), TISnÉRaT-laboRDe n.(1), ToUSSaInT f.(1), KeRHeRVÉ P.(2), TReIGnIeR c.(1), lanSaRD b.(1), boWleS K.(3), SUn M.Y.(3), TRoncZYnSKI J.(4), PaSToR l.(5)

(1) lSce, cea-cnRS-UVSQ, GIf-SUR-YVeTTe, fRance;(2) cefReM, PeRPIGnan, fRance;(3) Department of Marine Sciences, University of Georgia, aTHenS, UnITeD STaTeS;(4) laboratoire biogéochimie des contaminants organiques, IfReMeR, nanTeS, fRance;(5) lGe, Université Paris VII, PaRIS, fRance

AbstractRivers are natural links between the continent and ocean carbon cycles, as they concentrate most of the delivery of Organic Carbon (OC) from the land to the ocean. River deltas and estuaries, located at the ocean-continent interface, are mostly heterotrophic as they reprocess carbon more than they produce or bury new organic material but this heterotrophy is largely variable in time and space. Processes leading to mineralization or burial are highly dependent on the origin of organic matter and the mode of deposition in the coastal sea.The Rhône River is the major river contributor to the Mediterranean Sea (Ludwig et al, 2003): the delivery of particles shows a large range of origins linked to river hydrology and a potential mix with marine organic matter. A range of deposition conditions drives the degradation, transport and burial processes of organic matter in the Rhône River delta. A better understanding of the nature of the organic fraction, its lability and its distribution on the continental shelf is needed to constrain the reactivity of OC, its residence time and its fate.Two scientific cruises were conducted in June 2005 and April 2007 to study the export and the biogeochemical fate of organic particulate river inputs in the Rhône River delta and its adjacent continental shelf. Sediment and suspended matter were sampled and their organic carbon content was measured together with radiocarbon, stable carbon isotopes and lignin yields (Δ14C, δ13C, Λ6). Stable carbon isotopes of lignin phenols and PAH were also measured.Carbon isotopes and lignin contents show a clear spatial distribution with a decrease of Δ14C values and carbon-normalized lignin contents with the distance from the Rhône mouth. Terrestrial modern material is concentrated at the river mouth, with isotopic signatures similar to the Rhône River ones. A clear gradient in δ13C and Δ14C is visible offshore as heavier and older OC constitutes a large proportion of the organic mix on the continental shelf. PAH and δ13C of lignin phenols rule out a larger fraction of petrogenic carbon or a mix with C4 plants. The offshore trend could be explained by the degradation of young terrestrial particles exported offshore and the transport towards the Rhone prodelta of shelf resuspended particles. Benthic mineralization rates and the clear decoupling between the water column and sediment isotopic signals on the continental shelf indicate a small preservation of marine recent organic matter in surface sediments.

ReferencesLudwig, W., M. Meybeck, et al. (2003). Riverine transport of water, sediments, and pollutants to the Mediterranean Sea. UNEP MAP Technical Report Series. Athens, UNEP/MAP. 141: 111.

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S12-O-02

SOURCES AND CYCLING OF ORGANIC COMPOUND FRACTIONS IN HIGH MOLECULAR WEIGHT DISSOLVED ORGANIC MATTER IN LAKE SUPERIOR: INSIGHTS FROM ∆14C AND σ13C

ZIGAH P.K.(1), RePeTa D.(2), MInoR e.c.(3), McnIcHol a.(4), XU l.(4), WeRne J.(3)

(1) Swiss federal Institute of aquatic Science and Technology, KaSTanIenbaUM, SWITZeRlanD;(2) Department of Marine chemistry and Geochemistry, WHoI, WooDS Hole, UnITeD STaTeS;(3) large lakes observatory & Dept. chemistry and biochemistry, Univ. of Minnesota, DUlUTH, UnITeD STaTeS;(4) noSaMS, WHoI, WooDS Hole, UnITeD STaTeS

AbstractDissolved organic matter (DOM) in the water column of aquatic systems contains different biochemical compound fractions with numerous sources, reactivities, and different formation and diagenetic pathways. In this study we used the natural abundance radiocarbon (Δ14C) and stable carbon (δ13C) isotopes to investigate the sources, ages, and cycling of carbohydrates, amino acids, lipids, and acid-insoluble organic fractions within high molecular weight (HMW) DOM in Lake Superior’s water column. Solvent extractable lipid was relatively 13C-depleted (-29.7‰ to -28.0‰) and persisted much longer (Δ14C of -10‰ to -256 ‰; 20-2320 BP years) than the lake water residence time. Total hydrolyzable carbohydrates (TCHO) had δ13C of -26.9 to -25.8‰, with modern (post-1950) Δ14C values of 20-31‰ reflecting a recent algal and/or terrestrial photosynthetic origin. Δ14C of total hydrolyzable amino acids (THAA) was mostly modern (34-39‰) indicating rapid turnover time and a recent photosynthetic source. Coupled Δ14C and δ13C values indicate multiple sources, and the co-existence of different formation pathways for the acid insoluble fraction in the lake.

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141

S12-O-03

RADIOCARBON SIGNATURES AND CYCLING OF DISSOLVED ORGANIC CARBON IN THE SOUTH PACIFIC AND SOUTH ATLANTIC OCEANS

DRUFFEL E., GRIffIn S.

University of california Irvine, IRVIne, UnITeD STaTeS

AbstractRadiocarbon (Δ14C) measurements of bulk dissolved organic carbon (DOC) in the deep ocean range from -390 per mil in the North Atlantic to -550 per mil in the Northeast Pacific. We report the first Δ14C measurements of DOC collected from five sites in the South Pacific and three sites in the South Atlantic on Repeat Hydrography cruises P6 (2010) and A10 (2011). We will compare our new results with those reported earlier for the North central Pacific, the Northeast Pacific, the Southern Ocean and the Sargasso Sea. We find that the Δ14C results from the deep South Pacific are lower than expected, given the range between Southern Ocean DOC Δ14C values (-500 per mil) and those from the North central Pacific (-525 per mil). We will report results of duplicate seawater samples analyzed for DOC Δ14C that estimates the total uncertainty for DOC 14C measurements.

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142

S12-O-04

DECADAL CHANGES IN THE BOMB-PRODUCED RADIOCARBON IN THE PACIFIC OCEAN FROM THE 1990S TO 2000S

KUMAMOTO Y., MURaTa a., KaWano T., WaTanabe S., fUKaSaWa M.

JaMSTec, YoKoSUKa, JaPan

AbstractIn the 2000s, radiocarbon in dissolved inorganic carbon was measured during revisit cruises along the WOCE (World Ocean Circulation Experiment) lines of P01 (47°N approx., 2007), P03 (24°N approx. 2005), P06 (32°S approx., 2003), P10 (149°E approx., 2005), P14N/C (179°E approx., 2007), P17N (135°W approx., 2001), and P21 (17°S approx., 2009) conducted in the 1990s in the Pacific Ocean. Comparison of radiocarbon data from the 1990s and 2000s revealed decadal changes of radiocarbon concentration in the thermocline, most of which were due to temporal changes in the bomb-produced radiocarbon. Vertical profiles and vertical-integrated inventories of the bomb radiocarbon in the subarctic and equatorial regions have not changed significantly. In the subtropical regions, radiocarbon decreased in upper thermocline from surface to about 500-m depth. In contrast, radiocarbon increased in lower thermocline from about 500-m to 1500-m depths. In the southern and northeastern subtropical regions, the two opposing directions in radiocarbon change resulted in small temporal changes of the total inventory of the bomb radiocarbon. On the other hand, the water column inventory significantly decreased in the northwestern subtropical region because the radiocarbon decrease in the upper thermocline was larger than the radiocarbon increase in the lower one. These decadal changes are primarily due to the meridional transport of the bomb radiocarbon from high latitude into temperate zone. The decrease in the vertical-integrated radiocarbon in the northwestern subtropical region implies that the turnover time of the thermocline circulation in the region is faster than those in the other subtropical regions in the Pacific Ocean.

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143

S12-O-05

UPTAKE AND REDISTRIBUTION OF CARBON DIOXIDE IN THE SOUTHERN OCEAN: INCREASING OR DECREASING?

GUILDERSON T.(1), SWeeneY c.(2), TaKaHaSHI T.(3), loVenDUSKI n.(4), neWbeRGeR T.(2), KeY R.(5), SaRMIenTo J.(5)

(1) lawrence livermore national laboratory, lIVeRMoRe, UnITeD STaTeS;(2) cIReS/University of colorado, boUlDeR, UnITeD STaTeS;(3) lamont-Doherty earth observatory, PalISaDeS, UnITeD STaTeS;(4) InSTaaR/University of colorado, boUlDeR, UnITeD STaTeS;(5) Princeton University, PRInceTon, UnITeD STaTeS

AbstractThrough wind and buoyancy driven circulation the Southern Ocean provides a window into the deep ocean. This window is a conduit for the uptake and or release of carbon dioxide between the deep-ocean and the atmosphere. Future climate change scenarios predict an increasing and very delicate role for the Southern Ocean in controlling the atmospheric fraction of emitted carbon dioxide. Under elevated atmospheric CO2 concentrations model predictions from the 1990s [e.g., Sarmiento et al., 1998] predicted decreased overturning and a reduced uptake of atmospheric CO2 due to increased stratification. More recent model predictions [e.g., Le Quere et al., 2007] imply an increase in mixing due to increased winds and enhanced Ekman transport. The increase in mixing should result in a smaller ΔpCO2 gradient and consequently reduced uptake of CO2. We use radiocarbon of ∑CO2 in surface waters, a sensitive indicator of ocean dynamics and air-sea exchange, to explore these divergent scenarios.During crossing of the Drake Passage samples across and south of the polar front have been collected since 2006. Focusing on winter time observations: ∑14CO2 describe a 70±14‰ decrease in 14C between 1973 (GEOSECS) and post-2006 and a steeper meridional gradient. This has been accompanied by an increase in surface water pCO2. Using an ocean GCM that includes radiocarbon we estimate that ~75% of the observed decrease in surface water 14C is a result of the atmosphere-ocean disequilibrium effect (reduced atmosphere-ocean gradient). The remaining decrease in conjunction with an increase in surface pCO2 that exceeds the rate of increase in the atmosphere over the last 30 years (ie., reduced ΔpCO2) implies that increased upwelling of low-14C, high ∑CO2 water has occurred. These observations appear to support low resolution GCMs which predict a decrease in CO2 uptake in the Southern Ocean due to upwelling of carbon rich waters south of the Polar Front.

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144

S12-O-06

IMPROVED RADIOCARBON CONSTRAINTS ON ABYSSAL CO2 SEqUESTRATION DURING THE LAST GLACIAL PERIOD

SKINNER L.(1), ScRIVneR a.(1), fallon S.(2)

(1) Godwin laboratory for Palaeoclimate Research, University of cambridge, caMbRIDGe, UnITeD KInGDoM;(2) Research School of earth Sciences, australian national University, canbeRRa, aUSTRalIa

AbstractThe explanation of large atmospheric CO2 fluctuations associated with the glacial-interglacial cycles of the late Pleistocene represents an important test of our understanding of carbon cycle dynamics and feedbacks, and may also represent an important step towards an explanation of glacial-interglacial climate variability itself. While it is apparent that changes in the ocean’s capacity to sequester carbon dioxide must have played a key role in these global climate upheavals, the exact mechanisms that made this possible remain unclear. In particular, the contribution of physical ocean mixing/overturning processes versus the contribution of biological export productivity remains a key unresolved question. Here we present marine radiocarbon evidence from various sites around the globe, in an attempt to better constrain the evolution of the marine radiocarbon inventory across the last deglaciation. We show that, although it was heterogeneous, the glacial ocean carbon pool was not as well equilibrated with the atmosphere as it is today, and may have retained as much radiocarbon as is suggested by existing atmospheric radiocarbon calibration datasets. We consider the mechanisms that may have been responsible for the observed changes in deep ocean radiocarbon ‘ventilation’ and their possible impact on atmospheric CO2 in terms of variable ocean interior mixing (as a putative control on water-mass volumes and their homogeneity), and variable sea-ice or salinity stratification in the high latitude Southern Ocean. We use a simple three-layer outcrop-diffusion box-model to explore these processes, and show that the classically explored manipulations of biological export productivity and ocean overturning rates are not the only, or indeed the most effective mechanisms for simulating the deglacial patterns of e.g. CO2, D

14Catm, D14Cocean, δ13Catm and δ13Cocean. Instead

we propose that large changes in the ‘standing volume’ of deep water ventilated from a stably stratified or sea-ice occluded region of the Southern Ocean may represent the most parsimonious explanation for a significant portion of glacial-interglacial atmospheric CO2 (and radiocarbon) change.

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145

SESSION 13

RADIOCARBON AS A TRACER OF SOURCES, FLUXES AND TIME IN CONTINENTAL WATER

ConvenersP. Aggarwal (IAEA), A. Aureli (UNESCo), L. Bouchaou (mAR), J.L. michelot (FRA)

DescriptionThis session is dedicated to the applications of radiocarbon measurements in inorganic and organic, dissolved or particulate, compounds in continental water: surface water (lakes, rivers, estuaries) and groundwater. These applications include the tracing, quantification and modelling of natural and anthropogenic carbon fluxes in continental water, as well as the interpretation of radiocarbon measurements in terms of water dynamics in a reservoir (e.g. water “dating” and its implications on assessment and management of water resources).

Keywordssurface water, groundwater, tracing, dissolved and particular C fluxes, dating, water resources

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146

S13-O-01

VARIATIONS IN SOIL CO2 CONCENTRATIONS AND ISOTOPIC VALUES IN A SEMI-ARID REGION DUE TO BIOTIC AND A-BIOTIC PROCESSES IN THE UNSATURATED ZONE

CARMI I.

Tel aviv university, Tel aVIV, ISRael

AbstractInteractions of biological processes and a-biotic carbonate chemistry affect the isotopic composition of soil CO2 and have implications for groundwater dating and on ecosystems carbon fluxes. These interactions were investigated in the semi-arid Yatir forest in southern Israel (290mm mean annual precipitation), which is characterized by shallow soil overlying a carbonate base rock. PVC tubes for sampling of soil gas, open at both ends, were inserted into the unsaturated zone (USZ) at depths of 30cm, 60cm, 90cm, 120cm, 200cm and 250cm. Profiles of soil gas in the USZ were collected from the tubes five times between October 2007 and September 2008. Measurements of the collected profiles of soil gas included CO2 (ppm), δ13C (‰) and one profile of 14C (pMC). In the uppermost layer (30cm deep) the concentration of CO2 in the soil gas was at least 2 times higher than in surface air (CO2 ~ 390ppm) and the δ13C was lower (about -16‰) than in the atmosphere (~-8‰). 14C (77 pMC) was lower than the atmosphere and the biosphere. Throughout the USZ down to depth of 250cm, the CO2 increased with depth, up to ~9,500 ppm, and the δ13C(‰) became more negative (-17‰ to -21‰, at 250cm depth). Apparently, the main source of CO2 in soil gas is release from the roots. In fall-winter therelease of this biologically-derived CO2 is lowest, increasing in the spring and reaching the highest values in the summer with the δ13C closest to that of a C3 plant. While the main source of CO2 must be at the root zone, it fills up the profile to basis at or below 250cm (data from deeper level is not available). The decrease in CO2 with diminishing depth may be due to two processes: CO2 may be lost from the USZ into the atmosphere and lost due to dissolution into sediment water in the USZ. In the period of high production in the summer δ13C values indicated a mixture of the soil gas with the prevailing atmosphere of the USZ. In the early spring, the 14C (77 to 91 pMC) throughout the profile was lower than both the atmosphere and biosphere (~100 pMC) indicating a contribution of a-biotic carbonate from the sediment (2.8 pMC). These biological/geochemical interactions have implications for the isotopic signal of soil CO2 emitted to the atmosphere or dissolved in soil water to reach groundwater.

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147

S13-O-02

RADIOCARBON DATING OF MODERN GROUNDWATER: THE ROLE OF THE UNSATURATED ZONE

GILLON M.(1)(2), baRbecoT f.(2), GIbeRT e.(2), PlaIn c.(3), coRcHo alVaRaDo J.a.(4), MaSSaUlT M.(2)

(1) UMR UaPV-InRa 1114 eMMaH, Université d’avignon et des pays de Vaucluse, aVIGnon, fRance;(2) UMR cnRS-UPS 8148 IDeS, Université Paris Sud XI, oRSaY, fRance;(3) UMR Ul-InRa 1137 eef, Université de lorraine, nancY, fRance;(4) Institute of Radiation Physics, University Hospital and University of lausanne, laUSanne, SWITZeRlanD

AbstractBiological and physical processes occurring in soils may lead to significant isotopic changes between the isotopic compositions of atmospheric CO2 and of soil CO2. Also, during water and gas transport from the soil surface to the water table, isotopic changes likely occur due to numerous physical processes such as gas production and diffusion, water advection, and gas-water-rock interactions. In most cases, these changes are not included in the correction models developed for groundwater dating, whereas they can significantly impact the calculation of the 14C age (Fontes, 1992; Gillon et al., 2009). We explore the role of these processes using:

i) experimental data from two aquifer sites (Fontainebleau sands and Astian sands, France),

ii) a distributed model to simulate the 14C activities of soil CO2,

and iii) numerical simulations in order to highlight the role of the physical processes.

The 13C content in soil CO2 showed seasonal variations and highlighted the competition between CO2 production and CO2 diffusion. Their respective contributions played a significant role in defining the isotopic composition of CO2 at the water table. On both study sites, variations of the 14C activity in soil CO2 reflect the competition between the fluxes of root derived-CO2 and of organic matter derived-CO2. Since the nuclear weapon tests in the fifties and sixties, soil CO2 became significantly depleted in 14C compared to atmospheric CO2. Models that take into account this 14C depletion in soil CO2 for dating modern groundwater would lead to apparent younger 14C ages than models that only consider the 14C activity in atmospheric CO2. Moreover, since 2000-2005, the inverse effect is observed as soil CO2 is enriched in 14C compared to atmospheric CO2 (Gillon et al., in revision).Therefore, we conclude that the isotopic composition of CO2 at the water table have to be taken into account for the dating of modern groundwater. This requires a systematic sampling of soil CO2 and the measurement of its 13C and 14C contents. We used this information in a numerical simulation to calculate the evolution of isotopic composition of CO2 from the soil surface to the water table. This simulation integrated physical processes in the unsaturated zone (e.g. CO2 production and diffusion, water advection, etc.) and gas-water-rock interactions.

References1. Fontes (1992) Radiocarbon after four Decades, 242-2612. Gillon et al. (2009), Geochim. cosmochim. acta 73, 6488-65013. Gillon et al., geoderma, in revision

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148

S13-O-03

EVOLUTION OF RADIOCARBON IN A SANDY AqUIFER ACROSS MULTIPLE TEMPORAL AND SPATIAL SCALES: CASE STUDY FROM SOUTHERN POLAND

DULINSKI M., RoZanSKI K., KanIa J., KUc T., KaPUSTa M.

aGH University of Science and Technology, KRaKoW, PolanD

AbstractAlthough radiocarbon has been perhaps the most often used tracer to quantify timescales of groundwater flow in the age range from ~103 to ~3×103 years, its usage has been plagued by numerous uncertainties related to non-conservative behaviour of carbon in groundwater systems. The results of a comprehensive study aimed at tracing the evolution of carbon isotope composition of TDIC reservoir, from unsaturated zone down to the discharge area, in a sandy aquifer near Krakow, southern Poland, are presented. Over the past two decades, the studied aquifer has been a test ground for various tracer methods being in use to define timescales of groundwater flow and to calibrate 3D numerical flow and transport models. Physical and chemical parameters (T, pH, Eh, major and trace ions) as well as concentrations of various environmental tracers including tritium, SF6, SF5CF3, CFC-11, CFC-12, stable isotopes of water, 85Kr, 39Ar, heavy noble gases, 3He/4He content, 13C and 14C content of TDIC have been analyzed in more that 45 wells. Here we focus on the potential of carbon isotope composition of TDIC reservoir for providing information on timescales of groundwater flow in the studied system.A multi-level well equipped with horizontally mounted piezometers and probes to collect pore water and soil CO2 was installed in the unsaturated zone of the studied aquifer. Strong seasonal fluctuations of pCO2 extending down to the water table, coupled with well-defined depth profiles of δ13CTDIC and almost constant Δ14CTDIC values, comparable with radiocarbon levels in the local atmosphere were observed. Simple models (closed/open system) do not account for the observed carbon isotope variations in both pore water and soil CO2. Model simulations and experimental data suggests that the TDIC reservoir is gradually evolving towards the closed-system conditions in the lower part of the unsaturated zone.Further downstream, in the confined part of the studied system, the evolution of carbon isotope composition of TDIC reservoir was modelled using several approaches:

(i) the piston-flow groundwater ages were calculated on the basis of the measured 13C and 14C isotope composition of TDIC reservoir and water chemistry, adopting the measured initial radiocarbon content in the recharge area and using several correction models available in the literature to account for chemical evolution of TDIC reservoir;

(ii) the chemistry and carbon isotope composition of TDIC reservoir between selected pairs of wells has been modelled using PHREEQC-2 and NETHPATH geochemical codes,

(iii) radiocarbon has been transported in the system using the 3D numerical flow and transport model calibrated with the aid of other available tracer data and using effective decay constant for 14C to account for dilution and non-radioactive losses of this element along groundwater flowpaths. The results of these three approaches are presented and discussed.

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149

S13-O-04

RADIOCARBON AND STABLE ISOTOPES OF WATER AS TRACERS OF GROUNDWATER DYNAMICS IN THE DANUBE RIVER BASIN OF THE SW SLOVAKIA

POVINEC P.(1), ZenISoVa Z.(1), SIVo a.(1), RIcHTaRIKoVa M.(1), bReIeR R.(1), oGRInc n.(2), aGGaRWal P.(3), aRaGUÁS-aRaGUÁS l.(3)

(1) comenius University, bRaTISlaVa, SloVaKIa;(2) Josef Stefan Institute, lJUblJana, SloVenIa;(3) International atomic energy agency, VIenna, aUSTRIa

AbstractSpatial variations in the distribution of water isotopes and radiocarbon in groundwater of the Zitný ostrov (Rye Island) at the Danube River Basin, which is the largest groundwater reservoir in the Central Europe (about 10 Gm3), has been carried out using the geostatistical analysis of experimental isotope data. It has been found that subsurface water profiles showed enriched δ18O levels at around 20 m water depths, which was probably caused by water irrigation of the land for agricultural purposes. Depleted δ18O levels were found below 30 m depths. The core of the subsurface 14C profile represents contemporary groundwater with 14C values above 80 pMC. Spatial distributions of δ18O, δ13C and 14C in different groundwater horizons will be discussed in detail. This has been for the first time when vertical distributions of isotopes in different groundwater horizons have been studied.

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150

S13-O-05

CO2 RADIOCARBON MEASUREMENTS IN SOUTH-FRANCE CAVES INTEREST FOR THE CARBON ORIGIN AND FOR CAVE AIR AND HYDROLOGY DYNAMICS

GENTY D.(1), MaSSaUlT M.(2), DelMoTTe M.(1), boURGeS f.(3), MoReaU c.(4)

(1) lSce - cnRS, l’orme des Merisiers, bat. 701, GIf-SUR-YVeTTe, fRance;(2) IDeS, Paris-Sud University, bat. 405, oRSaY, fRance;(3) Geoconseil, SaInT GIRonS, fRance;(4) laboratoire de Mesure du carbone 14, UMS 2572, cea, SaclaY, fRance

AbstractCO2 radiocarbon measurements made in three different caves from South-France for several years reveal significant differences between them, as well as within each cave, and temporal variations that we try to explain with the help of CO2 isotopes and other environmental factors (i.e. T, pCO2). In all caves, and for all measurements, the 14C activity of the cave CO2 appears to be lower than that of the outside atmosphere (from 2 pMC to 13 pMC). At the same period, a CO2

14C activity difference of more than 11 pMC can be observed between two caves that are relatively close to each other (70 km), and with similar climate and vegetation conditions. Inside the same cave, differences of more than 2 pMC can be observed; we have noted that more confined parts of the caves have lower 14C activity and higher pCO2 compared to parts that are closer to the surface/entrances. Delta 13C data tell us that the main source of the cave CO2 is the soil/OM CO2, with average values of ~ -23‰ in all three caves (within -20.3 to -24.8‰ limits). There is a strong correlation between δ13C and pCO2: δ

13C increases when pCO2 decreases, suggesting a mixing of atmospheric and soil/OM sources, especially when the pCO2 is below 3000 ppmv. In the Villars cave, where we have more frequent measurements, the CO2 maximum occurs in September-October. In the same cave, there is a time offset of ~1.5 month between external mean air temperature and cave pCO2 maximum, suggesting a close link between the soil/OM CO2 production and cave air dynamics that control its accumulation in the cave. At the same site, there is a significant opposite correlation between 14C activity and pCO2 which, combined with the δ13C data, suggests that the cave atmosphere CO2 is contaminated by dead carbon from organic matter degradation whose exact source is still unknown (old soil OM, other ?). Apparent present day CO2 age is 50 years for the Chauvet Cave, 160 years for the Villars Cave and 1000 years for the Cussac Cave. The low CO2

14C activity of this later site is discussed here too.

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151

S13-O-06

«IT IS A MATTER OF SIZE»: IDENTIFYING OPTIMAL GRAIN SIZE FRACTIONS FOR A RADIOCARBON BASED CHRONOLOGY OF LAKE SEDIMENTS

ROTHACKER L.(1)(2), DReVeS a.(2), GRooTeS P.M.(2), naDeaU M.J.(2), SIRocKo f.(1)

(1) Department of Sedimentology, University of Mainz, MaInZ, GeRManY;(2) leibniz-laboratory for Radiometric Dating and Isotope Research, University of Kiel, KIel, GeRManY

AbstractRadiocarbon measurements on bulk sediments have typically provided ages significantly older than actual time of deposition. The working hypothesis is that larger, less mobile organic particles are more likely to be linked to the deposition event. This study focuses on dating organic material associated with different grain sizes selected from bulk sediments to confirm if there is a relationship between radiocarbon ages and grain size. The main goal is to identify a grain size threshold for which 14C measurements give a reliable deposition chronology.

Samples have been collected from four depths of an 8 m long lake sediment core at the Gemündener Maar (Eifel, Germany), a lake of volcanic origin. Sediment radiocarbon activity in each layer is influenced by several factors including natural limnic reworking, flood events (transporting differently aged material), bioturbation, and age offsets caused by depleted 14C introduced in a hard water context or by expelled volcanic CO2. Samples have been classified into four standard grain size fractions: gravel, sand, silt and clay. These were separately treated using a standard acid-alkali-acid protocol (Grootes et al. 2004). The 14C concentration of each sample is determined using an accelerator mass spectrometry system (AMS) at the Leibniz-Laboratory for Radiometric Dating and Isotope Research (Kiel, Germany).

The implications of the results for carbon cycling in lake sediments obtaining radiocarbon ages for sediment deposition will be discussed.

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152

S13-O-07

AGE INVERSIONS AND EXCESS GEOLOGIC AGES IN RADIOCARBON DATING OF HOLOCENE LACUSTRINE SEDIMENTS FROM TECTONIC LAKE CHAPALA, WESTERN MEXICO

ZARATE DEL VALLE P.F.(1), SIMoneIT b.(2), feRneX f.(3), RaMIReZ-SancHeZ H.U.(1), ISRaDe-alcanTaRa I.(4)

(1) Guadalajara University, GUaDalaJaRa, MeXIco;(2) oregon State University, coRVallIS, UnITeD STaTeS;(3) Université de nice, nIce, fRance; (4) University of Michoacan, MoRelIa, MeXIco

AbstractHere we present a case study of age inversions (AI) and excess geologic ages in radiocarbon dating (RD) of shallow lacustrine sediments from neotectonic Lake Chapala in western Mexico. It is well known that RD could potentially be in error due to contamination of samples by either modern or old carbon. Such contamination can be evident as AI at some levels of the sedimentary column under analysis and as altered geologic ages (in excess or in deficit). In those cases, it is necessary to couple 14C dating of sediment with other radiometric techniques as short-lived isotope counting (SLIC) of 210Pb and 137Cs. Eight radiocarbon (site T46) and fifteen 210Pb (site CHP4; constant initial concentration model) dates were obtained for the lake sediments. The 14C age at 30 cm depth (2,000±40 yr B.P.) is one order of magnitude greater compared to the 210Pb age (200 yr A.D.) at the same level. The linear sedimentation rate (LSR) calculated from 14C ages do not match the LSR calculated from unsupported 210Pb activity for the upper sediments. This approach leads to the following conclusions:

1- The incorporation of detrital particles with ancient carbon into the sedimentary column of the lake occurred by a combination of:

a) the presence of outcrops of hydrothermal petroleum with radiocarbon ages >40 ka in the tectonic lake,

and b) mass transport due to the presence of two elongated gyre flow patterns integrated by cyclonic circulation (counterclockwise) in the north portion of the lake and anticyclonic circulation in the southern part.

2- A bioturbation mechanism is not necessary to explain the 14C AI in the top 70 cm.

3- Paleoseismicity is also not necessary to clarify the AI between 110 to 150 cm depth of the sediments.

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153

S13-O-08

C AS A TOOL TO TRACE TERRESTRIAL CARBON IN A COMPLEX LAKE SYSTEM: IMPLICATIONS FOR FOOD-WEB STRUCTURE AND CARBON CYCLING

KEAVENEY E.M.(1), baRRY c.D.(2), ReIMeR P.J.(1), foY R.H.(2)

(1) 14cHRono centre, Queen’s University belfast, belfaST, UnITeD KInGDoM;(2) agri-food and biosciences Institute, belfaST, UnITeD KInGDoM

AbstractGlobally lakes bury and remineralise significant quantities of terrestrial C, and the associated flux of terrestrial C strongly influences their functioning1. Changing deposition chemistry, land use and climate induced impacts on hydrology will affect soil biogeochemistry and terrestrial C export2,3 and hence lake ecology with potential feedbacks for regional and global C cycling.

C and nitrogen stable isotope analysis (SIA) has identified the terrestrial subsidy of freshwater food webs. The approach relies on different 13C fractionation in aquatic and terrestrial primary producers, but also that inorganic C demands of aquatic primary producers are partly met by 13C depleted C from respiration of terrestrial C, and ‘old’ C derived from weathering of catchment geology. SIA thus fails to differentiate between the contribution of old and recently fixed terrestrial C. Natural abundance 14C can help untangle riverine food webs4 where aquatic and terrestrial 13C overlap, but may also have utility for examining the age and origin of the C utilised by food webs.

Primary production in lakes is based on dissolved inorganic C (DIC), but DIC in alkaline lakes is partially derived from weathering of carbonaceous bedrock, a proportion of which is 14C-free. The low 14C activity yields an artificial age offset leading samples to appear hundreds to thousands of years older than their actual age. With terrestrial C inputs likely to increase, the origin and utilisation of allochthonous C in the food-web is in question: is it ‘modern’ C or from ‘old’ soil C stocks?

Stable isotopes and 14C were measured for biota, particulate organic matter (POM), DIC and dissolved organic carbon (DOC) from Lough Erne, Northern Ireland, a humic but alkaline lake. High winter δ15N values in calanoid zooplankton (δ15N = 24‰) relative to phytoplankton and POM (δ15N = 6‰ and 12‰ respectively) may reflect several microbial trophic levels between terrestrial C and calanoids. Furthermore winter calanoid 14C ages are consistent with DOC from inflowing rivers (87 and 75 year BP respectively) but not phytoplankton (355 year BP). Summer calanoid δ13N, δ15N and 14C (312 years BP) indicate greater reliance on phytoplankton.14C ages of the endangered coregonid whitefish, Pollan indicate significant utilisation of terrestrial C. There is also temporal and spatial variation in DIC, DOC and POM C isotopes.

References1. Prairie, Y.T. (2008) canadian Journal of fisheries and aquatic Sciences, 65:543-548.2. Monteith, D.T et al., (2007) nature, 450:537-5353. Futter, M.N. et al., (2007) Water Resour. Res. 43:doi:10.1029/2006WR004960.4. Caraco, N., et al.,(2010) ecology, 91: 2385-2393.

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S13-O-09

A CONCEPTUAL WATERSHED MODEL DESCRIBING THE RIVERINE EXPORT OF PARTICULATE ORGANIC RADIOCARBON

BLAIR N.(1), cHIlDReSS l.(1), leITHolD e.(2)

(1) northwestern University, eVanSTon, Il, UnITeD STaTeS; (2) north carolina State University, RaleIGH, nc, UnITeD STaTeS

AbstractA conceptual model is proposed that describes the influence of watershed properties on the nature of riverine exported particulate organic carbon (POC). As a basic principle, the integrated storage of organic carbon-bearing particles in sediment and soils should lead to a replacement of material derived from upland sources by fresher organic carbon. POC that is not replaced will age. These processes should be reflected in POC 14C-compositions.There are robust relationships between radiocarbon content, suspended load concentrations and % organic C. These are explained as a result of mixing 14C-free fossil C from sedimentary rocks with 14C-containing material derived from extant ecosystems and soils. The mixing of the two types of OC obscures proposed replacement and ageing effects. Evidence for each can be seen when bulk 14C POC measurements are deconvoluted into constituent signatures. The two key parameters that emerge are the concentration of fossil C and the apparent age of the non-fossil fraction. Hypothetically, fossil C derived from upland sources via the mass wasting of sedimentary rocks should decrease in abundance with time spent within soils because of oxidative losses. Likewise, the 14C-age of non-fossil C (contemporary plus aged soil C) should increase with time spent in the watershed. Using watershed size as a surrogate for residence time we find these relationships thus the conceptual model appears valid to a first approximation. The model will aid in the interpolation of exported POC compositions among world’s rivers, which in turn will contribute to a more accurate description of the global C-budget and its response to environmental change.

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S13-O-10

RAMPED PYROLYSIS RADIOCARBON AGE DISTRIBUTIONS IN RIVERINE POC

ROSENHEIM B.(1), RobeRTS b.(2), GalY V.(3), allISon M.(4), KolKeR a.(2), beaUPRe S.(3), Roe K.(1)

(1) Tulane University, neW oRleanS, UnITeD STaTeS;(2) louisiana Universities Marine consortium, cHaUVIn, UnITeD STaTeS;(3) Woods Hole oceanographic Institution, WooDS Hole, UnITeD STaTeS;(4) University of Texas, aUSTIn, UnITeD STaTeS

AbstractRiverine POC represents a significant flux of atmospheric, soil, and petrogenic carbon to the world’s oceans. Radiocarbon determination of bulk POC has illustrated that rivers of different sizes and locations can have quite different radiocarbon ages, and radiocarbon determination in specific compounds of POC has constrained both modern and 14C-free carbon within the POC mixture. Here we present measurements of the bulk POC, separated by ramped pyrolysis to exploit differences in relative stability, from two different major river systems. Our measurements of ramped pyrolysis 14C on the Mississippi – Atchafalaya River system (MARS) benefitted from repeated sampling through several hydrographic years, including two significant high water events in 2008 and 2011. The results indicate that a large proportion of the POC pool becomes older with higher river discharge, implying that events disproportionately responsible for delta building carry a higher proportion of pre-aged terrigenous carbon. Our measurements from the Ganges-Brahmaputra River system (G-B) benefit from large scale investigations into the chemical and isotopic makeup of POC in the main rivers and tributaries. Results indicate that POC in G-B headwaters consist of three discernible pools of C – modern, protracted biospheric carbon on the scale of 10-15,000 14C y, and 14C-free petrogenic carbon. The ramped pyrolysis method allows for direct measurement of petrogenic carbon and results corroborate earlier estimates of the amount of this pool that is transported by the G-B and buried in Bay of Bengal sediments. Taken together, the results from the MARS and the G-B demonstrate changes that can occur in carbon transport both temporally and spatially. Results from our work indicate that small, steep bypass river systems can carry straightforward mixtures of petrogenic and biospheric carbon, but such constrasts can be blurred by long residence times and ample mixing with floodplain sediments in large integrative river systems. These results lead to the question of how much petrogenic OC has been buried in the world’s river deltas, diminishing their role as moderators of greenhouse gases on millennial time scales.

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SESSION 14

CONTINENTAL CARBON CYCLE

ConvenersT. Chiti (ITA), P. moreira-Turcq (FRA), J. Rethenmeyer (DEU)

DescriptionThe investigation of organic carbon dynamics in continental carbon reservoirs is complicated by the highly heterogeneous composition and relatively rapid turnover of organic matter in soils and continental aquatic sediments. 14C has proven to be a useful indicator for different carbon sources and tracer for organic matter degradation and transport processes. In this session we would like to bring together scientists using 14C analysis to determine residence times and stable/labile carbon pools, identify microbial degradation of organic matter, the loss of gaseous and dissolved carbon from terrestrial systems, and transport of plant and soil derived carbon into rivers, lake and coastal sediments. Contributions using or further developing methodical approaches such as fractionation methods and compound-specific 14C analysis are also welcome.

Keywordssoil carbon cycling, turnover times, carbon transport, compound-specific 14C

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S14-INV-01

qUANTIFYING RADIOCARBON ISODISEqUILIBRIUM IN TERRESTRIAL ECOSYSTEMS

TRUMBORE S.(1), RanDeRSon J.T.(2), lIn H.-. .W.(2)

(1) MPi-biogeochemistry, Jena, GeRManY;(2) Uc Irvine, IRVIne, UnITeD STaTeS

AbstractA key characteristic of ecosystems is the age distribution of C in plants and soils, which can be measured directly using radiocarbon. In particular, comparison of the radiocarbon signature of decomposition-derived CO2 with the time history of 14C in the atmosphere provides a measure of the time elapsed between C uptake by photosynthesis and its ultimate return to the atmosphere from terrestrial ecosystems. This isodisequilibrium integrates the residence time of C in plants and the time required for them to decompose. It thus provides a useful observational constraint that can be directly compared with predictions made using ecosystem models that track carbon flow through ecosystems. The age of respired CO2 also constrains estimates of the potential for C storage in response to increased productivity.This talk will summarize measurements of the 14C signature of CO2 respired in incubations of soil and surface litter from ecosystems ranging from tropical forests to tundra. Measurements of the 14C signatures of fresh plant litter components indicate a range in the age of C being added to ecosystems, with especially enriched 14C values in woody tree roots. Thus turnover times calculated using the flow of bomb radiocarbon through soils may underestimate decomposition rates unless the time lag in living plant tissues is included in model estimates. The 14C signature of respired CO2 ranges from <1 year (annual grasslands) to >50 years (in tundra). Radiocarbon in CO2 respired from surface litter layers are similar to the 14C signatures of the organic matter being decomposed. In contrast, the radiocarbon signature of CO2 derived from mineral soils is often older than that being respired from the surface litter, and has no relationship to the 14C signature of bulk soil organic matter. Shifts in microbial substrate age with changes in land use or climate are also detectable when changes in carbon stocks are too small to measure.Although time lags in vegetation (particularly roots) are important and require more investigation, the radiocarbon signature of respired CO2 provide a direct test for comparison with carbon cycle models that include plant allocation and decomposition (here we compare with the CASA model predictions). These time lags can also constrain estimates of ecosystem carbon storage under scenarios of increased productivity with elevated CO2. Such estimates do not require a knowledge of C stocks, which do not necessarily have the same age as fast-cycling C pools that contribute the most to respiration. Using tropical forests as an example, we show that observations of C storage using permanent plots are unlikely to be caused by CO2 fertilization.

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S14-O-02

50 YEARS OF CARBON CYCLE STUDIES AT THE RAFTER RADIOCARBON LABORATORY: LESSONS LEARNED FROM BOMB C-14 STUDIES OF THE BIOSPHERE

BAISDEN W.T.

GnS Science, loWeR HUTT, neW ZealanD

AbstractAthol Rafter, as the founding Director of New Zealand’s Institute of Nuclear Sciences, developed a deep interest in the flow of bomb 14C through the atmosphere, biosphere, soil and ocean. The laboratory initiated measurements of atmospheric 14C prior to Keeling’s reliable pCO2 measurements. As the pronounced enrichment of atmospheric 14C became evident during the period of atmospheric thermonuclear weapons testing, the potential to quantify the carbon cycle and test the assumptions underlying radiocarbon dating became apparent. Rafter, and his successor Bernie O’Brien, initiated a series of studies in organisms, litter, and soil that demonstrated both the potential and pitfalls of applying bomb-14C to study the flow of C through the biosphere. These pioneering studies often require modern analytical tools to enable mathematical interpretations without confusion, and in many cases benefit from recent 14C measurements. Recent research has shown that reinterpreting and building on these early studies has the potential to enable important conclusions about the soil carbon cycle in particular. For New Zealand pasture soils, these include recognising that a substantial proportion of deep soil carbon can be mobilised or oxidised on decadal timescales (Baisden and Parfitt, 2007), and that the structure and dynamics of soil carbon “pools” commonly employed in ecosystem carbon cycle models is supported and easily constrained by bomb-spike 14C modelling (Baisden et al., 2012). In this presentation, I contribute to the conference’s theme by focussing on using the extensive archive of laboratory correspondence to compare and contrast the examples that have, thus far, enabled remarkable and unique contributions to carbon cycle science, from those proving less successful. Lessons learned range from confirming and quantifying carbon cycle behaviour, to identifying that reductionist approaches determined to “take ecosystems apart” often lead to ongoing frustration and confusion. Surprisingly, in carbon cycle studies bulk 14C measurements appear to hold utility that stands the test of time, while it now appears clear that humic fractionations generated little progress, and even sequential density fractionation may be limited in the quantity and quality of additional information it provides over simple bulk measurements. Overall, the biggest gains have been made from improving model-data architecture so that integrative models can be applied with robust assumptions. Ideally, models can be simplified rather than complicated by additional progress.

References1. Baisden WT, Parfitt R. 2007. Bomb 14C enrichment indicates decadal C pool in deep soil? Biogeochemistry

85(1):59-68.2. Baisden WT et al. 2012. Evaluating 50 years of time-series soil radiocarbon data: towards routine calculation

of robust C residence times. Biogeochemistry:10.1007/s10533-011-9675-y.

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S14-O-03

A THEORETICAL SOIL CARBON MODEL FOR DECIPHERING HOLOCENE TROPICAL VEGETATION CHANGES IN CENTRAL CAMEROON

TURCQ B.(1), DeSJaRDnS T.(2), ManDenG-YoGo M.(1), nGUeTnKaM J.P.(3), acHoUnDonG G.(4), leZIne a.M.(5)

(1) locean (UPMc/cnRS/IRD/MnHn), bonDY, fRance;(2) bIoeMco/IRD, bonDY, fRance;(3) Université de ngaoundéré,faculté des Sciences, Département des Sciences de la Terre., nGaoUnDeRe, caMeRoon; (4) Herbier national du cameroun, YaoUnDe, caMeRoon; (5) locean (UPMc/cnRS/IRD/MnHn), PaRIS, fRance

AbstractSoil organic matter (SOM) is composed of a large diversity of organic compounds originating from organic matter decomposition. These compounds can be groups into functional pools (Trumbore, 2009), more or less labile, having different decomposition rates and different turnover times.Using this basic principle we built a theoretical mathematical model that could explain the carbon soil profiles observed in Central Cameroon savannah-forest transition zone. The model is composed of three pools of organic matter whose rates of accumulation and decomposition are tuned based on 14C analysis of 5 soils profiles.The same model has been used to interpret the 13C variations of soil organic matter in the 5 profiles. Analyses of 13C in SOM profiles allow to reconstruct the succession between forest and savannah because these ecosystems present very different ∂13C values (-14 to -18‰ for the savannah SOM and -25 to -28‰ for the forest SOM). This method has been use to trace the savannah-forest boundary fluctuations in Congo (Schwartz et al., 1992). The savanna profiles are characterized by the dominance of C4 plants (poaceae) in SOM with values from -17‰ to -14‰ in the upper part. In depth, the values decrease rapidly reaching values from -24 ‰ to -18‰ at around 150 cm. These values correspond to vegetation varying between forest (-24 ‰) and open forest/arboreal savannah (-18‰). A change from open forest to savannah at the Middle-Late Holocene transition can explain most of the studied 13C profiles. This change would be in agreement with paleovegetation studies in the same region (Lezine et al, 2007).

References1. Lezine, A.-M. 2007. Postglacial Pollen Records of Africa . In Encyclopaediaof Quaternary Sciences, ScottA Elias

ed., Elsevier. Vol.4, 2682-2698.2. Schwartz, D., Mariotti, A., Trouve, C.; Klaas Van Den B., Guillet, B., 1992. Étude des profils isotopiques 13C et

14C d’un sol ferrallitique sableux du littoral congolais. Implications sur ladynamique de la matière organique et l’histoire de lavégétation. C. R. Acad. Sci. Paris, t. 315, Série II, p. 1411-1417.

3. Trumbore, S., 2009. Radiocarbon and Soil Carbon Dynamics. Annu. Rev. Earth Planet. Sci. 37:47-66.

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S14-O-04

SEARCHING OLD CARBON IN PERMAFROST SOILS

HÖFLE S.(1), ReTHeMeYeR J.(1), RoobRoecK D.(2), boecKX P.(2), MÜlleR c.W.(3), MollenHaUeR G.(4)

(1) University of cologne, coloGne, GeRManY;(2) Ghent University, GHenT, belGIUM;(3) Technical University Munich, MUnIcH, GeRManY;(4) alfred-Wegener Institute for Polar and Marine Research, bReMeRHaVen, GeRManY

AbstractGlobal warming is predicted to affect Polar Regions most strongly. This will lead to the degradation of permafrost soils, to an increase in thickness of the active layer, the upper permafrost soil layer thawing during summer, and turn these large carbon reservoirs into a source of CO2 and CH4 for the atmosphere (Khvorostyanov et al. 2008). Recent measurements of the active layer thickness indicate a rapid increase, e.g. about 20% during the last ten years (unpublished data) in the Lena-Delta, Russia. Old organic carbon, previously freeze locked, will be exposed and become then available for microbial degradation as shown by previous studies (Schuur et al. 2009). Little is known yet about the composition, stabilization and microbial availability of soil organic matter (SOM) in the active layer of permafrost soils.We characterized SOM distribution in different depth intervals of the active layer and the uppermost frozen permafrost layer in the polygonal tundra of the Lena-Delta (Siberia) using bulk, molecular and radiocarbon analysis with the aim to gain information on ‘old’ SOM components and their microbial availability.Different cryogenic structures (polygon rim and centre), formed by thawing and freezing cycles, showed great differences in the depth distribution of total organic carbon. The water saturated polygon centre soil had higher carbon contents than the rim. Preserved cell lipid compounds, like fatty acids, in soils or sediments can be used as biomarker indicating source organisms. The depth distribution of fatty acids indicated that most SOM is derived from terrestrial higher plants. We found surprisingly low 14C contents of bulk SOM in the very shallow active layer (25 cm thickness), which decreased from 89.78 pMC (0-6 cm) to 78.31 pMC(11-25 cm) and further in the uppermost frozen permafrost layer to 68.39 pMC (> 25 cm) in the polygon rim.To identify origin and microbial availability of the relatively ‘old’ SOM, 14C contents of individual plant-derived fatty acids as well as of phospholipid fatty acids (PLFAs) derived from cell membranes of living soil microbes, were determined. The compound-specific 14C concentrations were considerably higher for bacterial PLFAs in different depth intervals compared to the bulk SOM values suggesting that ‘old’ carbon is either not in favour of decomposition or is not available for these microorganisms. 14C results for different physically defined soil fraction are used to answer if ‘old’ OM is physically protected against microbial attack or if other stabilization mechanisms have to be considered.

References1. KHVOROSTYANOV D V et al. 2008. Vulnerability of permafrost carbon to global warming. Part II: sensitivity

of permafrost carbon stock to global warming. Tellus,60B, 265–275.2. SCHUUR E A G et al. 2009. The effect of permafrost thaw on old carbon release and net carbon exchange

from tundra. nature, 459, 556-559.

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S14-O-05

CAN COMPOUND-SPECIFIC RADIOCARBON ANALYSES TRACE LOCAL TERRESTRIAL CARBON CYCLES?

GIERGA M.(1), HaJDaS I.(2), SMITTenbeRG R.H.(3), WacKeR l.(2), beRnaSconI S.M.(1)

(1) Geological Institute, eTH Zürich, 8092 ZÜRIcH, SWITZeRlanD;(2) laboratory of Ion beam Physics, 8093 ZÜRIcH, SWITZeRlanD;(3) Department of Geological Sciences, Stockholm University, 10691 STocKHolM, SWeDen

AbstractSince the introduction of compound-specific radiocarbon analysis (CSRA) by Eglinton et al. (1996) this method has become a powerful tool to study the fate of individual biomarkers in terrestrial or marine ecosystems. Nevertheless, there are only few examples using CSRA for sediment records of lakes with small catchments (e.g. Uchikawa et al. 2008). Studying sediments of these small, well-defined systems allows a reconstruction of regional environmental processes.We present a CSRA study of the sedimentary record of the Swiss Lake Soppensee covering the last 14,000 years. The small, eutrophic, hard-water lake is a very well dated sediment record (Hajdas and Michczynski 2010) with undisturbed organic carbon-rich and partially laminated sediments. The aim of this study was to evaluate the potential of using specific compounds for either radiocarbon dating of the sediment core, or the extent to which terrestrial lipids are pre-aged on land. The latter provides insight in terrestrial carbon build-up through time.We target compounds of exclusive terrigenous origin for CSRA in order to compare their radiocarbon (14C) signature with the existing data set of sediment ages given by macrofossil dating (Hajdas and Michczynski 2010; van Raden et al. unpublished). Additionally, we measured 14C ages of bulk organic matter. Other biogeochemical evidence determined in this study will also support the interpretation of these various 14C signatures.We purified individual long-chain n-alkanes and fatty acids by the use of gas- and liquid chromatography for subsequent radiocarbon analysis. Bulk organic material was treated with an acid-base-acid protocol prior analysis. Until 4000 yr BP, the biomarker ages are similar to those of the macrofossils. However, after 4000 yr BP an increasing offset between the biomarker and sediment age can be observed. These results are discussed in the context of landscape evolution and soil carbon dynamics.

References1. Eglinton, Aluwihare, Bauer., Druffel, McNichol. Anal. Chem. 68, 904 (1996).2. Uchikawa, Popp, Schoonmaker, Paleolimnol. 39, 43 (2008)3. Hajdas, Michczynski. Radiocarbon, 52, 1027 (2010)

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S14-O-06

CONTROLS ON THE RADIOCARBON AGE OF BIOSPHERIC CARBON DISCHARGED FROM RIVER DRAINAGE BASINS

EGLINTON T.(1)(2), GalY V.(2), VoSS b.(2), PonTon c.(2), WU Y.(3), DIcKenS a.(4)(2), DRenZeK n.(2)(5), HUGHen K.(2), ScHefUSS e.(6)(2), fenG X.(1)(2), GIoSan l.(2), MonTlUcon D.(1)(2), PeUcKeR-eHRenbRInK b.(2)

(1) eTH Zurich, ZURIcH, SWITZeRlanD;(2) Woods Hole oceanographic Institution, WooDS Hole, UnITeD STaTeS;(3) east china normal University, SHanGHaI, cHIna;(4) Mt. Holyoke college, SoUTH HaDleY, UnITeD STaTeS;(5) Schlumberger Research, caMbIRDGe, UnITeD STaTeS;(6) bremen University, bReMen, GeRManY

AbstractThe transfer and burial of organic carbon produced by the terrestrial biosphere in marine sediments represents a key component of the carbon cycle that exerts long-term control on the balance of O2 and CO2 in the atmosphere. However, our current understanding of the timescales and pathways involved in the transfer of terrestrial biospheric carbon from biological source to sedimentary sink remains limited. Such information is crucial for developing a mechanistic understanding organic matter cycling on the continents. Radiocarbon is increasingly being used to constrain the «age» of organic constituents in the dissolved and particulate phase in river systems in order to examine the dynamics of terrestrial carbon delivery to the oceans. In addition to measurements on bulk carbon phases, molecular-level radiocarbon analyses are enabling specific pools of terrestrial carbon to be tracked.A wide range of 14C ages have been observed for different organic components in rivers, indicating that land-ocean organic matter transfer via rivers may be rapid (years, decades) or may take place over centuries to millennia. This observation leads to questions concerning the controls of drainage basin properties on biospheric carbon dynamics within continental drainage basins, the provenance and transformation of organic signals emanating from river systems, and past variability in storage times of organic carbon on the continents.This presentation will provide examples from studies of a range of different fluvial systems in order to explore the factors that influence radiocarbon ages of specific components of terrestrial biospheric carbon carried by rivers to the ocean. Radiocarbon measurements have been made on bulk phases and molecular markers of vascular plant input (plant leaf waxes and lignin-derived phenols) isolated from particulate matter collected from within river systems, as well as on sediment cores collected near the mouths of rivers. Additional molecular isotopic (stable carbon and hydrogen isotopes) measurements of specific markers are used to provide complementary information on the provenance of the vegetation signals and on regional environmental conditions. Findings are discussed in the context of the biospheric carbon mobilization and storage within drainage basins and its implications for our understanding of continental organic carbon cycling.

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SESSION 15

ATMOSPHERIC CARBON CYCLE

ConvenersJL Jaffrezo (FRA), I. Levin (DEU)

DescriptionThis session is devoted to the applications of radiocarbon measurements for the understanding of the atmospheric carbon cycles of gases and aerosols. This potentially includes a wide range of applications, from global to regional scale carbon fluxes fingerprinting to process level investigations. The important aspects of sampling and analysis of minute amounts of carbon for radiocarbon measurements as well as measurements with separation techniques between different fractions (e.g. EC and OC or gaseous compounds) are also welcome.

Keywordsatmospheric carbon cycle, source apportionment, flux measurements, sampling, separation, and analysis

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S15-O-01

14CO2 MEASUREMENT ACTIVITIES WITHIN THE NOAA/ESRL COOPERATIVE GLOBAL AIR SAMPLING NETWORK

LEHMAN S.(1), MIlleR J.(2), TanS P.(3), MonTZKa S.(3), SWeeneY c.(2), anDReWS a.(3), WolaK c.(1), TURnbUll J.(4), SoUTHon J.(5)

(1) University of colorado, boUlDeR, UnITeD STaTeS;(2) noaa eSRl and the University of colorado, boUlDeR, UnITeD STaTeS;(3) noaa eSRl, boUlDeR, UnITeD STaTeS;(4) national Isotope center, loWeR HUTT, neW ZealanD;(5) University of california, IRVIne, UnITeD STaTeS

AbstractThe small radiocarbon fraction of total CO2 has proven to be an ideal tracer for its fossil fuel derived component. Unlike all other contributions to the CO2 budget, the fossil fuel component is devoid of radiocarbon, so that temporal and spatial gradients in recently added fossil fuel CO2 can be readily identified as radiocarbon gradients provided there is adequate precision in the measurements. Over large industrialized land areas such as Eurasia and North America, the use of 14C to isolate the recently added fossil fuel contribution also quantifies (by difference) the change in atmospheric CO2 due to uptake and release by the terrestrial biosphere. Here we will report on a growing number of 14CO2 measurement activities within the NOAA Cooperative Global Air Sampling Network, with a focus on the use of 14CO2 to constrain the relative and absolute emissions of a large suite of anthropogenic trace gases measured in the same samples. We will also evaluate “non-fossil” contributions to the tropospheric 14CO2 distribution as a means of estimating possible biases in our fossil fuel CO2 detection algorithms.

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165

S15-O-02

A YEARLY CYCLE OF RADIOCARBON IN ORGANIC AND ELEMENTAL CARBON AT A RURAL SITE IN THE NETHERLANDS

DUSEK U.(1), Monaco M.(1), SZIDaT S.(2), MeIJeR H.a.J.(3), Van DeR PlIcHT J.(3), RÖcKMann T.(1)

(1) Utrecht University, UTRecHT, neTHeRlanDS;(2) University of bern, 3012 beRne, SWITZeRlanD;(3) University of Groningen, GRonInGen, neTHeRlanDS

AbstractMeasurement of the radioactive carbon isotope 14C in aerosols can provide a direct estimate of the contribution of fossil fuel sources to aerosol carbon. In aerosol science, measurements of 14C/12C ratios are usually reported as fraction modern (fm). The radiocarbon signature gives a clear distinction between ‘modern’ carbon sources (fm around 1.1-1.2 for biomass burning and around 1.05 for biogenic secondary organic aerosol) and ‘fossil’ carbon sources (fm = 0 for primary and secondary formation from fossil fuel combustion).High volume filter samples have been collected since February 2011 at Cabauw, a rural location in the Netherlands. We report measurements of fm for total carbon (TC), organic carbon (OC), water insoluble OC (WIOC) and thermally refractory carbon (RC) as a proxy for elemental carbon. The carbon fractions are isolated by combusting TC at 650°C, OC and WIOC at 360 °C. Refractory carbon is defined as the carbon remaining on the filter after water extraction, combustion at 360°C for 15 min and at 450°C for 2 minutes. The method has been tested with test substances and real aerosol filters and indicates little charring for water-extracted filters.First results of 7 filter samples taken from February – Mai 2011 show fm(OC) generally larger than 0.86 at the rural site, except for one case, when a strongly polluted air mass originating in Eastern Europe reached the site. This indicates a strong contribution of natural sources to OC, even in the Netherlands, a very densely populated country with one of the highest levels of aerosol pollution in Western Europe. In particular, water soluble OC in the rural springtime aerosol seems to originate almost entirely from contemporary sources. Refractory carbon also showed relatively high fm, generally between 0.3-0.5, except in two cases, when marine air masses reached the site from the west and fm(RC) dropped to around 0.1. This could mean that biomass combustion plays a significant role around the Netherlands even in springtime. It is also possible that there exists a biogenic, organic component of the aerosol that evolves at such high temperatures that it is virtually inseparable from elemental carbon.Currently, filter samples from other seasons are prepared for radiocarbon analysis and a full yearly cycle of 14C measurements in various fractions of the carbonaceous aerosol will be presented.

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S15-O-03

RADIOCARBON CONCENTRATION IN SOIL-RESPIRED CO2 FLUX: MODEL-DATA COMPARISON FOR THREE DIFFERENT ECOSYSTEMS IN SOUTHERN POLAND

GoRcZYca Z., KUC T., RoZanSKI K.

aGH Univ. of Science and Technology, KRaKoW, PolanD

AbstractThe flux of soil-respired CO2 entering the atmosphere is an important component of atmospheric carbon budget on continents. Whereas monitoring networks for studying isotopic variability of atmospheric CO2 are relatively well developed, the relevant data for soil CO2 flux are still fragmentary.Here we report the results of long-term observations (1999-2006) of monthly mean soil CO2 flux and its carbon isotope composition (13C/12C and 14C/12C ratios), performed on a grassland site located in the urban area of Krakow, southern Poland. The site was exposed to anthropogenic impact, intensified within last 6 decades. The results obtained in Krakow are compared with analogous measurements performed at remote, «clean» sites located in a mixed forest and on the cultivated agricultural field, located ca. 40 and 150 km east of Krakow, respectively. A dedicated sampling system based on the closed-chamber approach was used to collect monthly cumulative samples of soil-respired CO2.Large differences in the measured Δ14CO2 values were observed among the monitored ecosystems: the soil-respired CO2 collected at the mixed forest site was depleted in 14C with respect to European free-atmosphere continental Δ14CO2 background (high mountain station Jungfraujoch in Swiss Alps) by ca. 40‰, while the urban site revealed 14C depletion by ca. 20‰ against the same reference. The Δ14CO2 values observed at the agricultural site were lying in-between, clustering along the regional reference atmospheric trend curve. The Δ14CO2 values measured in soil-respired CO2 at the urban site turned out to be indistinguishable from the Δ14CO2 values measured in parallel in the local atmosphere.Radiocarbon concentration in soil-respired CO2 flux was interpreted using a multi-layer box model accounting for input of carbon to the soil profile via autotrophic respiration and deposition of fresh organic matter, as well as three different sources of CO2 in the soil profile:

(i) root respiration,

(ii) «fast», and (iii) «slow» box of decomposing organic matter. The model allowed the estimation of mean turnover time of carbon in the soil profile for each of the monitored sites. The obtained values were equal ca: 14, 22 and 10 years for mixed forest, agricultural field and urban grassland site, respectively.

The observed differences in Δ14CO2 values of the measured fluxes of soil-respired CO2 representing mostly heterotrophic respiration, suggest that radiocarbon content of the biogenic component in the local atmospheric CO2 budget is site-specific and may differ significantly from the regional atmospheric background Δ14CO2 value. The assumption that 14C concentration in the biospheric CO2 component is equal to that of regional atmospheric reference value, widely used in the radiocarbon-based assessments of the fossil-fuel contribution in the local atmospheric CO2 load, needs to be carefully evaluated on case-by-case basis.

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S15-O-04

DIURNAL CYCLE OF FOSSIL AND NON-FOSSIL TOTAL AND ORGANIC CARBON USING 14C ANALYSES DURING CALNEX

ZOTTER P.(1), PRÉVÕT a.(1), el-HaDDaD I.(1), ZHanG Y.(2), SZIDaT S.(2), WacKeR l.(3), ZHanG X.(4), lIn Y.H.(5), HaYeS P.(6), SURRaT J.(5), JIMeneZ J.l.(6), WebeR R.(4), balTenSPeRGeR U.(1)

(1) Paul Scherrer Institut, VIllIGen PSI, SWITZeRlanD;(2) Department of chemistry and biochemistry & oeschger centre for climate change Research, University of bern,

beRn, SWITZeRlanD;(3) laboratory of Ion beam Physics, Swiss federal Institut of Technology, Zurich, Switzerland, ZÜRIcH, SWITZeRlanD;(4) School of earth and atmospheric Sciences, Georgia Institute of Technology, aTlanTa, UnITeD STaTeS;(5) Department of environmental Sciences & engineering, University of north carolina, cHaPel HIll, UnITeD STaTeS; (6) Department of chemistry and cIReS, University of colorado, boUlDeR, UnITeD STaTeS

AbstractCarbonaceous particles (total carbon, TC) are a major fraction of the fine aerosol and effect climate and human health. TC is classified into the sub fractions elemental carbon (EC) and organic carbon (OC). EC originates only from fossil fuel combustion and biomass burning. OC can be emitted directly as primary organic aerosol from biogenic sources, wood burning and fossil fuel combustion or can be formed in the atmosphere as secondary organic aerosol (SOA) (Szidat et al. 2006). Analysis of the radioactive isotope 14C is a unique tool for distinguishing fossil and non-fossil sources of TC, since 14C in fossil fuels is completely depleted whereas other sources have a contemporary 14C level.Previous 14C analyses have been performed on aerosol filters with a sampling time ≥6h. This study presents the first 14C measurements performed on high time resolution (3-4h) filter samples from the CalNex-LA 2010 campaign, which was conducted at the California Institute of Technology in Pasadena. Separation of OC and TC was carried out using the THEODORE system (Szidat et al. 2004) and a Sunset ECOC analyzer. The evolving CO2 was cryo-trapped and sealed in glass ampoules for 14C measurements which were then performed with the mini radiocarbon dating system MICADAS (Synal et al. 2007). The analysis of small samples (3-50µg) with a high stability and accuracy was possible using a CO2 feeding system and a gas ion source (Ruff et al., 2007) installed at MICADAS.First results for June 4 and 14 show a distinct diurnal variation with a peak for fossil TC (TCf) in the early afternoon after the plume of the L.A. basin is transported to Pasadena with the sea breeze. The low EC concentrations (max. 0.8 and 1.0 µg/m3 for June 4 and 14, respectively), the low increase of EC during the day and aerosol and gas-phase measurements from other groups (e.g. Zhang et al. 2011) indicate that the increase of TCf in the early afternoon is mainly due to fossil SOA formed from anthropogenic precursor gases in the L.A. plume. The non-fossil TC is on average 41% and 45% for June 4 and June 14, respectively, and stays constant between 2 and 3 µg/m3 throughout both days, even though the Los Angeles area is strongly influenced by traffic-related emissions. This indicates that biogenic, cooking or other contemporary carbon sources also significantly affect the total carbon budget in urban areas.

AcknowledgementThis work was supported by CALTECH (J. Seinfeld) CARB, NOAA (J. de Gouw), the University of California, Los Angeles (J. Stutz) and the NSF.

References1. M. Ruff et al., Radiocarbon 49(2), 307-314 (2007)2. H.-A. Synal et al., Nuclear Instruments and Methods in Physics Research Section B: Beam Interactions with

Materials and Atoms 259(1): 7-13 (2007)3. S. Szidat et al., Nuclear Instruments and Methods in Physics Research Section B: Beam Interactions with

Materials and Atoms 223-224: 829-836 (2004)4. S. Szidat et al., J. Geophys. Res. 111, D07206 (2006)5. X. Zhang et al., Geophys. Res. Lett. 38, L21810 (2011)

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S15-O-05

IMPLICATIONS OF USING PARAMETERIZED NUCLEAR POWER PLANT EMISSIONS OF 14CO2 ON DERIVING RELIABLE ESTIMATES OF FOSSIL FUEL CO2 FROM ATMOSPHERIC OBSERVATIONS

VOGEL F.R.(1), leVIn I.(2), WoRTHY D.e.J.(1)

(1) environment canada, ToRonTo, canaDa;(2) Institut für Umweltphysik, HeIDelbeRG, GeRManY

AbstractTo assess the continental carbon balance at regional scale (e.g. North America) requires a quantitative knowledge of the anthropogenic CO2 component from the burning of fossil fuels. Measuring the Δ14C depletion due to the local surplus of fossil fuel CO2 (ΔFFCO2) is a widely used technique, however, the addition of 14CO2 from nuclear power plants (14CO2 nuc) can significantly mask this depletion and alter the estimated anthropogenic CO2 contribution. To correct for this artifact, high-resolution models need to include adequate 14CO2 nuc fluxes. Uncertainties in the 14CO2 nuc fluxes will translate to an increased uncertainty of the ΔFFCO2 estimate.In this study, we compare a commonly used parameterization of 14CO2 fluxes for nuclear power plants (based on a constant emission factor of power output to 14CO2 nuc emissions) with measured 14CO2 nuc fluxes from an in-situ stock monitoring program. We assess the implications of different 14CO2 nuc flux estimates for observations performed in Egbert, Canada, in an area with elevated anthropogenic 14CO2 fluxes. We also utilize a high-resolution modeling framework to compare the influence of 14CO2 nuc emissions on the 14CO2 levels to the modeled depletion due to ΔFFCO2. Lastly, a two-year long 14CO2 measurement record is used to assess the 14CO2 nuc emissions on 2-week time scales.Our results show that the average 14CO2 nuc emission estimates derived from the parameterization compares well with the measured fluxes; however, it does not capture the strong inter-annual variations. The ratio of (what is true) observed vs. parameterized annual 14CO2 nuc fluxes ranges from 0.25-2 (P10%-P90%). At Egbert, the nuclear power plant correction is on the order of 50% of the FFCO2 caused depletion. The large uncertainty in the annual 14CO2 nuc fluxes (of the parameterization) thus leads to an uncertainty up to 100% for ΔFFCO2 estimates. Neglecting the inter-annual changes also introduces an artificial trend in estimated ΔFFCO2 of about 15% for 2006-2010. Comparing our modeling results with the two year integrated Δ14C observational record reveals that the model is only able to simulate both the general level as well as the variability of Δ14C when including appropriate 14CO2 nuc fluxes. Furthermore, we find that 14CO2 nuc fluxes increase by one order of magnitude during maintenance periods at the CANDU sites.We conclude that the strong inter-annual variability of the 14CO2 nuc fluxes implies that a parameterization approach is not sufficient for sites with a strong influence of 14CO2 nuc. It significantly increases the uncertainty of the ΔFFCO2 estimate and can potentially produce trends in ΔFFCO2. Given that ΔFFCO2 observations will become increasingly important for independently quantifying anthropogenic emissions, it is critical to further improve the available (global) 14CO2 nuc emission inventories and aim for an intra-annual resolution of the 14CO2 nuc fluxes including episodes with elevated emissions.

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S15-O-06

qUANTIFICATION OF FOSSIL FUEL CO2 EMISSIONS FROM AN URBAN REGION: EARLY RESULTS FROM THE INDIANAPOLIS FLUX PROJECT (INFLUX)

TURNBULL J.(1), SWeeneY c.(2), GUenTHeR D.(2), KaRIon a.(2), neWbeRGeR T.(2), DaVIS K.(3), MIleS n.(3), RIcHaRDSon S.(3), laUVaUX T.(3), SHePSon P.(4), caMbalIZa M.o.(4), GURneY K.(5), SonG T.(5), RaZlIVanoV I.(5), leHMan S.(2), TanS P.(6)

(1) GnS Science, loWeR HUTT, neW ZealanD;(2) University of colorado, boUlDeR, UnITeD STaTeS;(3) The Pennsylvania State University, UnIVeRSITY PaRK, UnITeD STaTeS;(4) Purdue University, WeST lafaYeTTe, UnITeD STaTeS;(5) arizona State University, TeMPe, UnITeD STaTeS;(6) noaa/eSRl, boUlDeR, UnITeD STaTeS

AbstractEmissions of fossil fuel CO2 (CO2ff) from anthropogenic sources are the primary driver of observed increases in the atmospheric CO2 burden, and hence global warming. Quantification of the magnitude of fossil fuel CO2 emissions is vital to improving our understanding of the global and regional carbon cycle, and independent evaluation of reported emissions is essential to the success of any emission reduction efforts. The urban scale is of particular interest, since most CO2ff is emitted from urban regions, and cities are leading the way in attempts to reduce emissions.The Indianapolis Flux Project (INFLUX) aims to develop and assess methods to quantify urban greenhouse gas emissions. Indianapolis was chosen as an ideal test case since it has relatively straightforward meteorology; a contained, isolated, urban region; and substantial and well-known fossil fuel CO2 emissions. INFLUX incorporates atmospheric measurements of a suite of gases and isotopes including 14C from light aircraft (providing high spatial resolution) and from a network of existing tall towers (providing high temporal coverage) surrounding the Indianapolis urban area. The recently added CO2ff content is calculated from measurements of 14C in CO2, and then convolved with atmospheric transport models and ancillary data to estimate the urban CO2ff emission flux. Comparison with bottom-up CO2ff inventory estimates allows assessment of uncertainties in both the observational and inventory methods.This presentation will focus on the 14C sample collection and measurement for INFLUX. Significant innovations in sample collection include: collection of hourly averaged samples to average out very short term atmospheric variability; and collection of both upwind and downwind samples, so that background values can be accurately quantified. Our results show that CO2ff is consistently enhanced at the downwind site. Trace gases associated with combustion sources, such as CO, fossil fuel CO2, and hydrocarbons are well correlated with CO2ff. Total CO2 is also consistently enhanced in the downwind samples, even in summer. In winter, total CO2 enhancement is slightly higher than the fossil fuel CO2 enhancement, in agreement with Indiana’s requirement for 10% bioethanol use in gasoline.

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S15-O-07

RADIOCARBON ANALYSES OF DISSOLVED ORGANIC CARBON FROM ALPINE ICE CORE SAMPLES: METHODOLOGICAL APPROACH AND FIRST APPLICATION

MAY B.(1), HoffMann H.(1), WaGenbacH D.(1), PReUnKeRT S.(2), leGRanD M.(2), lIebl J.(3), STeIeR P.(3)

(1) Institute for environmental Physics, University of Heidelberg, HeIDelbeRG, GeRManY;(2) laboratoire de Glaciologie et Géophysique de l’environnement, ST. MaRTIn D’HÈReS, fRance;(3) VeRa laboratory, faculty of Physics, University of Vienna, VIenna, aUSTRIa

AbstractThe perturbation of the European aerosol budget by anthropogenic emissions is relatively well settled in view of inorganic species like major ions and heavy metals. Respective knowledge has been achieved by atmospheric monitoring, emission modeling, and, most convincingly, by Alpine ice core studies. However, much less is known in this field on the organic aerosol fraction where even the contemporary source mix is still a matter of debate. Although chemical analysis of a high-accumulation ice core from Col du Dôme (Mont Blanc region) revealed that the dissolved organic carbon (DOC) level has increased over the 20th

century by roughly a factor of two, attribution of the main cause for this observation remained ambiguous. Note that DOC is believed to constitute a proxy for the secondary organic aerosol fraction. Aimed at reducing this deficit we developed a method to analyze the radiocarbon signature of DOC extracted from Alpine ice cores. First DO14C quantifications have been made on selected samples from a Col du Dôme ice core which cover the last sixty years (i.e. a good deal of the nuclear bomb peak). Main steps of the radiocarbon analysis procedure comprise:

(i) bubble degassing of carbonate derived CO2,

(ii) UV-oxidation of dissolved organic substances to form CO2 which is again extracted by bubble degassing followed by cryogenic trapping,

(iii) AMS-analysis at the VERA facility (University of Vienna) of the manometrically quantified CO2 samples. The procedural extraction blank amounts to (1.90 ± 0.02) μgC with F14C = 0.74 ± 0.02 while the remaining ice contamination is estimated to add typically (4.1 ± 3) μgC with F14C = 0.70 ± 0.45. Radiocarbon analyses of DOC ice core samples are thus shown to be feasible down to some 20 μgC (corresponding, in the case of Alpine ice, to several 100 ml of meltwater). Results obtained so far on twelve DOC samples show the best correlation with the atmospheric 14CO2 record if a turnover time of the DOC source in the order of three years is assumed. This implies an only minor contribution from biomass burning. By simply considering only the living biosphere and fossil fuel combustion as relevant sources of DOC in the ice core (thus neglecting biomass burning), we arrive at a fossil fuel fraction of about 25% in summer samples of the 1940-1990 period. This finding is consistent with radiocarbon results we obtained from total organic aerosol sampled at the high Alpine Sonnblick Observatory.

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SESSION 16

ANTHROPOGENIC IMPACTS

ConvenersS. Ledizes (FRA), A. Pazdur (PoL)

DescriptionAnthropogenic impacts on the environment are a major cause of recent and significant changes in isotopic composition of carbon in modern atmosphere and biosphere. For example, human activities are changing the isotopic composition of atmospheric carbon mainly from burning fossil fuels, which increase the amount of stable carbon dioxide, and nuclear weapon tests, which are sources of additional 14C. Increased concentrations of stable and radioactive CO2 could also have a significant impact on the change of specific carbon activity in plants, even without climate change. Scientific characterization based on both field studies and laboratory experiments to measure 14C activity in terrestrial environmental samples and/or modeling approaches is crucial to understanding how such anthropogenic changes impact ecosystems. This session includes a wide range of CO2 and radiocarbon measurement techniques and/or modelling approaches used to determine the increased 14C activity caused by humans. Of particular interest are presentations that focus on the impacts of human activities resulting from fossil fuel and nuclear facilities - including reprocessing plants - that contribute to the increased 14C activities in atmosphere and biosphere. This theme, more commonly discussed in the context of plant physiology, agro-meteorology, soil sciences, hydrology and climatology, will be discussed with experts on isotope studies and 14C modelling (radio-ecology, model calibration and validation) allowing different scientific communities to exchange knowledge, data acquisition and/or modelling approaches.

Keywords14C activity, environment, human impact, modelling, data acquisition methods

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S16-INV-06

SOIL-PLANT-ATMOSPHERE MODELLING IN THE CONTEXT OF RELEASES OF 14C AS A CONSEqUENCE OF NUCLEAR ACTIVITIES

LIMER L.(1), KloS R.(2), WalKe R.(3), SHaW G.(4), noRDÉn M.(5), XU S.(5)

(1) limer Scientific consulting limited, neWTon-le-WIlloWS, UnITeD KInGDoM;(2) aleksandria Sciences limited, SHeffIelD, UnITeD KInGDoM;(3) Quintessa limited, HenleY-on-THaMeS, UnITeD KInGDoM;(4) University of nottingham, noTTInGHaM, UnITeD KInGDoM;(5) Strålsäkerhetsmyndigheten, STocKHolM, SWeDen

AbstractThe need to address radiological impacts from 14C released to the biosphere has been recognised for some time. However, because of its role in biological processes and its ecological cycling, the standard methods employed to model long-term radionuclide transport and accumulation in the biosphere cannot be used satisfactorily for 14C. The degree of complexity in any 14C model used must be balanced against the availability of supporting data and the assessment context.

Following SKB’s SAR-08 assessment of the SFR low- and intermediate-level waste facility at Forsmark, the importance of 14C in long-term dose assessments in Sweden has been re-emphasised (Thomson et al., 2008). 14C has also been important elsewhere to the extent that the international BIOPROTA forum has carried out a series of studies of 14C modelling. Outcomes from these studies indicate that the choice between dynamic and equilibrium assessment models is of particular interest, raising the issue as to whether dynamic models are useful and/or necessary. The complex processes governing carbon exchanges within the soil and between the soil and the atmosphere are not always well understood, and thus are difficult to represent appropriately in assessment models. Another difficulty surrounding the conceptual model for 14C concerns the identification of conditions under which mixing and isotopic equilibrium may reasonably be assumed.

In this study, a review of existing contemporary 14C models has been performed, considering models developed to assess operational and accidental releases of 14C from surface facilities and also those developed for safety assessments associated with the disposal of 14C-containing radioactive materials. Following on from this review a model, SSPAM14C, has been developed and is described herein. SSPAM14C has been applied to a data set from a study carried out at Imperial College London, which involved a series of experiments in which the 14C activity concentrations in a variety of plants were measured following an atmospheric release of 14C-labelled carbon dioxide (Tucker and Shaw, 1997). Some of these data have previously been used in the IAEA’s EMRAS programme (IAEA, 2008).

The results of this model review and development study are discussed with a view both to the need for further research and implications for model development.

References1. IAEA (2008). The Potato Scenario, Final Report. EMRAS Tritium/C14 Working Group, September 2008.2. Thomson G et al. (2008). Radionuclide Release Calculations for SAR-08. Swedish Nuclear Fuel and Waste

Management Company, SKB Report R-08-14. Stockholm.3. Tucker S and Shaw G (1997). Quality Assured Modelling Data for 14CO2 Fixation by Crops. IC.CARE/MAFF/

REP/C-14/4.0, Imperial College report to the Ministry of Agriculture, Fisheries and Foods, London, UK.

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173

S16-O-01

CONTINENTAL-SCALE ENRICHMENT OF ATMOSPHERIC 14CO2 FROM THE NUCLEAR POWER INDUSTRY: POTENTIAL IMPACT ON THE ESTIMATION OF FOSSIL FUEL-DERIVED CO2

GRAVEN H.(1), GRUbeR n.(2)

(1) University of california - San Diego, la Jolla, UnITeD STaTeS;(2) eTH Zurich, ZURIcH, SWITZeRlanD

AbstractDilution of atmospheric 14C/C ratios (Δ14C) by fossil fuel emissions provides a measurable signal that can be used to calculate the amount of fossil fuel-derived CO2 present and may allow emissions calculated by economic inventories to be validated using atmospheric observations. Dilution by fossil fuel-derived CO2 can be counteracted by 14C released during nuclear power generation and spent fuel reprocessing, however, requiring that nuclear sources are correctly accounted for. While this effect has previously been examined at local scales, we address the effect of nuclear sources on continental-scale gradients in Δ14C. To do so, we estimate annual 14CO2 emissions from individual nuclear sites and simulate the transport of emitted 14CO2 in the Eulerian TM3 transport model. We find that nuclear enrichment may offset at least 20% of the fossil fuel dilution in Δ14C over large regions of Europe, North America and East Asia. This corresponds to potential biases of more than −0.25 ppm in the CO2 attributed to fossil fuel emissions, larger than the bias from plant and soil respiration in some areas. Growth in nuclear emissions increased the simulated nuclear enrichment of Δ14C over 1985-2005, suggesting that nuclear emissions may bias apparent trends in fossil fuel-derived CO2. This presentation will summarize the work of Graven and Gruber (2011) and highlight a new database of annual 14CO2 emissions from individual nuclear sites that is available to the community.

ReferencesH. Graven and N. Gruber 2011, Continental-scale enrichment of atmospheric 14CO2 from the nuclear power industry: potential impact on the estimation of fossil fuel-derived CO2, Atmos. Chem. Phys., 11, 12339–12349, doi:10.5194/acp-11-12339-2011.

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S16-O-02

ASSESSING 14C TRANSFER FROM NUCLEAR FACILITIES TO GRASSLANDS ECOSYSTEMS: A MODEL EVALUATION IN THE VICINITY OF THE AREVA-NC REPROCESSING PLANT, LA HAGUE, NORTH FRANCE

le DIZeS S.(1), AULAGNIER C.(1), GonZe M.a.(1), MaRo D.(2), HebeRT D.(2)

(1) IRSn, ST PaUl leZ DURance, fRance;(2) IRSn, cHeRboURG-ocTeVIlle, fRance

AbstractRadiocarbon (14C) is naturally present in the atmosphere for about 240 Becquerel per kilogram carbon, but is also formed as a by-product of nuclear power generation, for example, by the AREVA-NC reprocessing plant, which releases about 10 tBq per year of 14CO2 in the environment. Estimating the transfer of 14C to ecosystems around nuclear power plants is then of national interest to check whether or not there is a contamination of the environment. The case of 14C is particularly important because carbon is very abundant in biological systems, can easily be incorporated into food webs via photosynthesis and has a long half-life. Consequently, increased environmental 14C specific activities may constitute an incremental radiation exposure to many environmental and anthropogenic systems. Carbon-14 concentration in terrestrial environment samples (air, grass, soil) is currently monitored on a monthly basis in five unmanaged grass fields around AREVA-NC, as part of AREVA environmental survey protocol. It has also been recorded monthly, along with sub-hourly atmospheric 85Kr specific activity, by an in-situ laboratory set up by the Institute for Radioprotection and Nuclear Safety (IRSN) on a managed pasture located 2 km downwind of the reprocessing plant, from 2006 to 2008. Krypton-85 and carbon-14 are released concomitantly by the reprocessing plant; relying on a quantitative relationship between their discharges rates, 85Kr is used to downscale 14C specific activities. This dataset offers a unique opportunity to test radioecology models independently to atmospheric dispersion models. The TOCATTA model developed by IRSN has thus been proven to be inappropriate in case of high-temporal frequency releases (Aulagnier et al., 2012), since it underestimates by nearly twice the grass 14C activity. The TOCATTA-khi model has then been developed as a possible alternative to TOCATTA. This new model has been tested against two independent but complementary datasets (from AREVA and IRSN). The simulated 14C activity is consistent with observations on both managed and unmanaged grass fields, but required a modification of the plant mean turnover time to account for different management. In the future, the TOCATTA-khi model could be extended to different terrestrial ecosystems like crops and vegetables. It may also be implemented within an operational tool, such as the SYMBIOSE modelling platform, which was co-funded by IRSN and Electricité de France as a reference tool for assessing doses induced by radioactive releases from nuclear facilities under accidental, decommissioning or normal operating conditions, and is to be used operationally starting from 2012.

ReferencesAulagnier, C., Le Dizès, S., Maro, D., Hebert, D., Lardy, R., Martin, R., and Gonze, M.-A., 2012. Modelling chronic and accidental releases of carbon-14 to the environment: A case study in a grass field near AREVA-NC La Hague. Journal of Environmental Radioactivity, submitted.

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S16-O-03

MONITORING OF CO2 EMISSION ON THE BASIS OF 14C AND 13C MEASU-REMENTS IN ATMOSPHERE AND BIOSPHERE IN SOUTHERN POLAND

PAZDUR A.(1), PaWelcZYK S.(1), PIoTRoWSKa n.(1), RaKoWSKI a.(1)(2), SenSUla b.(1), SaWIcKa n.(1), TUDYKa K.(1)

(1) Institute of Physics, GaDaM centre of excellence, Silesian University of Technology, Krzywoustego 2, 44-100 GlIWIce, PolanD;

(2) leibniz laboratory for Radiometric Dating and Stable Isotope Research, christian-albrechts-University, KIel, GeRManY

AbstractAs is shown in the IPCC (Intergovernmental Panel on Climate Change) report, the observed climate changes are caused, among others, by human activity. Mainly emission of CO2 to the atmosphere coming from the burning of fossil fuels, can have dire consequences for life on Earth and development of humankind. The report uses, among others, data obtained from isotopic measurements in the biosphere. Measurements of 14C and 13C concentration in modern atmospheric carbon dioxide and biosphere allow the determination of the decrease of the concentration of this isotope. Furthermore, the magnitude of emission to the atmosphere of carbon dioxide not containing the isotope 14C can be estimated on this basis. Such emission stems from fossil fuel combustion – petroleum, natural gas and black coal. A sensitive bioindicator of the emission are annual tree rings. The measurements of 14C concentration in tree ring material using AMS allow to see its seasonal changes.Trees, treated as an archive of changes in conjunction with information about the isotopic composition of carbon can be used for monitoring of environment as sensitive bioindicators on local, as well as on the global scale. Regular investigations of isotopic composition of carbon in trees have been carried out in the GADAM Centre for the urban areas of both Poland and worldwide. This method can be applied in the study of the emission of CO2 to the atmosphere and its spatial and temporal distribution connected with the production of energy by power plants based on fossil fuel combustion for the area of southern Poland. Modelling of CO2 emission using both 14C and 13C carbon isotopes measured in pine tree rings from Niepolomice Forest on the background of climatic changes will be presented.The national ecological policy in the era of global warming requires the manufacturers of energy to get involved in the development of methods suitable for monitoring the state of the environment. Hence, the interest in the area of monitoring the fossil fuel component in CO2 in our region is raising. The measurements of 14C (by AMS method) and 13C isotopes are being carried out in atmospheric CO2 and plants in the Gliwice city centre. A high decrease of both isotopes contents and their short-term seasonal changes during the year caused by human impact during the year are observed.

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S16-O-04

A COMPARISON OF DISTRIBUTION MAPS OF Δ14C FROM 2010 TO 2011 YEAR IN KOREA

PARK J., HonG W., PaRK G., SUnG K., lee K., KIM Y., KIM J., cHoI H., KIM G., Woo H., naKanISHI T.

KIGaM, DaeJeon, SoUTH KoRea

AbstractΔ14C values of leaves of a deciduous tree provide a means to map out regional scale fossil fuel ratio in air. We collected a batch of ginkgo (Ginkgo biloba Linnaeus, a deciduous tree) leaf samples in July from 2010 to 2011 in Korea to obtain the regional distribution of Δ14C. The Δ14C values of the samples were measured using Accelerator Mass Spectrometry (AMS) in KIGAM, Korea. Average of Δ14C values of Korea in 2011 becomes lower than that in 2011. The distribution maps of Δ14C in Korea were made using a batch of Δ14C values of Korea with Geostatistical and Spatial analyst tools in ESRI’s ArcMap software.The distribution maps of Δ14C shows that Δ14C values in western part of Korea is lower than those of eastern part of Korea. This is because a lot of industrial complex and population are in western part of Korea and westerly’s wind from China containing fossil fuel CO2 flows in Korean. We compared the distribution maps from 2010 and 2011 and tried to find traces of Fukushima power plant accident.

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S16-O-05

ESTIMATION OF THE ORDER OF 129I/127I RATIO AT SOIL SURFACE BEFORE THE FUKUSHIMA DAIICHI NPP ACCIDENT BY RADIOCARBON MEASUREMENT

MATSUZAKI H.(1), TSUcHIYa S Y.(1), HonDa M.(2), YaMaGaTa T.(2), MIYaKe Y.(1), MaeJIMa Y.(3), oHKURa T.(3), MURaMaTSU Y.(4)

(1) The University of Tokyo, ToKYo, JaPan;(2) nihon University, ToKYo, JaPan;(3) nIaeS, TSUKUba, JaPan;(4) Gakushuin University, ToKYo, JaPan

AbstractFor the reconstruction of 131I level in the region around the Fukushima Daiichi NPP just after the accident, detailed 129I distribution has to be measured. However the anthropogenic 129I had already been existed even before the accident at a certain level due to the emission from the spent nuclear fuel reprocessing plants all over the world (especially in Europa) [1]. To distinguish the accident origin 129I, this “background” level should be evaluated. Matsuzaki et al. (2010) showed the correlation between 129I/127I and 14C/12C in the undisturbed surface soil layer[2]. Considering such correlation, 129I/127I ratio at soil surface before the accident can be estimated by measuring 14C/12C. If 14C/12C is well below the modern, that surface should have been disturbed or well mixed before the accident and the 129I/127I should have been well low, thus more clearly we could see the accident origin 129I signal.

References[1] Y. Muramatsu, Y. Takada, H. Matsuzaki, S. Yoshida, 2008, AMS analysis of 129I in Japanese soil samples

collected from background areas far from nuclear facilities, Quaternary Geochronology 3, 291-297.[2] H. Matsuzaki, Y.S. Tsuchiya, Y. Muramatsu, Y. Maejima, Y. Miyairi, K. Kato, 2010, Comparison of depth

profiles of 129I and 14C concentrationin the surface layer of soils collected from Northeastern Japan, Radiocarbon 52, Nr 2-3, 1487-1497.

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SESSION 17

14C TRACER OF LIFE

Convenersm.J.I. Briones (ESP), J. Vogel (USA)

DescriptionThis session seeks papers and discussions of the use of 14C and other isotopes, natural or anthropogenic, to the study of current living members of the plant and animal kingdoms, from humans to fungi. The primary connection among possible topics is use of isotopic signals to distinguish the metabolic paths and compositional sources within living systems. In particular we welcome those studies investigating the ecology of organisms in soils and sediments, nutrient sources in extremophile environments, regeneration of physiological isolates («bomb pulse» dating) and tracing isotope labeled compounds in humans, animals and plants. Distinct isotopic sources include the Earth’s surface biosphere, isotope-depleted reservoirs, anthropogenic isotope excursions, and intentionally isotope-labeled products (e.g. quantification of nutrient or pharmaceutical metabolism and distinction of natural versus manufactured components).

Keywordsecology of dwelling organisms, living system, metabolism, nutrient, regeneration, extremophile, pharmaceutical, isotope-labeled

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S17-O-01

LIFE SCIENCE APPLICATIONS UTILIZING RADIOCARBON TRACING

SALEHPOUR M., HÅKanSSon K., PoSSneRT G.

Physics and astronomy, UPPSala, SWeDen

AbstractThe life science research in our laboratory is mainly centred on radiocarbon as a tracer, in conjunction with the Uppsala University Tandem Accelerator Laboratory facilities, including a 5 MV Pelletron tandem accelerator and two stable isotope ratio mass spectrometers. A dedicated sample preparation laboratory for biological samples with natural activity is used routinely, as well as a second laboratory specifically for labelled samples with elevated levels of carbon-14. A variety of collaborative projects are presented.Examples are:

1) Ultra-small sample AMS. We routinely analyse samples below 10 microgram C. Data is presented regarding the sample preparation method,

2) Bomb peak Biological dating of ultra-small samples. A long term project is presented where purified and cell-specific DNA from various part of the human body including the heart and the brain are analyzed with the aim of extracting regeneration rate of the various human cells,

3) Bomb peak biological dating of various human biopsies, including surgically removed atherosclerosis related plaques and triglycerides from human fat tissues,

4) In addition to clinical phase-0 microdosing measurements using small pharmaceutical drugs, pre-clinical pharmacokinetic data from a macromolecular drug candidate is presented,

and 5) Forensic dating of teeth is also addressed.

Other radiocarbon applications are being pursued using the laser based intracavity optogalvanic spectroscopy which is described in a separate paper in these proceedings.

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S17-O-02

DIET INFLUENCE OF BOMB-PULSE DATING ON HUMAN PLAqUE SAMPLES

GEORGIADOU E.(1), STenSTRÖM eRIKSSon K.(1), GonÇalVeS I.(2)(3), nIlSSon J.(3)

(1) lund University, Department of Physics, Division of nuclear Physics, lUnD, SWeDen;(2) Department of cardiology, Skåne University Hospital, MalMÖ, SWeDen;(3) cardiovascular Research Group, Institution for clinical Sciences, MalMÖ, SWeDen

AbstractBomb-pulse radiocarbon effect, caused by the excessive atmospheric testing of nuclear weapons, in the middle of 20th century, opened new horizon in the radiocarbon dating method.This technique can be used nowadays to provide information e.g on the formation of new cells and on the staring date of a disease in the human body.In 2010, different parts of plaque were sampled from 20 patients. Their 14C and stable isotopes, 13C and 15N, content were analyzed.Radiocarbon dating of the samples can provide useful information about the date of formation of the plaque fractions that the samples originating from.Besides, stable isotope analysis can give insight to the diet of the subjects, taking under consideration the originating plaque fraction and e.g. its fat and calcium content. The use of this diet information to correct the radiocarbon dating results of the samples is under discussion.

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S17-O-03

RADIOCARBON ANALYSIS OF TREE RINGS FROM CAMEROON

TANDOH J.B.(1)(2), MaRZaIolI f.(1)(2), PaSSaRIello I.(1)(2), caPano M.(3)(2), TeRRaSI f.(1)(2), MaRcHeTTI M.(4), laSSeRRe b.(4), ValenTInI R.(5), caSTalDI S.(1)

(1) Seconda Università di napoli, Dipartimento di Scienze ambientali, caSeRTa, ITalY;(2) InnoVa, cIRce (centre for Isotopic Research on cultural and environmental Heritage), caSeRTa, ITalY;(3) Seconda Università di napoli, Dipartimento di Studio delle componenti culturali del Territorio, S. M. c. VeTeRe ce, ITalY;(4) laboratorio di ecologia e Geomatica forestale Dipartimento di Scienze e Tecnologie per l’ambiente e il Territorio, PeScHe

(IS), ITalY;(5) University of Tuscia Department for innovation in biological, agro-food and forest systems (DIbaf), VITeRbo, ITalY

AbstractRadiocarbon measurements have been obtained for three different tree species namely Entandrophragma cylindricum (Sapele), Erythrophleum suaveolens (Tali) and Triplochiton scleroxylon (Ayous) from Cameroon using Accelerator mass spectrometry (AMS) at CIRCE laboratory in Caserta (Italy). The study site is a natural semi-deciduous forest in the southwest province of Cameroon located between 4°53’ to 5°28’ N and 8°42’ to 9°16’ E and situated at about 100km from Mt Cameroon volcano area.This study sought to discuss three pertinent issues of radiocarbon applications in climate studies:

- to use radiocarbon measurements to test the annual nature of growth rings from three different tree species

- to identify the response of individual tree species to climatic stress factors which mostly results in missing growth rings

- to relate these stress factors to the growth rates of individual species and local climate data from study site

Calibrating the radiocarbon dates obtained for the three species with the Southern Hemisphere radiocarbon calibration curve (Hua and Barbetti, 2004) revealed a shift of several years with respect to the average bomb spike data which, in the case of Entandrophragma cylindricum (Sapele) and Erythrophleum suaveolens (Tali), is increasing with increasing ring number. These observed shifts raised questions about the annual nature of the growth rings of these species. Climatic anomalies which can severely affect tree growth at certain seasons become the prime candidate for causing missing growth rings. We plotted the cumulative number of missing rings as a function of the 14C calibrated year. To extract climatic information from the missing ring data, a distribution of the number of missing rings per year as a function of calibrated year is derived by numeric differentiation and compared with climatic records and with the growth rates of all species in terms of ring widths and ring densities. This comparison will better explain how different tree species react to climatic conditions which also affect the growth.

ReferencesHua Q, Barbetti M. 2004. Review of tropospheric bomb 14C data for carbon cycle modeling and age calibration purposes. Radiocarbon, Vol 46, Nr 3, 2004, p 1273–1298

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SESSION 18

COSMOGENIC NUCLIDES

ConvenersD. Fink (AUS), S. Ivy-ochs (CHE), A.J.T. Jull (USA), W. Zhou (CHN)

DescriptionThis session will highlight new developments and improvements to cosmogenic radionuclide measurements (14C, 10Be, 26Al, 36Cl, etc). In the last 25 years, the development of measurements of cosmogenic nuclides produced in situ has gone from a simple idea to a wide variety of applications. The development of in-situ 14C is an excellent example. There are also related studies such as atmospheric 10Be in marine and non-marine sediments. In parallel, there has been a development of long-lived nuclear tracers, such as 129I for a rather different application of oceanic tracer studies.Themes:• Advances in in situ 14C techniques; • Applications of in situ 14C produced in terrestrial, extraterrestrial and ice samples • Improved chemical procedures in sample preparation and AMS measurements related to cosmogenic-nuclide studies. • Exposure dating of rock surfaces and sediment using cosmogenic nuclides; • Dating of soil and loess deposits using atmospheric 10Be • New applications including basin-wide erosion rate determinations, weathering and soil burial ages. • Archaeological applications of in situ cosmogenic nuclides. • Marine tracers

Keywordscosmogenic 14C, cosmogenic radionuclides, surface exposure dating, erosion, burial

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S18-INV-01

COMBINING IN SITU COSMOGENIC 14C AND 10Be ANALYSIS TO STUDY COMPLEX SURFACE PROCESSES AND EXPOSURE HISTORIES

HIPPE K.(1), KobeR f.(1), IVY-ocHS S.(1), WacKeR l.(1), KUbIK P.(1), ScHlÜcHTeR c.(2), WIeleR R.(1)

(1) eTH Zürich, ZÜRIcH, SWITZeRlanD;(2) University of bern, beRn, SWITZeRlanD

AbstractThe past decade has seen significant improvements to the analysis of in situ cosmogenic 14C. Routine in situ 14C extraction from quartz samples has been achieved but the range of possible applications in Earth surface sciences has just started to get fully explored. Because in situ 14C is sensitive to short-term surface cover or recent changes in geomorphic process rates, it allows to unravel complex exposure histories when combined with a long-lived isotope (e.g. 10Be).We present two examples that have used the in situ 14C-10Be nuclide pair to investigate largely different questions in geomorphology and geochronology:For the first study in situ 14C, 10Be (and 26Al) have been analysed in fluvial sediments from the eastern Altiplano, Bolivia, to evaluate and quantify denudation processes and sediment transfer times. Concentrations of the long-lived nuclides imply consistently low catchment-wide denudation rates and are in good agreement with published modern sediment yields. These results suggest long-term (since the late Pleistocene) geomorphic and isotopic steady-state conditions for the eastern Altiplano and are consistent with the low topographic gradients on the eastern Altiplano. Low concentrations of in situ 14C disagree with a simple exposure history and indicate that in situ 14C has decayed due to significant sediment storage lasting at least throughout the Holocene. Results for in situ 14C reflect the episodicity of fluvial processes (storage and remobilisation) on the eastern Altiplano and highlight the potential of in situ 14C to investigate sediment routing within fluvial systems. In this context, the influence of soil-mantled hillslopes on the in situ 14C concentration in slowly eroding landscapes will also be discussed.In the second study 10Be and in situ 14C were combined to reconstruct the deglaciation history of the Gotthard Pass, Central Swiss Alps, by exposure dating of bedrock surfaces. Results from both nuclides are overall in good agreement with each other confirming continuous exposure of the Gotthard Pass area throughout the Holocene. Slightly younger in situ 14C ages compared to the corresponding 10Be ages are interpreted to result from partial surface shielding due to snow cover. Thus, in situ 14C can be used to constrain the average Holocene snow depth. Integrating the snow-corrected exposure ages with detailed field studies allows to identify a gradual re-organization of the paleo-ice flow pattern and to trace the progressive downwasting of glaciers in the Gotthard Pass area throughout the Alpine Lateglacial. However, from the observation that few in situ 14C ages are slightly older than the 10Be ages, it is further suggested that the currently accepted in situ 14C production rate might be underestimated.

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S18-O-02

HIGH-PRECISION MEASUREMENTS OF IN-SITU COSMOGENIC 14C IN NATURAL GLACIER ICE FROM GREENLAND AND ANTARCTICA

PETRENKO V.(1), SeVeRInGHaUS J.(2), SMITH a.(3), ScHaefeR H.(4), RIeDel K.(4), baGGenSToS D.(2), HaRTH c.(2), oRSI a.(2), HUa Q.(3), baUSKa T.(5), bRooK e.(5), eManUele G.(2), fRanZ P.(4), TaKeSHITa Y.(2), lee J.(5), bRaIlSfoRD G.(4), WeISS R.(2), bUIZeRT c.(6), DIcKSon a.(2), KeelInG R.(2)

(1) University of Rochester, RocHeSTeR, UnITeD STaTeS;(2) Scripps Institution of oceanography, University of california San Diego, la Jolla, UnITeD STaTeS;(3) australian nuclear Science and Technology organisation, KIRRaWee Dc, aUSTRalIa;(4) national Institute of Water and atmospheric Research ltd, WellInGTon, neW ZealanD;(5) oregon State University, coRVallIS, UnITeD STaTeS;(6) centre for Ice and climate, University of copenhagen, coPenHaGen, DenMaRK

AbstractWe present measurements of in-situ cosmogenic 14C (in the forms of 14CO2,

14CO and 14CH4) in natural glacier ice from Greenland and Antarctica. Very large (~1000 kg per sample) amounts of ice were sampled, allowing for unprecedented precision and detection limits for in-situ 14C. The first set of measurements is from shallow (3 - 6 m) firn (consolidated snow) at Summit, Greenland. Most prior measurements from Summit ice and firn have found large amounts of in-situ cosmogenic 14C, suggesting that this 14C is well retained in the ventilated porous firn. Our results, on the contrary, suggest that very little (<1%) in-situ cosmogenic 14C is retained in Summit shallow firn. This very low retention rate of in-situ cosmogenic 14C in the upper firn suggests that 14CO2 can be used as an absolute dating tool for ice cores.The second set of measurements is from shallow (2 – 20 m), ~50 kyr old ablating ice at Taylor Glacier, Antarctica. 14CO was quantified to ~2% relative uncertainty and showed the quasi-exponential decrease with depth that is expected from ablation-zone 14C production. Both sets of measurements succeeded for the first time in detecting a small in-situ cosmogenic 14CH4 component, which was quantified with a precision as low as 0.01 molecules / gram ice. The Taylor Glacier measurements suggest a constant 14CH4 /

14CO partitioning of 0.0078 for 14C production by muons, and a higher value for production by neutrons. These measurements demonstrate that a reliable correction for the in-situ cosmogenic component of 14CH4 in ice is possible, allowing for accurate reconstructions of paleoatmospheric 14CH4. Paleoatmospheric 14CH4 measurements would allow to determine the fossil component of the past atmospheric CH4 budget as well as to test the hypothesis that marine methane clathrates release CH4 to the atmosphere during times of warming.Our melt-extraction technique is not well suited for precise 14CO2 determinations, mainly because of interfering CO2 produced from carbonates and organics in the ice upon melting. More approximate determinations, however, are possible and allow for constraints on the total in-situ 14C content in Taylor Glacier ice. These estimates suggest that the currently used muon 14C production rates may be overestimated by a factor of 2 or more.

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S18-O-03

BERYLLIUM ISOTOPES IN HALITE AND THE AGE OF THE SEDOM FORMATION, ISRAEL

BELMAKER R.(1), TePelYaKoV n.(2), beeR J.(3), cHRISTl M.(4), laZaR b.(1), STeIn M.(2)

(1) Hebrew University of Jerusalem, JeRUSaleM, ISRael;(2) Geological Survey of Israel, JeRUSaleM, ISRael;(3) eaWaG, Swiss federal Institute of aquatic Science and Technology, DUebenDoRf, SWITZeRlanD;(4) laboratoty of Ion beam Physics, eTH, ZURIcH,, SWITZeRlanD

AbstractPliocene-Pleistocene saline deposits that lack conventionally datable material (i.e. biostratigraphic markers or igneous material) are difficult to directly date. However, due to its half-life (T1/2: 1.39 Ma), the cosmogenic isotope 10Be may potentially serve as a dating tool for such deposits. In this study we assessed the feasibility of this dating tool by measuring beryllium isotopes (9Be, 10Be and 7Be, the short-lived “brother” of 10Be T1/2: 53.3 d) and major elements (Ca, Mg, Br, Cl) in contemporary halite deposits (i.e. Dead Sea and saltpan halite) and ancient halite deposits of the Sedom and Amora formations, Israel.

The measurements in contemporary halite enabled us to:

(a) determine whether beryllium is incorporated into halite via entrapment of settling dust or by co-precipitation of dissolved beryllium and primary sediment and to

(b) evaluate the beryllium halite-brine partition coefficient (D). The measurements in ancient halite enabled us to test the use of 10Be as a halite chronometer. Our work presents one of the first measurements of 10Be in marine halite and evaluates for the first time the partition coefficient of beryllium towards halite.

Our results demonstrate that:

(a) the source of beryllium isotopes in the halite is predominantly dissolved beryllium,

(b) the halite-brine partition coefficient of beryllium lies between 3-10 i.e. beryllium is highly compatible towards halite,

(c) the initial (prior to decay)10Be concentration in halite is seemingly constant over various geographical locations. The 10Be-ages we determined for the Sedom Formation salts lie between ~3 to ~ 5 Ma and are consistent with previous independent age estimates of the Sedom Formation. Thus, it appears that 10Be can be used as a halite chronometer of late mid to late Neogene evaporitic water-bodies.

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S18-O-04

NEW CONSTRAINTS ON THE CHAUVET CAVE ARTWORK ELABORATION

SADIER B.(1), DelannoY J.J.(1)(2), beneDeTTI l.(3), boURlÈS D.l.(3), JaIlleT S.(2)(1), GeneSTe J.M.(4), aRnolD M.(3), lebaTaRD a.É.(3)

(1) laboratoire eDYTeM, cnRS, Université de Savoie, le boURGeT DU lac, fRance;(2) cnRS, le boURGeT-DU-lac, fRance;(3) aix Marseille Univ. ceReGe UMR cnRS 7330, aIX en PRoVence, fRance;(4) centre national de la Préhistoire, PeRIGUeUX, fRance

AbstractSince its discovery, the Chauvet cave elaborate artwork called into question our understanding of Palaeolithic art evolution and challenged traditional chronological benchmarks(1,2).Chronological approaches revealing human presences in the cavity during the Aurignacian and the Gravettian are indeed still debated on the basis of stylistic criteria(3,4). The presented 36Cl Cosmic Ray Exposure ages demonstrate that the cliff overhanging the Chauvet cave has collapsed several times since 29 ka until the sealing of the cavity entrance prohibited access to the cave at least 21 ka ago. Remarkably agreeing with the radiocarbon dates of the human and animal occupancy, this study confirms that the Chauvet cave paintings are the oldest and the most elaborate ever discovered, challenging our current knowledge of human cognitive evolution.

References1. Clottes, J.et al. (1995) Les peintures paléolithiques de la grotte Chauvet à Vallon Pont d’Arc (Ardèche, France);

datations directes et indirectes par la méthode du radiocarbone. c.R. acad sciences Paris 320: 1133 - 1140.2. Valladas, H.et al. (2001) Evolution of prehistoric cave art. nature 413: 479.3. Pettitt, P. (2008) Art and the middle-to-upper Paleolithic transition in Europe: comments on the archeological

arguments for an early Upper Paleolithic antiquity of the grotte Chauvet Art. J of Hum. evol. 55: 908 – 9174. Alcolea, J. and R. de Balbin (2007). 14C and style - The chronology of the Upper Paleolithic art at present.

L’anthropologie, 111: 435 - 466

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SESSION 19

UNUSUAL APPLICATIONS OF 14C MEASUREMENT

ConvenersI. Hajdas (CHE), G. Hodgins (USA)

DescriptionSometimes radiocarbon projects are like detective stories. Often the ‘bomb peak’ is central to such cases, however, measurements of natural radiocarbon levels and admixtures of bomb and fossil C can also provide interesting testimony. We would like to call for papers that utilize either C signal (‘bomb’ or ‘natural’ 14C) to address questions of authenticity or forgery in museum studies, forensic, food, environmental or medical sciences, or other novel applications. Moreover, studies that provide ‘unexpected’ radiocarbon dating results that might lead to new interpretations of historical records would be of interest. We invite papers that present such studies from the whole range of 14C ages and disciplines.

Keywords14C dating, applications, 14C bomb peak, fossil C, authentic, fraud, forensic, environmental, historical, food, medical

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S19-INV-01

RADIOCARBON DATING OF PEARLS

KRZEMNICKI M.S.(1), HaJDaS I.(2), bonanI G.(2), WacKeR l.(2)

(1) Swiss Gemmological Institute SSef, baSel, SWITZeRlanD;(2) laboratory of Ion beam Physics, eTH, ZURIcH, SWITZeRlanD

AbstractSince historic times, pearls are ranking among the most appreciated gems and until nowadays they are widely used in jewellery. With the development of pearl cultivation in the early 20th century, and further cultivation progress in the last 30 years, pearls have gained even more importance in the international jewellery trade.Pearls are calcium carbonate concretions, formed by biomineralisation processes in a wide range of freshwater and saltwater molluscs. To maintain the confidence of the consumer in this product, it is one of the main tasks of commercial gemmological laboratories to identify pearls, i.e. to distinguish natural pearls from cultured pearls and from pearl imitations. A pearl identification is commonly based on radiography, X-ray luminescence and X-ray computed µ-tomography, apart from microscopic examinations. Especially for historic pearl jewellery, it would be highly interesting to have access to the age of the pearls, thus to be able to confirm the historic provenance of the item or to unveil a more recent forgery.For this study, we investigated the feasibility of radiocarbon age dating of pearls, using the AMS at the ETH Zurich. We selected a small number of pearls of different ages (from 2001 to late 17th century) and shells of documented historic provenance (from early 20th to mid 17th century). Preliminary results show, that age determination of pearls is possible in principle, especially for pearls of recent ages, using the “bomb-peak” as a reference. However, the historic freshwater shells (collected from rivers and lakes in Switzerland) revealed a distinct shift of the determined radiocarbon age towards much older ages than the real formation of the shell, which is caused by the presence of old carbonates dissolved in water (reservoir effect). Preliminary results of this study will be presented and an outlook of their relevance for commercial pearl testing.

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S19-O-02

PRESENT-DAY RADIOCARBON CONTENT OF SELECT FLAVORING COMPOUNDS REVEALS VANILLIN PRODUCTION PATHWAY

CULP R., PRaSaD G.V.R.


AbstractRadiocarbon and stable isotope determination in foods, flavors and beverages, for the authentication of source material and process of formation, is a well-established method of identity used in industry. New methods of provenance determination, using stable isotopes of oxygen and hydrogen, have added to the host of other isotopic methods used for characterizing natural or botanically derived products. The unambiguous determinant of a product’s fossil fuel origin be it from petroleum, natural gas or coal, is through the measurement of its radiocarbon content. The absence of 14C confirms a fossil fuel derivation. The 14C content can also be used to determine the fraction dilution of recently grown and harvested material with that derived from fossil fuel, and even confirms the vintage of agricultural products based on the well-established decrease of bomb-produced atmospheric 14C. For this purpose, the present-day 14C activity, taken up by agricultural products, should be accurately defined. This paper documents 14C measurements at the University of Georgia’s Center for Applied Isotope Studies accelerator mass spectrometry and stable isotope laboratories, over the last 3 years, for ten important flavoring compounds. This data expands on, and appends, previous work documenting 14C activity levels in botanically derived products over more than twenty years. By establishing an accurate and current level of 14C in botanically derived products, we were able to confirm a particular source for vanilla production, the most popular consumer flavor in the marketplace. Over the years, vanilla extract has been produced less and less from vanilla beans (eg. Vanilla planifolia), particularly those from Madagascar and the Comoros Islands, and more from other botanical precursors such as ferulic acid, clove oil and guaiacol. Although the term “natural” vanilla has been reserved for vanillin derived from vanilla beans, other non-vanilla bean sources can evade detection by the 14C method since they are also from a recent botanical source. Vanillin derived from lignin, the structural component of coniferous trees, and previously a minor production pathway for vanillin, has increased in occurrence. Because lignin is from pulpwood, derived from the entire tree, the 14C content is the average of the yearly growth rings over the life span of the tree, including bomb-produced 14C still in the atmosphere. We reveal here, isotopic data to support this precursor for vanilla production based on high 14C levels accumulated during the tree’s life, incorporated in the tree rings and their associated stable isotope abundances.

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S19-O-03

MEASUREMENT OF 14C CONCENTRATION IN DISTILLED ETHANOL FROM WINE TO MONITOR GLOBAL DISTRIBUTION OF 14C

naMaI S.(1), SAKURAI H.(2)(1), TaKaHaSHI Y.(1), SaTo T.(1), InUI e.(3), MaSUDa K.(4), ToKanaI f.(2)

(1)(3), KaTo K.(3), KURIYaMa Y.(5), SHIbaTa K.(1)

(1) Graduate School of Science and engineering, Yamagata University, YaMaGaTa, JaPan;(2) Dept. of Physics, Yamagata University, YaMaGaTa, JaPan;(3) faculty of Science, Yamagata University, YaMaGaTa, JaPan;(4) STe lab, nagoya University, aIcHI, JaPan;(5) Dept. of Material and biological chemistry, Yamagata University, YaMaGaTa, JaPan

AbstractIt is still interested in investigating the global distribution of 14C concentrations in the atmosphere, although the 14C concentrations are well mixed with air-mass circulation between the troposphere and the stratosphere for the Northern and Southern hemispheres, and by carbon circulation system. In particular, however, the extent of locality for the 14C concentrations is not well known including urban effects due to fossil fuel etc. 14C produced by cosmic rays are different in the production rates for the geomagnetic latitudes because of the cut-off rigidity to incoming cosmic rays. These 14C are diffused in the atmosphere with a time constant. Another 14C are residuum from the atmospheric nuclear bomb tests. Although these 14C are spread out from the Northern hemisphere to the Southern hemisphere, tree rings data of 14C are shown similar concentrations for both the hemispheres.However, we have attempted to check the global distribution of 14C concentrations saving work and cost by commercially distributed wine. It is because the sampling is easy and same chemicals of ethanol are distilled from the wine sample. Moreover, the liquid scintillation counting method is advantageous to measure the 14C concentrations in the distilled ethanol because of its liquid condition.We have realized the ethanol concentrations of 99% by twice distillations and the elimination of water content using zeolite. It is similar to the manufactured ethanol purification. The 14C concentrations in the ethanol are fluctuated in the relative standard deviation of 0.5% for the distilled samples indicating the similar fluctuation to the counting statistics. The 14C concentration of a wine produced in Chilly was 5.6 cpm per 1g ethanol compared with 5.9 cpm for manufactured ethanol.We will describe the motivation measuring wines, the development of the distillation of ethanol and the purification, and a comparison between the Japanese and southern hemisphere wines.

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S19-O-04

RADIOCARBON MEASUREMENTS ON SILVER GELATIN PRINTS ATTRI-BUTED TO THE AMERICAN PHOTOGRAPHER LEWIS HINE (1874-1940)

HODGINS G.(1)(2), RoSenSTeIn D.D.(2), faIRbanKS-HaRRIS T.(3)

(1) nSf-arizona aMS laboratory, University of arizona, TUcSon, aRIZona, UnITeD STaTeS; (2) School of anthropology, University of arizona, TUcSon, aRIZona, UnITeD STaTeS;(3) Yale center for british art, Yale University, neW HaVen, connecTIcUT, UnITeD STaTeS

AbstractWe are investigating the dynamics of atomic bomb-derived radiocarbon uptake into the organic components of photographs, namely the paper support and the protein-based emulsion layer. The initial motivation of this research was to develop a method to date fine art photographs. Original prints by famous early 20th Century photographers such as Ansel Adams, Henri Cartier-Bresson, and Dorothea Lange are highly valued. The reproductive nature of the photographic process makes it amenable to forgery. Two known examples of this were the forgeries of numerous prints by Man Ray (1890-1976) and Lewis Hine (1874-1940). Many experts believe the problem of fine art photograph forgery is wide spread. Measuring bomb-derived radiocarbon in photographs for dating purposes is a complement to existing approaches that cannot produce absolute results.In investigating the Hine forgeries, photograph conservator Paul Messier (Messier et al. 2005) exploited a technological change in the composition of photographic paper that occurred in the 1950’s, namely the inclusion of optical brighteners. Messier demonstrated the presence of optical brighteners in photographs purportedly printed by Hine himself, who died in 1940, and thus confirmed acts of forgery.Previously, we developed methods for isolating photographic paper and emulsion carbon, and through measurements on known-age photographs demonstrated that emulsion radiocarbon content tracks the atmospheric radiocarbon levels throughout the late 20th Century more closely than paper. Moreover paired emulsion and paper measurements can actually date when photographic materials were produced, rather than simply indicate they are post-1955, as is the case with optical brighteners.We measured paper and emulsion radiocarbon content in two photographs attributed to Lewis Hine. One print is solidly attributed to Hine, while the other, though a well-known image bearing the Hine Studio stamp on the reverse, was printed on paper containing optical brighteners. The implication is that it was probably printed after Hine’s death. Here we report on these measurements, and compare them with our data set of radiocarbon measurements on known-age, late 20th Century photographic papers.

ReferencesMessier P, Baas V, Tafilowski D, and Varga, L (2005) Optical Brightening Agents in Photographic Paper Journal of the American Institutes for Conservation 44(1):1-12.

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S19-O-05

RADIOCARBON AS MARKER OF CHANGES FOR RADIOLOGICAL SITUATION IN THE LADOGA LAKE WATER SYSTEM

KULKOVA M., neSTeRoV e.

Herzen State University, ST.PeTeRSbURG, RUSSIan feDeRaTIon

AbstractThe concentration of radiocarbon is at high level in the environment after nuclear tests of 1950-1960 years till now. The most of technogenic radiocarbon is emitted in result of neutron activation of fuel admixture and heat-transfer material in the Nuclear Power Plant. The most part of DNA damage in animal and human bodies in result of decay 14C nuclei lead to genetic mutations. In period of 1945-1980 years in result of the nuclear tests about 2,2 · 1017 Bq 14C was emitted in the atmosphere. It is in 1,6 time higher than the natural radiocarbon equilibrium activity in the troposphere.The investigations of distribution of long-life radionuclide 14C in the water were conducted in the regions of Gulf of Finland and Ladoga Lake basins. In the Gulf of Finland the Leningrad (Sosnovy Bor) Nuclear Power Plant, the depositories of radioactive waste is situated. The atomic submarines and ships are repairing on the coastal parts. The automatic system for sample preparation Sample Oxidizer 307 and low background scintillation counting Quantulus 1220 were used for determination of radiocarbon activity in water.Ladoga Lake is a freshwater lake located in the Republic of Karelia and Leningrad district in northwestern Russia, not far from St.Petersburg. It is separated from the Baltic Sea by the Karelian Isthmus and it drains into the Gulf of Finland via the Neva River. It is the only river flows out of Lake. The biggest rivers flow in of Lake are Svir’, Volkhov, Syas’. The Tikhvin Water System was built at 1811 year on the Syas’ River. This was one of main artificial water ways connecting Volga River and Baltic Sea through Tikhvin connecting channel, at Syas’ River, Ladoga Lake and Neva River. The Tikhvin Water System consisted of seven big artificial gateways and fifty small artificial gateways which were connected by channel. Unlike from other artificial water systems the Thikhvin Water gateways worked in both directions. At 1966 year the Tikhvin Water System was closed. Our investigations have showed the increased radiocarbon activity in the water of Syas’ River basin in comparison with other river basins of Southern region of Leningrad district. In this region there have no any radiation hazardous facilities. The increased radiocarbon activity was registered in the water of Ladoga Lake near Konevez, Makarinsaari, Heynjasenmaa, islands. At 1950-1960 years the military facilities have been located here and the tests of weapons have been conducted. The artificial Tihkvin gateway system contributed to inflow of water with the high level of radiocarbon in Syas’River basin from Ladoga Lake. So, the artificial water constructions have became the cause of radionuclide contamination of environment. The radiocarbon is the good marker for sources of radionuclide contamination of environment.

AcknowledgementsThe researchers are supported by project FCP N 1156 «The scientific and scientific-pedagogical specialists of innovation Russia, 2009-2013».

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193

S19-O-06

DETERMINATION OF THE BIO-BASED CONTENT IN PLASTICS BY RADIO- CARBON

CALCAGNILE L.(1), GIffonI M.(2), QUaRTa G.(1), bRaIone e.(1), D’elIa M.(1)

(1) ceDaD,, DePT. of enGIneeRInG of InnoVaTIon, UnIVeRSITY of SalenTo, lecce, ITalY; (2) Polynt S.p.a., San GIoVannI ValDaRno, ITalY

AbstractFollowing the need of reducing the CO2 emissions into the atmosphere, international protocols have been introduced which aim to promote the use of products of biogenic origin. The development of fast, accurate and reliable experimental methods for the determination of the biogenic fraction in carbon-based industrial products such as polymers is thus an active research field. The use of the radiocarbon dating method for this purpose, quite simple in its basic principle, is based on the large difference in the 14C isotopic signature between the fossil-derived (not containing 14C) and the biogenic component of C-based materials, whose radiocarbon content reflects, in a first approximation, modern 14C atmospheric levels. In particular, in the chemical industry, a relevant interest exists on the possible use of this approach as a fast and reliable protocol for the assessment of the “bio-based” content in raw materials as well as for the certification of finished products. In order to assess the precision and accuracy levels achievable by this approach different polyester resins were produced by mixing materials with certified values of the biogenic components and with an expected bio-content ranging from 0 (fully fossil material) to 100 % (fully biogenic materials). In order to exclude possible sources of uncertainty the biogenic content was previously determined in some of the components used during the synthesis and namely succinic acid, monopropylene glycol and styrene. Furthermore the analyses were also carried out by sampling the resins both in the liquid and in the solid forms, after the catalytic polymerisation reaction. The results, demonstrates overall the high reliability of the method but has also highlighted some possible uncertainty sources and possible drawbacks associated with the need of a detailed analysis of the whole synthesis process (in order to exclude possible underestimated sources of fossil carbon), the determination of the 14C content expected for a fully biogenic material and the development of proper calculation procedures.

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194

SESSION 20

14C AND MODELLING

ConvenersF. marzaioli (ITA), R. muscheler (SWE), K. Rodgers (USA)

DescriptionRadiocarbon, the cosmogenic and anthropogenic (bomb carbon) radionuclide, is widespread in all the environmental compartments being naturally involved in the global carbon cycle. Due to its nature, 14C preserves the potential to serve as process tracer and/or chronometer. Since its discovery and the birth of the radiocarbon dating methodology, modelling approaches have been widely applied to disentangle the physical mechanisms governing its production and observed distributions. Over the last decades, with the advent of the earth and climate change sciences, radiocarbon became a preferential tool for the study of dynamical processes in climate and carbon cycle. For the carbon cycle, this includes interactions with the physical climate system, and this has been investigated using a variety of modelling tools and methods.This session aims to attract contributions applying modelling approaches to the study of processes characterizing the atmosphere, hydrosphere, biosphere and atmosphere and fluxes within and between these compartments. Contributions quantifying natural changes and the impact of anthropogenic actions on the contemporary and past climate system are also particularly welcome.

Keywords14C production modelling, direct/inverse modelling for global cycle, past and contemporary climate change

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195

S20-INV-01

TOWARDS A GCM-BASED REANALYSIS OF RADIOCARBON RECORDS AND RECONSTRUCTIONS

BUTZIN M.(1)(2), PRanGe M.(1), loHMann G.(2)

(1) University of bremen, bReMen, GeRManY;(2) alfred Wegener Institute for Polar and Marine Research, bReMeRHaVen, GeRManY

AbstractRadiocarbon is a powerful tracer to determine the state of the climate system as well as to investigate past environmental changes. However, 14C observations become increasingly scarce the further we look backward in time. General circulation models (GCMs) may help to interpret scattered 14C records by dynamically filling in spatio-temporal gaps. Here, we give two examples for such a GCM-based approach in which we apply an ocean GCM to study issues related to the last deglaciation.First we show results of equilibrium simulations indicating that during the Last Glacial Maximum, the overturning circulation of the ocean and the 14C partitioning between the various marine reservoirs were quite different from today.Then we will focus on transient simulations in which we assess the coevolution of marine 14C records and atmospheric 14C reconstructions between 21 and 14 cal ka BP. These simulations employ an iteration scheme in which atmospheric 14C reconstructions are reanalyzed and readjusted in a self-consistent way. An example considering data from the Caribbean Sea leads to enhanced variability of atmospheric Δ14C by +/- 30 ‰, and to an increase of the mysterious drop of atmospheric Δ14C between 17.5 and 14.5 cal ka BP by about 20 ‰. A by-product of this ‘reanalysis’ are crude estimates of cosmogenic 14C production fluxes which, for the given example, are in the lower range of reconstructions.

ReferencesButzin M., Prange M., and Lohmann G. (2012) Readjustment of glacial radiocarbon chronologies by self-consistent three-dimensional ocean circulation modeling. Earth and Planetary Science Letters, Vol. 317-318, pp. 177-184, doi:10.1016/j.epsl.2011.11.046.

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196

S20-O-02

ATMOSPHERIC MODELING AND DETECTION OF THE FOSSIL FUEL CO2 SIGNAL USING RADIOCARBON

MILLER J.(1), leHMan S.(2)

(1) noaa earth System Research laboratory, boUlDeR, UnITeD STaTeS;(2) University of colorado, boUlDeR, UnITeD STaTeS

AbstractWe have developed an atmospheric 14CO2 modeling framework that successfully reproduces most of our observed atmospheric 14CO2 spatial gradients in North America and other parts of the Northern Hemisphere; additionally, our model accurately simulates the secular decrease in atmospheric 14C seen at our background observation site at Niwot Ridge, Colorado, USA (NWR) between 2004 and 2010. The atmospheric model we use is TM5, run at 1 x 1 degree (lon x lat) resolution over North America and 3 x 2 resolution elsewhere. All atmospheric 14CO2,

13CO2, and total CO2 sources and sinks (fossil fuel emissions, two-way land and ocean C exchanges, biomass burning, nuclear emissions and atmospheric 14C production) are specified at monthly and 1 degree horizontal resolution. The resultant impact of these sources and sinks are tracked individually through the model atmosphere. Carrying each source or sink term as an individual tracer not only allows attribution of model (and observed) Δ14C signals, but also allows us to create linear combinations of tracers, ex post facto, that allow us to test the sensitivity of different specifications of, e.g., fossil fuel emissions, atmospheric production or air-sea gas exchange. Our preliminary sensitivity tests suggest that the most important sources and sinks in determining the Northern Hemisphere spatial gradients are fossil fuel emissions and the terrestrial fluxes. However, the global trend is also sensitive to atmospheric production (though not its spatial pattern) and ocean fluxes. Overall, our current analysis of the global atmospheric Δ14CO2 suggests that the present rate of decrease of about 5 per mil per year can not be simply described by a single dominant budget term. Rather, the magnitudes of the land and ocean flux terms and fossil fuel are all similar, but two of these are negative (fossil and ocean) and one positive (land).The primary goal of our model development is to assess the possibility of using a network of 14CO2 observations to constrain fossil fuel emissions at regional (i.e. ~106 km2) or smaller scales across continents, with monthly to annual time resolution. While economic statistic-based inventories provide relatively accurate (uncertainty estimated at ~ +/- 5%) emissions at annual and national scales, they are:

a) invariably out of date;

b) more uncertain at sub-national and sub-annual scales;

and c) need to be independently confirmed, especially in light of multi-national agreements and as large monetary values become associated with emissions.

We will present a synthetic model study (see Box 4.2 of committee on Methods for estimating Greenhouse Gas emissions, 2010), that shows how ~3 14CO2 observations per week at ~50 towers across the conterminous USA, could independently constrain fossil fuel CO2 emissions to ~10% over three-monthly periods across regions ~ 5 x 105 km2. We will discuss the requirements and uncertainties that need to be addressed in order to successfully translate atmospheric 14CO2 observations into fossil fuel emissions.

ReferencesCommittee on Methods for Estimating Greenhouse Gas Emissions (2010), Verifying Greenhouse Gas emissions: Methods to Support International climate agreements, 109 pp., The National Academies Press, Washington, DC.

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197

S20-O-03

MODEL STRUCTURE AND CALCULATION OF TURNOVER TIMES OF ORGANIC MATTER USING RADIOCARBON: THE SOILR PACKAGE

SIERRA C.A., MUelleR M., TRUMboRe S.

Max Planck Institute for biogeochemistry, Jena, GeRManY

AbstractRadiocarbon is a powerful tool for studying carbon dynamics in soil organic matter. Commonly, radiocarbon is used to estimate the turnover time of different soil organic matter fractions with the aid of mathematical models. However, the choice of model structure can significantly influence the calculation of turnover times. We developed a tool to represent different model structures and calculate turnover times of soil organic matter fractions. This tool, SoilR, was developed in the R environment for statistical computing. It allows the specification of any possible model structure of a compartment model and facilitates the integration of Bayesian algorithms for parameter estimation. We explored the effects of the choice of model structure on the calculation of turnover times using measurements taken at Harvard Forest, USA. Our results showed that model structures that include both stabilization and destabilization mechanisms of soil organic matter tend to produce longer turnover times than structures that only include stabilization processes or independent decay of different fractions. Our modeling tool should therefore help to reduce uncertainties in the estimation of turnover times of soil organic matter under different assumptions of stabilization processes in soils.

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PosterCommunications

Session A

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Monday July 9Tuesday July 10Session 2 - Advances in physical measurement techniques of Radiocarbon, and other long-lived radionuclides

Session 3 - Advances in radiocarbon pretreatment protocols

Session 4 - Specific compounds: Towards new applications

Session 13 - Radiocarbon as a tracer of sources, fluxes and time in continental water

Session 16 - Anthropogenic impacts

Session 17 - 14C tracer of life

Session 20 - 14C and Modeling

199

SESSION 2

ADVANCES IN PHYSICAL MEASUREMENT TECHNIqUES OF RADIOCARBON, AND OTHER

LONG-LIVED RADIONUCLIDES

ConvenersA. Hogg (NZL), J. Southon (USA), H.S. Synal (CHE)

DescriptionThis session aims to provide a comprehensive overview on the latest developments in measurement technology, particularly for Radiocarbon, but also including other long-lived radionuclides.The session also focuses on advances in sample preparation and handling procedures. Here we expect AMS contributions on ion sources (conventional sputter or hybrid systems), gas interfaces to ion sources, ultra small (micro gram size) sample preparation and measurement procedures. Radiometric contributions could include quench correction in liquid scintillation counting. Contributions on improvements in background blank assessment (applicable to all methods) will be welcome.In addition, we encourage contributions on alternative methods such as laser-based spectroscopy or conventional mass spectrometric systems.

KeywordsAMS, Ion source, micro gram samples, new detection technologies, liquid scintillation counting, gas proportional counting

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200

S02-P-001

MEASUREMENT OF 59NI WITH AMS AT CHINA INSTITUTE OF ATOMIC ENERGY(CIAE)

HE M.(1), RUan X.(2), DonG K.(1)

(1) china Institute of atomic energy, beIJInG, cHIna; (2) Guangxi University, nannInG, cHIna

AbstractThe long lived radioisotopes of Ni can be used in a number of applications including low-level radioactive waste management, cosmic radiation study, neutron dosimetry and astrophysics. 59Ni with a half life of 76ka is well suited to carry out these applications, in order to carry out the applications base on 59Ni, A method for AMS measurement of 59Ni has been established at CIAE with the HI - 13 Tandem accelerator and the newly developed ΔE - Q3D detection system.

The sample form of NiO was adopted for the AMS measurement of 59Ni at CIAE, Ni- was extracted from the source. After passing through the electrostatic analyzer and injection magnet, beams were selected for injection into the HI - 13 Beijing Tandem Accelerator which was set at 11.5 MV. A 90° double - focusing analyzing magnet was used to select 59Ni12+ with energy of 149.5 MeV. After the switching magnet, the 59Ni12+ and 59Co12+ were transported to the ΔE - Q3D detection system. A very homogeneous Si3N4 foil with thickness of 4.5 mm was place at the entrance of the Q3D magnet spectrometry as a absorber, after 59Ni and 59Co passing through the absorber, ions with the charge state of 19+ were selected and transported to the focal plane of the Q3D magnet spectrometry, due to the different energy loss of 59Ni and 59Co in the Si3N4 foil, the isobars are separated at the focal plane of the Q3D magnet spectrometer. The results shown that the peaks of 59Ni and 59Co were separated by about 130mm on the focal plane and each had a width 60mm(FWHM). A four-anodes gas ionization chamber was mount at the Q3D focal plane. By suitable adjusting the magnetic field of Q3D, more than 95% of 59Ni were detected with the gas detector while almost of the 59Co were eliminated. By this way, a suppression factor of about 103 was achieved. Then 59Co and 59Ni were identified with the gas ionization chamber. the 59Ni count can be extracted with appropriate gates on five signals from the detector, 59Co suppression factor of 2´104 was obtained with the detector. An overall suppression factor of higher than 107 for 59Co can be obtained by using the ΔE-Q3D detection system. The detection sensitivity of 59Ni/Ni=5.3´10-13 was obtained by using a commercial NiO sample.

*Corresponding author: (ph) +86 01 69358004, (fax) +86 01 69357787, [email protected] by National natural science foundation of China under grant number 11175266

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201

S02-P-002

THE 14C-AMS LABORATORY IN BRAZIL

MACARIO K., GoMeS P.R., anJoS R., caRValHo c.R., lInaReS R., alVeS e., olIVeIRa f., caRDoZo l.

Universidade federal fluminense, nITeRoI, bRaZIl

AbstractAfter around 20 years of collaborative projects with Brazilian researchers from Archaeology and Geosciences and with external AMS laboratories, the first 14C-AMS laboratory in Latin America was installed at the Physics Institute of the Fluminense Federal University. A 250 kV Single Stage Accelerator produced by National Electrostatics Corporation begins operation in 2012. At the radiocarbon sample preparation laboratory (L4C-UFF), separate areas are dedicated to chemical treatment and graphitization. A stainless steel based vacuum line using a turbo pump was constructed for carbon dioxide purification. Graphitization was initially performed in pre-treated quartz tubes in a muffle oven.

In the first tests with reference material prepared at L4C-UFF some samples had a poor graphitization yield, indicating an incomplete reaction probably due to a problem with the temperature in the muffle furnace. Moreover, most of the graphitized samples were solid chunks of graphite instead of a fluffy powder. Preliminary tests were run at Prime Lab, but because of the relatively small sample size, the currents in the accelerator were low, producing less reliable results due to isotopic fractionation. Modifications were made to the laboratory focusing on improving the yield and quality of the graphite. Graphitization is now being performed at lower temperatures in sealed Pyrex tubes, using Zinc and Titanium Hydrate.

In this work we report the first results of samples prepared at L4C-UFF and measured with our accelerator system. A set of samples among NBS 4990C standards, alfa aesar graphite and IAEA C6 were successfully combusted and graphitized. Reaction produced fluffy homogeneous graphite. Most samples produced stable and intense currents. Average uncertainty for 14/13 ratios was about 0.4% and background levels were around 40ky. Studies on isotopic fractionation and laboratory contamination are now under way in order to better understand and to improve quality of measurements.

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202

S02-P-003

THE ANSTO ISOTOPE CYCLING SYSTEM

WATT G.(1), boRonKaY S.(2), SMITH a.(1), HoTcHKIS M.(1)

(1) anSTo, lUcaS HeIGHTS, aUSTRalIa; (2) balaton Technologies, RoSe baY, aUSTRalIa

AbstractThe isotope cycling system on the ANTARES accelerator at ANSTO has undergone significant evolution since commissioning in 1993. At that time an in-house-designed programmable 15 bit digital pulse generator (‘sequencer’) was used to generate the timing & sequencing of the control signals for bouncing voltage selection, beam-chopping, Faraday Cup current, and rare isotope event measurements with time resolution at the µs level, accuracy ~ 5 ns, and overall cycle duration of up to 8 seconds, with provision for measuring up to 4 isotopes.While this has proven to be a highly reliable and versatile system over the intervening 19 years, the devices used are now obsolete, the interfacing to a host personal computer is no longer viable, and longer counting times and extra features are now desirable.

Recent work has resulted in replacement of the sequencer by a commercial National Instruments PCI–bus Xilinx Virtex 2 FPGA (Field Programmable Gate Array) card. The unit was programmed using the FPGA programming module of LabVIEW 2010, avoiding the need for specialised knowledge of VHDL and FPGA internal architecture. The first implementation of this unit is functionally identical to the previous system, but with vastly simplified interfacing, a much smaller footprint (it is located within the host PC, instead of in a separate housing), and with the ability to be quickly & inexpensively replaced off-the-shelf as necessary.

It is anticipated that future developments will provide for measurement of up to 8 isotopes, with counting durations between 1 µs and > 400 sec per isotope, while maintaining µs-level timing resolution and timing accuracy ~ 5 ns. These developments are easily implemented in the new sequencer system.

Programming of both versions of the sequencer is accomplished by software written in-house (‘Cycle.exe’) using Microsoft Visual Basic 6.0, which presents to the user a form with fields to accept values of duration, chopping duty cycle, and bouncing voltage for each isotope, and produces from this a text file whose contents define each of up to 15 output bit levels and time values where output transitions on them take place.In the original design these values were loaded into semiconductor SRAM memory via a Microsoft Quick Basic 4.5 DOS program (‘RAMload.exe’) and a 36 bit parallel interface. In the replacement design, LabVIEW writes these values directly into the FPGA memory via the PCI backplane interface.

Additional electronic systems, such as the high-voltage (‘bouncing’) amplifier, multiplexer, fast electrostatic beam chopper, gating modules, active current attenuators for precision current measurement and the high energy bouncers, are also described.

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203

S02-P-004

PRESENT STATUS OF YU-AMS SYSTEM

TOKANAI F.(1), KaTo K.(1), anSHITa M.(1), SaKURaI H.(1), ToYoGUcHI T.(2), KobaYaSHI T.(2), MIYaHaRa H.(3), oHYaMa M.(4), HoSHIno Y.(4)

(1) faculty of Science, Yamagata University, YaMaGaTa, JaPan; (2) Division of Pharmacy, Yamagata University Hospital, YaMaGaTa, JaPan; (3) Institute for cosmic Ray Research, The University of Tokyo, KaSHIWa, JaPan; (4) The center for academic Resources and archives botanical Gardens, Tohoku University, SenDaI, JaPan

AbstractAccelerator mass spectrometry (AMS) is a method of measuring extremely low ratios of isotopes in a very small sample of less than 1 mg. In particular, AMS measurements for 14C, which has a half-life of 5700 ± 30 years, have been widely utilized for radiocarbon dating in various fields such as archaeology, environmental science, geology, and space and earth sciences. In 2009, Yamagata University (YU) installed an AMS (YU-AMS) system [1], this is a Pelletron accelerator (1.5SDH-1) developed by National Electrostatics Corp. An automated acid–alkali–acid (AAA) treatment system and automated graphitization line were also installed at the same facility for sample preparation. This AMS system is the first AMS system installed in a university in the Tohoku-Hokkaido region of Japan. The facility also provides radiocarbon dating for samples from other universities, institutes, and public organizations.

Performance tests of the YU-AMS system were carried out by measuring the C series standard samples (C1 – C9) and HOxII provided by IAEA and NIST, respectively. The precision of 14C measurements for the standard samples is typically higher than 0.2%. Long-term stability more of than one year was demonstrated by carrying out the periodic measurement of standard samples C6 and C7 of IAEA. We evaluated the YU-AMS system by comparing the 14C ages of Japanese tree rings having dendrochronologically determined calendar ages with calibration data.

In the medical and pharmaceutical fields, microdosing studies using AMS measurements of 14C have been attracting considerable attention for drug development. The microdosing study is used to predict the pharmacokinetics of new drugs by labeling them with 14C and then administering them to human volunteers [2]. However, there are few AMS facilities in Japan for conducting measurements of the samples obtained from microdosing studies. To satisfy the requirement of 14C AMS for microdosing and medical studies as well as those of radiocarbon dating, we also carried out some performance tests using control serum, normal human serum, and a 14C-labeled drug (Oxaliplatin). In this paper, we describe the status and approach of the YU-AMS facility.

References[1] F. Tokanai et al., AIP Conference Proceedings, 1336, 70-74 (2011).[2] Ministry of Health, Labour and Welfare Guidance. Tokyo, Japan: Microdose clinical studies, Ministry of Health, Labour and Welfare, Pharmaceutical and Medical Safety Bureau, 2008.

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204

S02-P-005

THE NEW 250 KV SINGLE STAGE AMS SYSTEM AT CAIS: PERFORMANCE AND COMPARISON WITH A 500 KV COMPACT TANDEM MACHINE

PRASAD G., noaKeS J.e., cHeRKInSKY a., cUlP R., DVoRaceK D.


AbstractThe University of Georgia’s Center for Applied Isotope Studies has recently purchased a new compact 250 kV single stage AMS (SSAMS) unit from National Electrostatics Corporation. This unit is mainly intended for 14C measurements of natural and bio-based products. This unit augments the existing 500 kV tandem accelerator, which was one of the very early compact AMS (CAMS) machines built by NEC. The CAMS unit has been the workhorse of the AMS programme at CAIS for over ten years. Installation of new SSAMS system was completed in December 2011. The new AMS system is equipped with a 134 cathode MC-SNICS ion source, similar to that of the older tandem machine. Early tests indicate that the terminal voltage stability of SSAMS is superior to that of the tandem CAMS unit which uses the Pelletron charging system. Better terminal stability makes the SSAMS unit more suitable for stable isotope ratio measurements when compared with high energy AMS accelerators. We will be presenting the results of the performance tests carried out on SSAMS. These include the results of measurements of Oxalic acid 14C standards as well as other secondary standards. We will also present the stable isotope ratio measurements for comparison with the conventional stable isotope spectrometers. Finally, we will also compare the precision and background levels of SSAMS against that of the 500 kV CAMS unit.

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205

S02-P-006

HIGH PRECISION 14C ROUTINE COUNTING AND DELAYED RECOUNTING OF LSC SAMPLES

THEODORSSON P.

Science Institute, ReYKJaVIK, IcelanD

AbstractWhen 14C dating samples are counted with a stable liquid scintillation counting (LSC) system the precision only depends on the length of counting time. In archaeological investigations, where the collection effort behind each sample is generally high, highest economically acceptable precision is frequently needed. When the results have been analyzed, the need may arise to re-measure possible outliers or to increase the accuracy of some measurements. An important advantage of the LSC method, but apparently rarely used, is that it is non-destructive, the samples can be stored and recounted, even a year after the initial measurement. Inevitable evaporation loss of benzene from the vial and drift of system parameters over several months-long storage, may affect the accuracy. The low production cost of the compact single photomultiplier tube ICELS system used here, developed specifically for radiocarbon dating, allows a counting time of 1-3 weeks in routine dating. The result of the initial counting and delayed re-counting precision study, using an enhanced activity 14C benzene standard, is presented.

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206

S02-P-007

A NEW RADIOCARBON AMS LABORATORY AT THE UNIVERSITY OF BERN

SZIDAT S.(1)(2), SalaZaR G.(1)(2), ZHanG Y.(1)(2)(3), VoGel e.(1)(2), baTTaGlIa M.(1)(2), WacKeR l.(4), SYnal H.a.(4), TUeRleR a.(1)(2)(3)

(1) Department of chemistry and biochemistry, University of bern, beRn, SWITZeRlanD; (2) oeschger centre for climate change Research, University of bern, beRn, SWITZeRlanD; (3) laboratory of Radiochemistry and environmental chemistry, Paul Scherrer Institut, VIllIGen-PSI, SWITZeRlanD; (4) laboratory of Ion beam Physics, eTH Hoenggerberg, ZURIcH, SWITZeRlanD

AbstractThe University of Bern has a long history of experience in precise 14C measurements based on the conventional counting laboratory founded more than 50 years ago [1]. Due to the demanding preparation and measurement procedures, the throughput and required carbon mass of this technique both are the limiting factors. Therefore, the University of Bern decided to update the facility aiming at a new 14C laboratory equipped with an accelerator mass spectrometer (AMS) MICADAS [2]. The focus of this laboratory is twofold. On the one hand, the access to routine 14C analysis for climate research and other disciplines will be improved on site. On the other hand, new hyphenated analytical systems shall be developed for online separation and 14C detection of specific fractions or individual compounds [e.g., 3]. In this work, instruments, laboratory equipment, measures of quality assurance and first results of the new laboratory will be presented.

References[1] F.G. Houtermans and H. Oeschger, Helv. Phys. Acta, 31, 117-126 (1958).[2] H.-A. Synal et al., Nucl. Instrum. Meth. Phys. Res. B, 259, 7-13 (2007).[3] N. Perron et al., Radiocarbon, 52, 761-768 (2010).

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207

S02-P-008

RADIOCARBON MEASUREMENTS WITH LSC SYSTEM HIDEX 300SL AND ICELS OF WOOD SAMPLES DATED DENDROCHRONOLOGICALLY – COMPARISON OF RESULTS

KRAPIEC M.(1), THeoDoRSSon P.(2), WalanUS a.(1)

(1) aGH University of Science and Technology, KRaKoW, PolanD; (2) Science Institute, University of Iceland, ReYKJaVIK, IcelanD;

AbstractIn the Laboratory of Absolute Dating in Skała a tree ring chronology for Polish oak is being constructed. The approximate age of the oak samples used is first determined by the LSC technique. In the first phase of this work the Hidex 300 SL spectrometer was used but later a second LSC system was added, ICELS. Furthermore, some of the samples were measured to higher precision in ICELS systems at the University of Iceland. Both LSC systems are newcomers in the filed of radiocarbon dating. Hidex uses 3 photomultiplier tubes (PMT) and ICESL a single PMT.

15 three ml benzene samples were measured, prepared from approximately a dozen annual tree-rings wood samples of subfossil oaks (Quercus sp.) from alluvial sediments of the Vistula river in the vicinity of Krakow (S Poland). The samples were also dated dendrocornologically using the 3000 years long oak standard chronology for S Poland (aut. M. Krapiec). The results of the comparison will be presented.

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208

S02-P-009

DESIGN OF A COMMERCIAL ISA FOR AMS APPLICATIONS

ALARY J.F.(1), GHolaMReZa J.(2), coUSInS l.M.(2), Hao c.(1), ZHao X.l.(3), KIeSeR W.e.(3), lITHeRlanD a.e.(4)

(1) Isobarex corp., bolTon, canaDa; (2) Ionics Mass Spectrometry Group, bolTon, canaDa; (3) University of ottawa, oTTaWa, canaDa; (4) University of Toronto, ToRonTo, canaDa

AbstractA radiofrequency quadrupole (RFQ) cell filled with a thin reaction or collision gas provides an effective way to selectively remove isobars from the isotopes 36Cl, 41Ca, 90Sr and 135,137Cs, bringing these important radiotracers well within the application range of small AMS systems. When the RFQ cell is coupled with deceleration and acceleration stages, it becomes the central element of the Isobar Separator for Anions (ISA), a device having the demonstrated capability of performing on-line suppression of isobars in standard AMS injection lines. However, applying this technique to AMS measurements critically depends on its capacity to transmit the wanted anions at a high stable efficiency. Based on recent SIMION-8.1 studies and our most recent results on the attenuation of KF3-[1] and other anions, we have developed a commercially viable design for the ISA in which anion transmission through the RFQ cell and deceleration and reacceleration stages has been optimized to levels compatible with routine AMS analysis. Entrance optics have also been designed having in mind the easy integration of the ISA into new or existing AMS systems, and important features such as multi-staged split flow turbo molecule pumps have been implemented. Segmented RFQ rods are also used in the gas cell to fully control reaction time (chemical and kinetic reactions), fragmentation pathways and more effective ion beam transmission through the cell. The mechanical layout will be presented in 3D models using Solid Works; the beam optical properties will be shown by SIMION-8.1 simulations using a hard-sphere collision model to simulate the gas-anion dynamics in the gas cell. Results of confirmatory tests obtained on an improved version of the experimental ISA setup at IsoTrace will also be reported.

References[1] X.-L. Zhao et al., A Refined Study of KF3-Attenuation in RFQ Gas-Cell for 41Ca AMS, in this conference

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209

S02-P-010

C DATING WITH ICELS A LIqUID SCINTILLATION COUNTING SYSTEM USING FIXED ENERGY BALANCE COUNTING WINDOW METHOD

TUDYKA K., PaZDUR a.

Institute of Physics, Silesian University of Technology, GlIWIce, PolanD

AbstractIn this work we present an application of a fixed energy balance counting window in 14C dating of geological peat samples with archaeological significance. We determine the fixed energy balance counting window for a low cost LSC ICELS system. We show long term activity modern biosphere standard records which show good stability. The background stability is sufficient for dating samples up to approximately 30000 14C yr old.

We compare the results of radiocarbon dating to the ones obtained earlier using Quantulus 1220™. The results obtained with two ICELS system and Quantulus 1220™ are in agreement. Four age-depth models for archaeological site with metallurgy industry evidence from Upper Silesia region (Poland) were made using: two ICELS systems, one Quantulus 1220™ and weighted mean from all LSC spectrometers. The age-depth models are very similar, although there are differences caused mostly by the fact that not every sample was dated using all three LSC systems.

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210

S02-P-011

AMS MEASUREMENT OF 53MN AND ITS APPLICATION AT CIAE

DONG K.(1), He M.(1), lIU G.(2), JIanG S.(1)

(1) china Institute of atomic energy, beIJInG, cHIna; (2) college of oceanography and environmental Science, Xiamen University, XIaMen, cHIna

AbstractThe determination of cosmogenic 53Mn in terrestrial formations has many interesting applications in many scientific areas. However, the potential of 53Mn dating has not been fully tapped for many years, due to the lack of appropriate method for the determination of ultra-trace 53Mn. Recently, the AMS system of China Institute of Atomic Energy (CIAE), with the ΔE-Q3D detection system, has been set up for the measurements of 53Mn. A sensitivity of 10-15 has been achieved based on the sample material of MnF2 and the extraction ions of MnF-. Based on this, the measurement of depth profiles in deep sea ferromanganese crusts for dating with 53Mn is being carried out. The experimental setup, performances and newest results will be detailed in this presentation.

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211

S02-P-012

A NEW AMS/IBA LABORATORY AT THE COMENIUS UNIVERSITY OF BRATISLAVA

POVINEC P.(1), MaSaRIK J.(1), HolY K.(1), KUS P.(1), MacH l.(2), KoYS M.(2), boloGna M.(3), ZlaTnanSKY J.(3), SIVo a.(1), JeSKoVSKY M.(1), STanIceK J.(1), bReIeR R.(1), RIcHaRIKoVa M.(1), KaIZeR J.(1)

(1) comenius University, bRaTISlaVa, SloVaKIa; (2) KVanT, ltd., bRaTISlaVa, SloVaKIa; (3) Slovenske elektrarne, bRaTISlaVa, SloVaKIa

AbstractAs a part of the Centre of Excellence of Physics of Complex Systems, supported by the European Structural Funds, a Centre of Nuclear and Isotopic Technologies (CENT) is under construction at the Faculty of Mathematics, Physics and Informatics of the Comenius University. The basic instrumentation of the Centre is based on the 3 MV Pelletron accelerator (NEC, USA). The laboratory has been design to meet both Accelerator Mass Spectrometry (AMS) as well as Ion Beam Analysis (IBA) requirements for nuclear, atomic, environmental and nanotechnology research. It is expected that the first part of the laboratory will be operational during the year 2013.

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212

S02-P-013

CHARGE EXCHANGE CROSS SECTION FOR CARBON IONS IN HELIUM

SEILER M., WacKeR l., SUTeR M., SYnal H.a.

eTH Zürich, ZÜRIcH, SWITZeRlanD

AbstractGas strippers are widely used at AMS instruments for molecular dissociation and charge changing in TANDEM systems. A critical point is the reduction of losses due to angular straggling to provide stable measurement conditions. The low mass of Helium particles results in lower straggling angles compared to traditional stripper gases like nitrogen. This advantage of Helium allows even smaller measurement systems than the currently active ones for radiocarbon like the SSAMS and MICADAS. For AMS it’s also important to have high charge state yields in order to reduce the total measurement time. While developing a single stage AMS instrument at ETH the charge state yields of helium were measured. From the measurements at very low stripper gas pressure the charge changing process can be measured and quantified by reaction cross sections. The results will be shown in comparison to literature values from different energies. Difficulties and problems of the measurements will be discussed and analyzed with regard to the construction of an AMS system.

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213

S02-P-014

SIMPLE CARBON DIOXIDE TRANSPORT OF CARBONATE SAMPLES TO A GAS ION SOURCE

SEILER M., MÜnSTeReR c., WacKeR l., SYnal H.a.

eTH Zürich, ZÜRIcH, SWITZeRlanD

AbstractAt ETH radiocarbon samples containing less than 100 μg of carbon are measured directly at the gas ion source. The interface allows the introduction of CO2 from various sources. A suitable sampling technique for carbonates is to capture CO2 that is released after the reaction with phosphoric acid. A critical point is the transport of the gas from the sample vial to the measurement system. This process is sensitive to contamination and can cause memory effects. Therefore the transport has to be done carefully, but it’s crucial to get high transport efficiencies for small samples as the sample size is limiting the achievable precision of the measurement. Helium is often used to enhance the transport of CO2 but if large amounts are added the efficiency of the ion source is reduced. Therefore, in cases where too much helium is needed to flush the sample out of the vial, a trap is used to concentrate the CO2 while the excess helium can be blown out. In this study different trap types are evaluated, as well as a method without any trap where the gas is transported by expansion and a very limited helium flow. Transport efficiency, cross contamination and complexity of the installation are compared for the different methods.

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214

S02-P-015

PROSPECTS OF DIRECT 14C ANALYSES WITH AMS ON VOLATILE ORGANIC COMPOUNDS

WACKER L., SeIleR M.


AbstractAccelerator mass spectrometry allows precise radiocarbon measurements on small samples. A major drawback is the time-consuming conversion of the sample material to graphite that can be measured in a negative ion Cs sputter source. An alternative is the direct analyses of CO2 from combusted samples with a gas ion source [1]. However, the introduction of CO2 into a sputter gas ion source is not necessarily the best option when a high yield of C- is desired.

Our proof-of-principle experiment shows, that various volatile substances can directly be introduced into a Cs sputter gas ion source, even without combustion to CO2. Moreover, the C- ion yields for organic compounds are often higher than for CO2. However, the molecular currents of CH- can also be up to two orders of magnitude higher, when organic molecules are injected. The increased molecular current can cause some additional background from molecular fragments (eg. 13C+) and a reliable detection of 14C can be difficult. While we will present the prospects of direct radiocarbon analyses on different organic compounds in general, we will mainly focus on the advantages and disadvantage of the direct analyses of alcohol as an example.

References[1] M. Ruff, S. Szidat, H.W. Gäggeler, M. Suter, H.A. Synal, L. Wacker, Gaseous radiocarbon measurements of small samples, Nucl Instrum Meth B, 268 (2010) 790-794.

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215

S02-P-016

AMS MEASUREMENT OF 237NP AT CIAE

WANG X.G.(1)(2), JIanG S.(1), He M.(1), DonG K.(1)

(1) china Institute of atomic energy, beIJInG, cHIna; (2) college of Physics Science and Technology, nannInG, cHIna

Abstract237Np have a very half-life of 2.14(1) ×106 a, is a by-product of nuclear reactors and plutonium production and it can be used as a component in neutron detection equipment. Neptunium is also found in trace amounts in uranium ores due to transmutation reactions. The isotopic ratio of 237Np/238U in nature is lower than 10-12, depending strongly on the integral neutron flux received by the material.237Np causes much concern as an “alternative nuclear material”, and potentially applicable in the studies on nuclear safeguards and radwaste migration.

The measurement of naturally occurring 237Np is difficult or even impossible without AMS (Accelerator Mass Spectrometry). By extracting negative molecular ions NpO-from the oxide sample, using 208Pb16O2-molecular ions for the simulation of 237Np ion transport, identifying the interference isotopes by high resolution magnet analyzer, electrostatic analyzer, and TOF detector, a method for AMS measurement of 237Np on the HI-13 Accelerator at China Institute of Atomic Energy (CIAE) is set up.The energy difference between the background ions and the interested ions 237Np is very small, 235U ~ 0.8%, 236U ~ 0.4% and 238U ~ 0.4%, only the time of flight (TOF) detector has sufficient resolution to distinguish the neighboring isotopes which happen to pass the ion optical filters. In order to heighten the detection efficiency and sensitivity, the TOF time resolution was improved to ~ 500ps. The 237Np standard was produced via fast neutron induced 238U(n,2n)237U reaction [1]. Based on these efforts,the sensitivity is below~10-11for 237Np/238U in present work. Based on these efforts, the sensitivity is below~10-11for 237Np/238U in present work.

References[1] Xianggao Wang, Shan Jiang, Kejun Dong, et al., Nucl. Instr. and Meth., 2010, B,2 68:1949

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216

S02-P-018

A NEWLY DESIGNED EqUIPMENT FOR THE CO2 DIRECT ABSORPTION METHOD AND LOW LEVEL 14C LIqUID SCINTILLATION COUNTING

CANDUCCI C.(1)(2), baRToloMeI P.(3), MaGnanI G.(3), RIZZo a.(3), PIccolI a.(4), ToSITTI l.(2), eSPoSITo M.(1)

(1) U-Series srl, boloGna, ITalY; (2) Dipartimento di chimica G.ciamician, boloGna, ITalY; (3) enea, boloGna, ITalY; (4) nano4bio srl, boloGna, ITalY

AbstractThe discrimination of fossil and biogenic carbon in emissions, fuels or biobased products is gaining importance in the field of environmental and climate change. In this framework there will be a strong need to uniform the process through standardization, labeling and certification.

The present study shows the design, the realization and the preliminary testing of a new system for the CO2 absorption method and the definition of a new protocol for radiocarbon analysis in gaseous emissions, fuels and “biobased products”. The most innovative aspect of this system is the material used for the realization of the vial with the aim of improving the sensitivity of the method.

According to ASTM D6866 standard, carbon dioxide is chemically trapped as a carbamate in a suitable absorbing solution (3-methoxy-propyl-amine), gravimetrically measured and analyzed by Liquid Scintillation Counting (Quantulus 1220) to determine the content of 14C.The described system is composed of a flask and inlet for CO2 storage, several cryogenic traps with different volume capacity, inlet for vacuum pump, pressure transducer and vacuum gauges and the vial containing the absorbing solution. The vial, made in polytetrafluoroethylene (PTFE), has been designed with an internal thread so that it could be directly screwed to the end junction of the line.

The procedure for radiocarbon analysis requires first the collection of gaseous samples or of carbon dioxide originated from acid hydrolysis of carbonates or oxidative combustion of organic samples into a collection system previously evacuated. A sufficient amount of CO2 to stoichiometrically react with the adsorbing solution is then transferred and frozen in the cryogenics traps at liquid nitrogen temperature and finally it is allowed to sublimate and react with the amine previously poured in the vial under inert atmosphere.The system has been designed to operate in static conditions even with small amounts of gaseous samples and without the use of recirculation pumps or plastic bags or bladders normally used to ensure the complete saturation of the CO2 absorbent. This process speeds up the laboratory operations and enables to monitor the progress of the reaction in real time.

A further advantage of this system is the possibility to perform the reaction directly into the same vial used for the 14C measurement. This fact minimizes the risk of loss of sample during transfers as well as the risk of contamination by atmospheric CO2 that could interfere, thus invalidating the final results. The PTFE vial shows background counts, referred to 10 mL absorbent and 10 mL Permafluor E+, considerably lower than low-40K-glass vials usually used in these applications: 1.6(0.2) CPM in spite of 3.5(0.2) CPM. The choice of this material is supposed to reduce the low limit of detection and then to spread the possible fields of application.

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217

S02-P-019

INTRA CAVITY OPTOGALVANIC SPECTROSCOPY: A NEW WAY OF 14C MEASUREMENT

MURNICK D.E.(1), bacHa T.(1), IlKMen e.(1), DeGUZMan M.(1),, caRSon c.(2), STÜTe M.(2), PaUl D.(3), MeIJeR H.a.J.(3)

(1) Department of Physics, Rutgers University, neWaRK nJ, UnITeD STaTeS; (2) earth and environmental engineering, columbia University, neW YoRK cITY, UnITeD STaTeS; (3) centre for Isotope Research, University of Groningen, GRonInGen, neTHeRlanDS

AbstractA few years ago, we demonstrated the successful application of opto-galvanic spectroscopy for natural 14C detection (Murnick et al.,2008). The method combines the well-established technique for CO2-lasers, the high spectral selectivity of such a laser filled with 14CO2, and the subtle way in which impedance changes due to resonant radiation in a gas discharge can be detected. By placing the sample gas discharge cell intra-cavity, both the laser intensity and the effective path length are greatly enhanced, and the necessary sensitivity for 14CO2 detection could be proven. Potential rewards of this Intra Cavity Opto-Galvanic Spectroscopy (ICOGS) technique are high: the instrumentation is desktop size, much lower in cost than an AMS instrument, and it can operate in a fast, continuous flow mode, analyzing either pure CO2, or CO2 in a suitable buffer gas, typically N2.

At present, our three groups are collaborating to further develop this technique towards an established alternative way of measuring 14C. We aim at three different directions of application: the Rutgers group is concentrating on 14C-labelled samples for biological and pharmaceutical research requiring high dynamic range and modest precision. The Columbia group is interested tracking the inventory and detecting the migration of sequestered CO2 moderately labelled (typically 5 times modern) with 14CO2, requiring a limited dynamic range with good precision. The Groningen group is trying to develop the method into an alternative for dating, thus concentrating on the full 0-1 modern range with as high precision as possible.

The specific aims of our three groups allow differences in sample treatment: pulses of small CO2 samples (~ 100 µg C) in a continuous stream of N2 gas for the labeled samples or continuous flow of pure CO2 or CO2 diluted in N2 (for larger sample sizes but higher precision), for example. The basic instrumentation of ICOGS, however, is shared between the groups and is being further developed in concert.We will report on the present state-of-the-art, with examples of measurements, and figures of merit for our three systems.

ReferencesDaniel E. Murnick, Ozgur Dogru, and Erhan Ilkmen, 2008.Intracavity Optogalvanic Spectroscopy. An Analytical Technique for 14C Analysis with Subattomole Sensitivityanal. chem.80, 4820–4824

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218

S02-P-020

A SYSTEM FOR THE SIMULTANEOUS ON LINE MEASUREMENT OF δ13C AND δ15N BY IRMS AND 14C BY AMS

QUARTA G., bRaIone e., calcaGnIle l., MaRUccIo l., D’elIa M., Gaballo V.,


AbstractIn the frame of the ongoing ITH@CHA research project the analytical capabilities of CEDAD are being enhanced by the design and integration on the existing AMS system of a new ion source able to accept gaseous samples and of an IRMS (Isotopic Ratio Mass Spectrometry) system for the on-line determination of the stable carbon and nitrogen isotopic ratios. The new set-up is formed by an elemental analyzer (EA), by which the samples are combusted to CO2 by flash combustion, a chromatographic unit for the separation of the combustion gases and a gas splitting unit. The gas splitting unit separates the combustion gas into two aliquots, one of them is sent to a IRMS system for the measurement of both the δ13C and δ15N fractionation terms and the second to a gas ion source connected to the existing injector of the AMS system. Aim of the project is to have the determination of the radiocarbon age on the same samples for which the δ13C and δ15N is measured by IRMS, in one combustion step. The technical details of the new set-up are presented in terms of instrumental features, inlet apparatus and required modification of the existing ion injector to allow the installation of the new ion source.

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219

S02-P-021

RESEARCH AND DEVELOPMENT AROUND THE ARTEMIS 14C AMS FACILITY

MOREAU C., baVaY D., caffY I., coMbY c., DelQUe-KolIc e., DUMoUlIn J.P., DURanD n., HaIn S., QUIleS a., SeTTI V., SoUPRaYen c., VIncenT J.

lMc14, SaclaY, fRance

AbstractThe AMS facility, ARTEMIS, is dedicated to high precision 14C measurements. It routinely measures over 4500 samples a year for French laboratories. This paper is a status report, showing the measurements of standard, blank, and inter-comparison samples, FIRI.

Since 2008, research and development programmes were established by the ARTEMIS team. During the collaborations with other research laboratories, inter-comparisons on archaeological samples were performed and listed here to show the quality of the ARTEMIS measurements. Three ways of specific research and development are investigated: technical development, beam optic simulations and specific archaeological researches. The technical developments around the facility are based on the setup of a new bench for water sample preparation and the routine micro-sample preparation and measurement. Beam optic simulations are carried out to control the quality of the measurement related to the tuning of the facility. Researches inside international collaborations are constantly in progress. Specific programmes are running in 2012, like improving the accuracy of reigns for dynastic Egypt period and the radiocarbon dating of ancient iron.

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220

S02-P-022

ENVIRONMICADAS: A MINI C-14 AMS WITH ENHANCED GAS ION SOURCE INTERFACE IN HERTELENDI LABORATORY OF ENVIRONMENTAL STUDIES, DEBRECEN, HUNGARY

MOLNÁR M.(1), RInYU l.(1), VeReS M.(2), SeIleR M.(3), WacKeR l.(3), SYnal H.a.(3)

(1) MTa aToMKI, DebRecen, HUnGaRY; (2) Isotoptech ZRt, DebRecen, HUnGaRY; (3) eTHZ, ZÜRIcH, SWITZeRlanD

AbstractBecause of the rapidly widening scale of scientific applications of C-14, a more developed and modern measuring technology was needed in Hungary. It’s based on isotope separation by accelerator mass spectrometry (AMS) instead of the gas proportional counting. A research collaboration between Swiss Federal Institute of Technology in Zürich (ETHZ), Institute of Nuclear Research of the Hungarian Academy of Sciences (ATOMKI) and Isotoptech ZRt was started in the autumn of 2009 aimed to develop an optimized AMS machine for environmental radiocarbon dating studies. This new system (EnvironMICADAS) requires 100-1000 times less sample quantity and gives more than ten times higher sample throughput than the older GPC technique in ATOMKI. In the summer of 2011 it was installed in Debrecen. A fully equipped sample preparation laboratory was also built meanwhile including two different graphitization lines (hydrogen and zinc reduction) and capable of handling organic, inorganic and water samples.

As a special feature to make the AMS system more open for environmental research on ultra small sized (5-50 μg C) samples with lower precision requirements, an enhanced gas ion source interface was also developed by ETHZ and installed in the Laboratory of Environmental Studies, Debrecen.

This paper presents the successful factory and final acceptance test results and the performance of the EnvironMICADAS with the gas interface including overall precision, reproducibility, long term stability and background. Details of facility preparation, installation and operation experience will be also discussed.

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221

S02-P-023

DATA ANALYSIS AND qUALITY CONTROL AT THE JENA AMS SYSTEM

STEINHOF A

Max-Planck Institut für biogeochemie, Jena, GeRManY

AbstractFrom lab to lab the data analysis including the determination of the uncertainties of 14C data differs. Therefore the emphasis of the present contribution is to present also the basic equations and the check procedures of the Jena data analysis. Furthermore the long-term quality control management and the additional uncertainty for the transmission and the current measurement will be presented.

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222

S02-P-024

20-YEARS LONG OF 14C MEASUREMENTS AT THE INSTITUT DES RADIOISOTOPES (NIAMEY, NIGER): A REVIEW

SOULEY I., MaYaKI S., MInDaoUDoU Z., SalIfoU S., ben MoHaMeD a.

Institut des RadioIsotopes, Université abdou Moumouni, nIaMeY, nIGeR

AbstractThe C14 laboratory of the Institut des RadioIsotopes (IRI) was initially set up for the development of hydrological studies in three West African Countries: Burkina, Niger and Senegal (project NER /8/005-AIEI).

Actually, during 20 years, around 400 analyzes have been done for investigations in different fields as hydrology, paleoclimatology, paleoenvironment and archeology. Thanks to those accurate results, this laboratory became a reference laboratory in sub-Saharan Africa.

I will present a review of those 20-years results, pointing out our accurate methods (treatment of samples) leading to accuracies comparable to international references. I will also remind the interest of radiocarbon measurements against other methods.

I will also mention the difficulties that we have met from several years preventing us from keeping collaborating with for example IAEA and the international inter comparison.

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223

S02-P-025

ULTRA-SMALL GRAPHITE CAPABILITIES AT NOSAMS: PROGRESS AND INITIAL RESULTS

GAGNON A., McnIcHol a., XU l., SHaH S., RobeRTS M.

Woods Hole oceanographic Inst., WooDS Hole, UnITeD STaTeS

AbstractMeasuring the radiocarbon content of samples containing <100 µg C has greatly expanded its use in geochemical studies. The field of compound specific radiocarbon analysis (CSRA), critical to helping unravel the complex history recorded in marine sediments, would not be possible without this ability. Analyzing ever smaller carbonate samples is providing insights into the mechanics of carbonate dissolution within sediments, allowing one to better understand the age of the sediment bioturbated layer. At NOSAMS, we are working to reduce the size of the sample we can analyze to approach the capability of the accelerator.

Ultra-small graphite is defined at the National Ocean Sciences Accelerator Mass Spectrometry (NOSAMS) facility as any graphite produced containing less than 30ug of carbon. New, small-volume (approx. 1 ml) graphite reactors have been fabricated, and testing/monitoring of the reactions using CO2 from primary (NBS Oxalic Acid-I) standards and blanks (IAEA C-1) has been ongoing. Preliminary work demonstrates the ability of the accelerator to measure samples containing as little as 4-5 µg C.

An investigation of laboratory process blank contributions is necessary in order to firmly understand the radiocarbon measurements obtained from these very small samples. Efforts are presently being undertaken to minimize the blank associated with closed-tube combustion of organic matter. This will ultimately benefit samples isolated by preparative capillary gas chromatography (PCGC). Modifications to a commercial elemental analyzer (EA) are being explored for the analysis of discrete macrofossils and HPLC extracts. We are also exploring the limits set by our carbonate analyses in order to expand the useful range of paleoceanographic applications. A compact, low volume stainless steel vacuum system is being constructed in attempt to minimize the graphite reaction blank on such micro-scale samples. A high precision capacitance manometer will be used to accurately quantify the CO2 added to each reactor, and each reaction will be monitored using Labview software.

Here we will present the results generated and limitations encountered from the existing and newer systems, specifically as it applies to process blank contributions.

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224

SESSION 3

ADVANCES IN RADIOCARBON PRETREATMENT PROTOCOLS

ConvenersP. Ascough (GBR), K. Douka (GBR), A. Zazzo (FRA)

DescriptionPretreatment chemistry is one of the most important parameters in the application of radiocarbon dating and like other factors that affect dating accuracy it is continuously upgraded. Over the last decade, a suite of methodological advances has improved the characterization (using FTIR, SEM and XRD prior to 14C dating) and removal of chemical and physical contaminants from all sample materials (e.g. bone, charcoal and carbonates). Specialized pretreatment techniques, including preparation of very small sized samples, add another dimension in the ever-evolving preparation of samples prior to AMS measurement. In this session we will be focusing on novel developments in the field of radiocarbon pretreatment chemistry, and their application on archaeological, environmental and other samples.

KeywordsPretreatment methodology, sample characterization, physical/chemical contaminant removal, improved sample isolation

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225

S03-P-027

SECOND GENERATION LASER HEATED MICROFURNACE FOR GRAPHITISATION OF MICROGRAM SAMPLES

YANG B., SMITH a., Mann M.

anSTo, lUcaS HeIGHT, aUSTRalIa

AbstractWe present recent developments in design, construction and testing of a second generation laser heated microfurnace (mark-II MF). Based on our systematic studies aimed at optimising the performance of the first laser heated microfurnace (mark-I MF, references 1-3), we have designed the mark-II MF to have the following features: 1) it has a small volume of 0.35 cc allowing us to graphitise carbon dioxide samples containing just a few micrograms of C with reasonable reaction efficiency, 2) it can operate over a large pressure range (0 to 2 bar) and has the capacity to graphitise CO2 samples containing up to 100 µg of C; 3) it is compact, with three valves integrated into the microfurnace body, 4) these valves can be controlled electronically, enabling automation of the process through the LABview interface, 5) it is compatible with the new version of small-sample conventional graphitisation furnace and shares a common vacuum system. We use a ‘budget’ fibre packaged array for the diode laser with custom built focusing optics. The use of a new IR thermometer with a short focal length has allowed us to decrease the height of the unit. As with the mark-I MF, feedback control of the catalyst temperature and logging of the reaction parameters is handled by a LABview interface.

Our early experience and preliminary results with the mark –II MF are presented and discussed.

References1. A cold finger cooling system for the efficient graphitisation of microgram-sized carbon samples, Bin Yang,

A.M. Smith and Quan Hua, manuscript submitted for the 12th International Conference on Accelerator Mass Spectrometry, Wellington, New Zealand, 20th – 25th March 2011.

2. Laser-heated microfurnace – gas analysis & graphite morphology, A.M. Smith, Bin Yang, Quan Hua & Michael Mann, Radiocarbon 52(2–3), 2010, pp. 769–782.

3. New developments in micro-sample 14C AMS at ANSTO, A.M. Smith, Q. Hua and V.A. Levchenko, INQUA 2007 Abstracts, Quaternary International 167-168 (2007), pp. 390.

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226

S03-P-028

DEVELOPMENTS IN GAS EXTRACTION FOR 14C MEASUREMENT AT ANSTO

SMITH A.

anSTo, lUcaS HeIGHTS, aUSTRalIa

AbstractWe report on refinements to the apparatus used at ANSTO to cryogenically separate CO2 from a gas stream for 14C analysis. Principal changes are the incorporation an automated system to maintain a fixed pressure in the CO2 trap and the use of a variable-speed diaphragm pump to pull the gas through the line, permitting control of the flow rate whilst maintaining an optimal trapping pressure. A turbomolecular pumping system with a liquid nitrogen trap is used to ensure good base vacuum prior to commencing extractions and during transfer of the trapped CO2. A cryo-cooler is used to maintain the water trap at -100°C during extraction, eliminating the need to use of large quantities of alcohol and dry ice. This basic apparatus was used for rounds 2 and 3 of the First Atmospheric Radiocarbon Intercomparison (FARI), organised by INSTAAR and NOAA/CMDL (Miller 2009).

In late 2010 the entire processing line was relocated to a new laboratory and further improved. A dedicated quadrupole mass spectrometer (QMS) has been added to the line, enabling on-line analysis of the exhaust gas to check on the completeness of H2O and CO2 trapping. Furthermore, a CH4 combustion oven, using CuO in a quartz tube, plus additional H2O and CO2 traps, has been added after the CO2 processing line. This has been driven by demand for 14C of CH4 of samples from wastewater and landfill studies, which typically are mainly composed of CO2 and CH4. An overview of these and other projects and our preliminary experience with the CH4 line will be given.

ReferencesMiller, J., C. Wolak, S. Lehman, C. Allison, H. Graven, T. Guilderson, R. Keeling, H. Meijer, T. Nakamura, T. Nakazawa, R. Neubert, A. Smith, J. Southon, X. Xu, Preliminary results from the first inter-comparison of Accelerator Mass Spectrometry atmospheric 14CO2 measurements, 13th CO2 Experts Meeting, Jena, German, 7th -10th September 2009.

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227

S03-P-029

WOOD PRE-TREATMENT PROTOCOLS AND MEASUREMENT OF TREE-RING STANDARDS AT THE OXFORD RADIOCARBON ACCELERATOR UNIT (ORAU)

STAFF R.A.(1), ReYnaRD l.(1)(2), bRocK f.(1), bRonK RaMSeY c.(1)

(1) University of oxford, oXfoRD, UnITeD KInGDoM; (2) Harvard University, caMbRIDGe, Ma, UnITeD STaTeS

AbstractThis poster presents the pre-treatment protocols for wood samples processed at the Oxford Radiocarbon Accelerator Unit (ORAU), including recent implementation of a purification method to α-cellulose for non-routine samples. We examine the long-term reproducibility of measurement on wood samples at ORAU through the >1000 14C determinations made on ‘known-age’ tree-ring standards processed in each AMS wheel since our present High Voltage Engineering Europa (HVEE) AMS system came online in September 2002. A discussion of ‘background’ measurements is also provided.

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S03-P-030

HIGH-THROUGHPUT LOW-COST ANALYSIS OF CARBONATE SAMPLES FOR 14C

ROBERTS M., bURTon J., beaUPRe S.


AbstractWe have developed an automated system for high-throughput, low-cost analysis of 14C in carbonate samples (e.g., corals, carbonate containing sediments, speleothems, etc.). In the process, samples are weighed into septa-sealed glass vials. Then, using a Gilson 271 Liquid-Handler, the vials are evacuated and injected with 1 ml of 85% phosphoric acid to acidify the carbonate to CO2. After sample preparation, racks of vials are transferred to the AMS system for measurement using our new gas-accepting ion-source. Analysis cost is about 1/5th the price of a traditional 14C carbonate analysis, with an analytical precision of better than 2%. Typical throughput is 50 to 60 unknowns per day.

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S03-P-031

CARBONATE SAMPLES: IS PRETREATMENT NECESSARY?

ROBERTS M., beaUPRe S., bURTon J.


AbstractIn the analysis of carbonate samples (e.g., corals, carbonate containing sediments, speleothems, etc.) for 14C, it is common to pretreat the samples to remove organic material. This pretreatment can be as simple as a water wash or as complex as ultrasonication in a hydrogen peroxide bath. As part of the process of developing an automated system for high-throughput, low-cost analysis of carbonates we have explored the necessity of this pretreatment. In tests, we have mixed together carbonate and organic materials each having differing but known 14C content. The mixtures were then acidified using phosphoric acid and the fraction modern of the resultant CO2 compared to the known fraction modern of the carbonate component. Our tests indicate that, to a very high degree, extensive cleaning of carbonate samples to remove organic material is not necessary.

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S03-P-032

14C SMALL BACKGROUND CORRECTION AND 14C BACKGROUND LEVEL OF FORAMINIFERA (FAROE-SHETLAND CHANNEL, NORTH ATLANTIC OCEAN)

OLSEN J.(1)(2), ReIMeR R.(2), ReIMeR P.J.(2)

(1) aarhus University, aaRHUS, DenMaRK; (2) Queen’s University belfast, belfaST, UnITeD KInGDoM

Abstract14C dating samples close to background levels is challenging and often requires knowledge on the 14C background level of the dating material. Here we report on the 14C background level of N. pachyderma sinistral taken from a core in the Faroe-Shetland channel, North Atlantic Ocean. Foraminifera samples were chosen at two different depths known to be older than 50 cal kyr. The samples were 14C dated and compared to our normal Icelandic spar calcite background. A further challenge when dating foraminiferas is that sample sizes are frequently much lower than 1mgC required for full size AMS graphite targets. We therefore analysed background foraminifera samples in the range from 1 mgC to as low as ~0.1 mgC in order to produce a 14C background correction procedure of unknown small foraminifera samples. Our results showed that foraminifera background samples were significantly younger than our Icelandic spar calcite hence underscoring the importance of using sample specific 14C backgrounds. Further we report on our small samples correction procedure.

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S03-P-033

RADIOCARBON DATING OF MUMMIFIED HUMAN REMAINS – APPLICATION TO A SERIES OF COPTIC MUMMIES FROM THE LOUVRE MUSEUM

RICHARDIN P.(1), coUDeRT M.(2), GanDolfo n.(1), VIncenT J.(1)(3)

(1) centre de recherche et de restauration des musées de france, PaRIS, fRance; (2) Musée du louvre, Service du Récolement des Dépôts antiques et des arts de l’Islam (SRDaI), PaRIS, fRance; (3) laboratoire de Mesure du carbone 14, lMc14, GIf-SUR-YVeTTe, fRance

AbstractMany French museums — museums of art and archaeology, ethnography, anatomy, and even natural history — keep in their reserves many mummified human remains. Beyond any ethical or deontological issues that arise with such collections, it is evident that these human bodies are an important part of our archaeological and historical heritage. The mission of a curator or everyone in charge of mummies is, not only to preserve them, but also to develop historical or scientific researches in the aim to improve our knowledge on their origin, the process of mummification and more simply to answer to following questions: who were these people, from where they came or how the mummies were collected? However, in most cases, all the documentation has disappeared and thus, out of any context, these mummies lose their interest for the scientific community. The dating of these mummies is often inaccurate, and nevertheless this parameter would be very interesting if the results are correlated with other chronological or analytical data, as for example the process of mummification or the diet.

This study has been carried out in the context of a multidisciplinary scientific program, initiated by the Louvre Museum, on a set of mummies from the Roman and Byzantine Period, found in the site of Antinoé (Egypt), deposited by the Louvre or sent by the State to several French museums. Numerous scientists — including archaeologists, chemists, physicists, dentists, paleopathologists, radiologists and geneticists — have worked together to share their knowledge and skill. We have recently developed a new method for preparing hair samples from mummies for AMS-radiocarbon dating. This method permits to reduce the size of samples thus preserving as much as possible the integrity of the body.

Thus, we have taken hair samples from 30 mummies, distributed in 8 museums around France, and also different fragments of textile or plant found near or on the bodies. We will present only a few results and conclusions showing the importance of the dating criterion. For example, AMS radiocarbon dates exclude the assumed filiation of a woman and her supposed son. Similarly, a hair sample from the head of a mummy presents a very different radiocarbon age from that of the hair covering her chest. This result shows that these hair come from another mummy and were probably placed there intentionally.

References1. Richardin P., Gandolfo N., Carminatti P., Walter P. (2011) A New protocol for radiocarbon dating of hair and

keratin type samples – Application to an Andean mummy from the National Museum of Natural History in Paris, Archaeological and Anthropological Sciences, 3(4), 379-384.

2. Sowada K., Jacobsen G. E., Bertuch F., Palmer T., Jenkinson A. (2011) Who’s that lying in my coffin? An imposter exposed by 14C dating. Radiocarbon, 53(2), 221-228.

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S03-P-034

PROCESSING OF CO2 SAMPLES COLLECTED USING ZEOLITE MOLECULAR SIEVE FOR 14C ANALYSIS AT THE NERC RADIOCARBON FACILITY (EAST KILBRIDE)

GARNETT M., MURRaY c.

neRc Radiocarbon facility, eaST KIlbRIDe, UnITeD KInGDoM

AbstractCartridges containing zeolite molecular sieve are used for the field-collection of CO2 from a variety of environments (e.g. atmosphere, soil respiration, evasion from surface waters) for AMS 14C analysis. Previously, application of heat and a vacuum was used to recover sample CO2 from the sieve, prior to cryogenic purification and graphitisation. An additional heating and evacuation stage was used to prepare the cartridge for the next sample. We have recently developed an alternative method using heating and purging with nitrogen gas to remove sample CO2 from the molecular sieve. An infrared gas analyser (IRGA) is used to monitor CO2 content in the purge gas allowing the recovery of CO2 to be monitored much more closely. The preparation of the cartridge for the next use is performed at the same time and the IRGA reading is used to verify that all sample CO2 has been completely removed from the sieve, ensuring no carry-over into the next sample. We present the results of a suite of standards of distinctly different radio- and stable- carbon isotope composition which we used to confirm the reliability of the new procedures. The new method has considerably reduced the time required to process a single sample from at least 2 hours, to 40 minutes, and allowed the minimum sample size to be reduced by half.

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S03-P-035

THE USE OF HOT-WASHED VIVASPIN™ FILTERS FOR PRETREATMENT OF BONE COLLAGEN FOR RADIOCARBON AND STABLE ISOTOPE ANALYSES: A REVISED BRONK RAMSEY et al. (2004) METHODOLOGY

SVYATKO S.V., HoPeR S.T., ReIMeR P.J.

Queen’s University of belfast, belfaST, UnITeD KInGDoM

AbstractThis study is aimed to test the cleaning procedure for Vivaspin™ filters developed by Bronk Ramsey et al. (2004) and currently widely used for pre-treatment of bone collagen subjected to stable isotope and 14C analyses. The AMS 14C measurements have been conducted on 28 bone collagen samples, 11 of which were pre-treated using the filters cleaned with ultrapure water (MilliQ™) at 90ºC in addition to the Bronk Ramsey et al. procedure. The results demonstrate that: a) the use of hot-water treatment facilitates the removal of glycerine from the surface of filter membrane and, therefore, helps to reduce the respective contamination; b) the new procedure is particularly effective for old bone specimens, however the difference decreases for younger samples.

ReferencesBronk Ramsey, C., T. Higham, et al. (2004). «Improvements to the pretreatment of bone at Oxford.» Radiocarbon 46(1): 155-163.

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S03-P-036

RADIOCARBON DATING OF HISTORICAL PARCHMENTS

BROCK F.


AbstractRadiocarbon dating of historical parchments can be problematic for a variety of reasons, in particular: the requirement of destructive analysis of valuable samples (and the reluctance of museums and archives to allow such sampling); uncertainty over the best pre-treatment techniques, especially for poorly preserved pieces, in order to ensure that dating can be completed with accuracy and precision; and (often unfounded) concerns about the accuracy and potential precision of 14C dates for such materials (especially relative to those achieved by non-destructive palaeographical and codicological techniques).

Only a handful of publications detail pre-treatment methods for radiocarbon dating of parchments, and these tend to focus on mild acid-base-acid (ABA) approaches. In this study, a range of pre-treatment techniques, including acid-only, mild and strong ABA methods, and collagen extraction, were applied to 6 known-age historical parchments from Great Britain, in varying states of preservation. Sufficient material for dating survived each pre-treatment method for all 6 parchments, even when relatively small amounts of material were treated, and regardless of the preservation state of the parchment. The pre-treatment yields, stable isotopic data (δ13C, δ15N and C:N atomic weight ratio) and radiocarbon dates for these different pre-treatments are presented here.

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S03-P-037

IMPORTANCE OF WOOD SAMPLING TO THE INTERPRETATION OF THE RESULTS OF AMS RADIOCARBON DATING

LAVIER C.(1), GanDolfo n.(2), locaTellI c.(3), RIcHaRDIn P.(2)

(1) laboratoire d’archéologie Moléculaire et Structurale (laMS), UMR8220-cnRS - Université Pierre et Marie curie (Paris VI), IVRY-SUR-SeIne, fRance;

(2) centre de recherche et de restauration des musées de france, PaRIS, fRance; (3) laboratoire d’expertise du bois et de datation par dendrochronologie, leb2d - SaS cIPReS, beSanÇon, fRance

AbstractIf the performances and the reliability of the AMS radiocarbon dating method are well known, the selection of wood samples to be dated is of utmost importance in the distribution of the results and in their interpretation. Indeed, curators, archaeologists or the other people in charge of patrimonial collections, take samples depending on their technical possibilities and/or to their access to the material, without taking into account the wood species and/or the way it was cut in the tree. It is the reason why one can regularly observe discrepancies between the results obtained by dendrochronology and the radiocarbon date measurements.

Some significant examples will show how the choice of the sample localisation mainly depends on the experience and the know-how of an archaeodendrometry specialist, able to realise microsamples in collaboration with researchers in radiocarbon dating. These case studies will also show that the interpretation of the results has to be made in several steps by both communities’ specialists, and will reveal the systematic errors ensued by the lack of a strict protocol.

ReferencesRichardin P., Gandolfo N., Moignard B., Lavier C., Moreau C., Cottereau E. (2010) Centre of Research and Restoration of the Museums of France – AMS Radiocarbon Dates List 1, Radiocarbon, 52(4), 1689–1700.

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S03-P-038

SOURCES OF EXTRANEOUS CARBON CONTAMINATION IN SAMPLES COLLECTED BY PREPARATIVE CAPILLARY GAS CHROMATOGRAPHY

ZHANG D., DRUffel e., XU X., SoUTHon J., SanToS G.

University of california, Irvine, calIfoRnIa, UnITeD STaTeS

AbstractWe conducted several experiments to evaluate the extraneous carbon sources introduced during the preparation and analysis of PLFA (phospholipid fatty acid) samples (i.e. methylation, solvent extraction and silica gel column separation) when performing 14C-PCGC analysis. The Δ14C value of our standard compound C-18 PLFA, corrected for dilution by 14C-dead carbon during methylation, matched that of a bulk sample analysis, demonstrating that the methylation occurs quantitatively without contamination. Extraneous carbon may be introduced from solvent treatment and column separation. GC chromatographs show that impurities manifest themselves as groups of small peaks or elevated GC base lines. Superimposed on the existing GC bleed, these impurities constitute the major part of the blank for PCGC analysis. Effects of these sources of extraneous carbon on the Δ14C results will be presented.

References1. Guaciara M Santos et al (2010) Blank assessment for ultra-small radiocarbon samples: chemical extraction

and separation versus AMS. Proceedings of the 20th International Radiocarbon Conference, edited by A J T Jull Radiocarbon, Vol 52, Nr 2–3, 2010, p 1322–1335

2. L. Zelles (1999) Fatty acid patterns of phospholipids and lipopolysaccharides in the characterisation of microbial communities in soil: a review. Biol Fertil Soils (1999) 29:111–129

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S03-P-039

MICROGRAM LEVEL RADIOCARBON (14C) DETERMINATION OF CARBONACEOUS PARTICLES IN FIRN SAMPLES: TOWARDS PRE-TREATMENT AND OC/EC SEPARATION

CAO F.(1)(2), ZHanG Y.l.(1)(3)(4), ZaPf a.(1)(3)(4), SZIDaT S.(3)(4), WacKeR l.(5), ScHWIKoWSKI M.(1)(3)(4)

(1) Paul Scherrer Institut, VIllIGen, SWITZeRlanD; (2) Guangzhou Institute of Geochemistry, chinese academy of Sciences, GUanGZHoU, cHIna; (3) oeschger centre for climate change Research, University of bern, beRn, SWITZeRlanD; (4) Department of chemistry and biochemistry, University of bern, beRn, SWITZeRlanD; (5) laboratory of Ion beam Physics, eTH Hönggerberg, ZURIcH, SWITZeRlanD

AbstractCarbonaceous particles (CP) which comprise organic carbon (OC) and elemental carbon (EC) are of increasing interest in climate research because of their influence on the radiation balance of the earth. Nevertheless, long-term concentration records of carbonaceous particles emissions are still inadequately understood. The method of microgram level radiocarbon (14C) determination on CP in ice has already been established and also proved to be a powerful tool to distinct and quantify natural (biogenic) and anthropogenic (fossil) sources of CP in the past (Jenk et al,. 2006). Before melting and filtering the ice samples for subsequent extraction of 14CO2, a rigorous decontamination step is required since the ice had been in contact with the drill and the packing material. This step includes removing the outer parts of an ice section with a bandsaw and rinsing with ultra-pure water (Sigl et al., 2009). However, this procedure can not be applied for the upper 10 to 50 m of ice cores (termed firn, thickness depending on glacier) which has lower density and higher porosity. In this study, we developed a new decontamination method for firn samples consisting in chiselling off the outer parts instead of rinsing them. Analysis of artificially produced clean ice results in procedural blanks per filter of 2.8±0.1 μgC for OC and 0.3±0.1μgC for EC, which is relatively low compared to the expected OC and EC amounts in the upper part of Alpine ice cores. Furthermore, we also optimized the method of separating OC and EC for the subsequent 14C analysis by using a thermal-optical separation in contrast to the purely thermal separation. To validate our new method, the concentrations of OC and EC as well as their corresponding fraction of modern carbon were investigated for firn samples from Jungfraujoch and Fiescherhorn ice core samples which had been previously analysed by the old method.

References1. Jenk, T.M., S. Szidat, M. Schwikowski, H.W. Gäggeler, S. Brütsch, L. Wacker, H.-A. Synal, M. Saurer,

Radiocarbon analysis in an Alpine ice core, Record of anthropogenic and biogenic contributions to carbonaceous aerosols in the past (1650-1940), Atmos. Chem. Phys. 6, 5381-5390 (2006).

2. Sigl, M., T.M. Jenk, T. Kellerhals, S. Szidat, H.W. Gäggeler, L. Wacker, H.-A. Synal, C. Boutron, C. Barbante, M. Schwikowski, Towards radiocarbon dating of ice cores, J. Glaciology 55, 985-996 (2009).

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S03-P-040

A STUDY ON TRAPPING CO2 BY USING THE MOLECULAR SIEVE FOR THE 14C AMS SAMPLE PREPARATION

CHOE K.(1), KanG J.(1), lee J.H.(1), SonG S.(1), SonG Y.M.(1), YUn M.H.(1), KIM J.c.(2)

(1) ncIRf, Seoul national University, SeoUl, SoUTH KoRea; (2) Dept. of Physics and astronomy, Seoul national University, SeoUl, SoUTH KoRea

AbstractIn the Seoul National University AMS laboratory, we are now planning to develop an automatic sample preparation system for higher throughput of the 14C dating [1, 2]. This system will consist of several sections which include combustion line, CO2 trap, graphitization, and so on. We are usually collecting CO2 by cryogenic trapping. However, since handling liquid nitrogen is expected to be not so easy, we are interested in replacing the cryogenic method with the molecular sieve method for the collection of CO2. In this study, we are mainly comparing the performance of these 2 methods; cryogenic trapping method and molecular sieve method. As a molecular sieve, zeolite 13X is used [3], and as test samples, we use the oxalic acid standard (NIST SRM 4990c), IAEA-C4, graphite powder in high purity, and archaeological charcoals. The pMC values and the radiocarbon ages obtained for samples prepared by above 2 methods are very close each other. We especially focused on the memory effect of the molecular sieve that means the contamination by CO2 from previous sample, which can cause errors in the age determination. To reduce this effect, we made He gas flow through zeolite container for several minutes in high temperature before the CO2 is introduced. By the addition of this stage, we have obtained more reliable result.

References1. L. Wacker, et al., Nucl. Instr. and Meth. in Phys. Res. B 268 (2010) 931-9342. W. Hong, et al., Radiocarbon 52 (2010) 1277-12873. M. Ruff, “Radiocarbon Measurement of Micro-Scale Samples - A carbon dioxide inlet system for AMS,” Ph.D.

thesis at the dept. of Chemistry and Biochemistry, the University of Berne (2008) 65-67

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S03-P-041

A PUZZLING 14C RESULT OBTAINED FOR CARBONIZED WOOD SAMPLE EMBEDDED IN VOLCANIC LAVA

LEE J.H.(1), cHoe K.(1), KanG J.(1), SonG S.(1), SonG Y.M.(1), YUn M.H.(1), KIM J.c.(2)

(1) ncIRf, Seoul national University, SeoUl, SoUTH KoRea; (2) Dept. of Physics and astronomy, Seoul national University, SeoUl, SoUTH KoRea

AbstractIt had been reported [1,2] that the characteristics of a very old wood charcoal are different from those of modern wood charcoal by its preservation state. Then it can be assumed that these differences may induce some difficulties for a radiocarbon dating of the very old wood charcoal samples. Fortunately, for this curiosity to be studied further, a carbonized trunk of Prunus pendula for. acendens tree, buried inside of lava was found at the Hantan River lava plateau of Korean peninsula. 14C date of this sample has been previously measured as > 30 000 BP. However, separate 14C results of its outer crust and inner wood part showed a considerable difference exceeding estimated age differences by tree ring counting. Accordingly, to study the reason for this discrepancy, optical microscopy and FTIR (Fourier Transform Infra-Red spectroscopy) were performed to examine the differences of structural and chemical states of the samples. Along with them, to have a reference data and expand understanding for a very old wood charcoal, we applied the same analyzing tools (AMS, FTIR, optical microscopy) to a variety of old wood charcoals excavated from different chronological stages such as Bronze, Neolithic, and Paleolithic sites. The result of these observations will be discussed.

References1. Ilit Cohen-Ofri, Lev Weiner, Elisabetta Boaretto, Genia Mintz, Steve Weiner, “Modern and Fossil charcoal:

aspects of structure and diagenesis”, Journal of Archaeological Science 33 (2006) 428-439.2. N R Rebello, I Cohen Ofri, R Popovitz-Biro, O Bar-Yosef, L Meignen, P Goldberg, S Weiner, E Boaretto,

“Structural Characterization of Charcoal exposed to high and low pH: Implications for 14C Sample Preparation and Charcoal Preservation”, Radiocarbon 50 (2008) 289-307.

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S03-P-042

PYROLYSIS-GC/MS OF ARCHEOLOGICAL WOODS CONSERVED WITH POLYEHTYLENE GLYCOL

NISHIMOTO H.(1), naKaMURa S.(2), oHTanI H.(3), naKaMURa T.(4)

(1) aichi University, MoYoSHI, JaPan; (2) Kanazawa Gakuin University, KanaZaWa, JaPan; (3) nagoya Institute of Technology, naGoYa, JaPan; (4) nagoya University, naGoYa, JaPan

AbstractArcheological woods conserved with polyethylene glycol (PEG) were analyzed with pyrolysis GC/MS and compared to untreated woods and pure PEG. As the results, characteristic pyrograms and mass spectra indicating existence of PEG were observed in the conserved woods, and PEG was detected clearly. Peak area in the pyrogram depends on amount of pyrolysate. In order to quantitative analysis of PEG in the conserved woods, a standard curve was generated to specific peaks characterizing PEG measured from woods (castanea crenata) including from 1 to 20% PEG. The curve is almost appropriate and it indicates that reliable radiocarbon dating of archeological woods impregnated with PEG will be available by calibration using the standard curve. The conserved wood has been regarded as a contaminated sample for radiocarbon dating. Pyrolysis GC/MS has ability to expand this limitation.

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S03-P-043

PREPARATION INFLUENCE ON THE CONTENT OF RADIOCARBON – DARK LAYERS IN SPELEOTHEMS CASE STUDY

HERCMAN H.(1), PaWlYTa M.(2), leReaH Y.(3)

(1) Institute of Geological Sciences, PaS, WaRSZaWa, PolanD; (2) Institute of engineering Materials and biomaterials, Silesian University of Technology, GlIWIce, PolanD; (3) Department of Physical electronics, faculty of engineering, Tel-aviv University, Tel_aVIV, ISRael

AbstractDevelopment of measurement methods in recent years allows the analysis of ever smaller samples with increasing accuracy and sensitivity. It creates new possibilities of structural and chemical characterization of materials even with nanometric resolution.But beyond the advantages there are also pitfalls which can be formulated as a question if the results of nano-sample analyses are still characteristic for the studied layer, rocks or other larger object.

Presented study was inspired by the results obtained during the investigation of dark layers occurring within the speleothems in Domica Cave (Slovakia). It was necessary to demonstrate link between the occurrence of dark layers and periods humans activity in the cave at prehistoric times. Searching for genetic indicators detailed microstructure studies of dark layers separated from the Domica Cave speleothems was conducted. Occurrence of soot aggregates formed by burning fragments of beech wood was confirmed by high resolution SEM and TEM studies. Typical morphology of soot aggregates make possible to interchangeablyrecognize them even if their contentis extremelysmall. Chemical treatment is necessary for sample purification and effective extraction of carbon soot and for good microscopy specimen preparation. A big advantage of electron microscopy is opportunityto precise control structure and chemical changes after each performed steps. Several samples obtained as result of soot preparations, with different purities(a mixture of aggregates soot, “carbonaceous particles” and impurities - mainly clay), have been analyzed by radiocarbon method.

Surprisingly, it shows that the soot aggregates radiocarbon age is systematically shifted (about 500 and 1000 years) towards younger values with respect to previously obtained results (samples with no preliminary purification). This results appeared to cause some questions. First - if the identified problem is general or is merely accidental «mistake». Next question is whether this problem is characteristic only for samples from Domica Cave (that is a local) or occurs regardless of the cave location. Final question is if fractionation process occurs during the combustion of the sample or at the stage of its purification (preparation).

The first stream of research was to answer the question whether the reported problems are local or wider. We have studied speleothems samples and fragments of limestone from the cave walls from Poland, Slovakia and Slovenia. Similar effect was observed in all experiments. The radiocarbon age of “clear” soot aggregates was shifted to younger values in respect to samples with lower purity. Finally experiment with burning of recent wood was performed. We compare radiocarbon content in different combustion products and found the presence of similar effect.

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S03-P-044

STUDY ON THE ACCURACY AND PRECISION OF THE «PURE LIME LUMPS» TECHNIqUE FOR THE RADIOCARBON DATING OF OLD LIME BASED MATERIALS

PESCE G.L.A.(1), calcaGnIle l.(2), VeccHIaTTInI R.(3), QUaRTa G.(2), ball R.J.(1), D’elIa M.(2)

(1) bRe-cIcM, Department of architecture and civil engineering, University of bath, baTH, UnITeD KInGDoM; (2) ceDaD (centre for Dating and Diagnostic), Department of Innovation engineering, University of Salento, lecce, ITalY;(3) Department of Science for architecture, University of Genoa, Genoa, ITalY

AbstractThe recently developed “pure lime lumps” technique for the radiocarbon dating of old lime-based mixtures has been applied with interesting results over several years (Gallo, et al., 1998).Contrary to alternative techniques, which involve physical and/or chemical pre-treatment of specimens, this technique is based on a careful selection of a specific type of lump usually embedded in old lime-based mixtures (Pesce, et al. 2009). The founding principle underlying this technique is, in fact, the use of the “pure lime lumps”. These are lumps of pure lime which are not mixed with the aggregate and thought to originate from imperfect mixing of the wet mix or from an incomplete slaking process of the lime. Pure lime lumps contain the same lime as that used in other parts of the mixtures (Franzini, et al., 1990) but, importantly, as they are not mixed with aggregate they are free of contaminants such as sand grains or under burned pieces of limestone. For this reason this technique can dramatically reduce the errors in the radiocarbon dating. Although this technique has been used in several cases, a comprehensive study of its accuracy and precision is still missing. This paper will address this issue by showing radiocarbon results of 5 specimens of pure lime lumps coming from the same part (i.e. same stratigraphic unit in archaeological terms) and from the same depth of the external surface of a specifically chosen wall. The wall, in fact, is the façade of a medieval building located in the old city of Genoa (Italy) where it is based also one of the most experienced Italian research centres for the building archaeology. This wall has been dated independently from radiocarbon through the others archaeological methods commonly used in building archaeology such as mensiochronology of bricks.The lumps collected in this wall have been characterised with several techniques such as Raman spectroscopy, scanning electron microscopy and thermal analysis and then sent to the AMS laboratory.The precision of the radiocarbon dating results has been determined from the scattering of the data obtained from the analysed terms while accuracy has been estimated by comparing the 14C results with those obtained by the archaeological analysis of the wall.

References1. Franzini, M., Leoni, L., Lezzerini, M. & Sartori, F. 1990. On the binder of some ancient mortars. Mineralogy

and Petrology, 67, pp.59-69.2. Gallo, N, Fieni, L, Martini, M, Sibilia, E. 1998. Archèologie du bati, 14C et thermolumiscence: deux exemples

en comparaison. actes du 3e congrés International 14c et archéologie. 1998.3. Pesce, GLA, Quarta, G, Calcagnile, L, D’Elia, M, Cavaciocchi, P, Lastrico, C, Guastella, R., 2009. Radiocarbon

dating of lumps from aerial lime mortars and plasters: methodological issues and results from the S. Nicolò of Capodimonte Church (Camogli, Genoa – Italy). Radiocarbon.51(2), pp.867-872.

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S03-P-045

AUTOMATED GRAPHITE PRODUCTION SYSTEM FOR 14C-AMS IN YAMAGATA UNIVERSITY, JAPAN

KATO K.(1), ToKanaI f.(1), anSHITa M.(1), SaKURaI H.(1), oHaSHI M.S.(2)

(1) Yamagata University, YaMaGaTa, JaPan; (2) JaSco International co., ltd., HacHIoJI, JaPan

AbstractAccelerator mass spectrometry (AMS) was introduced into Yamagata University in 2010, and radiocarbon measurement has been carried out. In YU-AMS (Yamagata Univ. AMS), application of 14C-AMS is aimed at to microdose pharmacokinetics investigation, and sample preparation technique development has been started. Moreover, radiocarbon measurement of an environmental sample is also carried out simultaneously. With the installation of this AMS system, we also installed a new automated sample production system, which is composed of an elemental analyzer (EA), a glass vacuum line (GVL), and an isotope ratio mass spectrometer (IR-MS). These components are connected on-line, and up to 20 samples can be processed in automatically.

About 1 mg of carbon is extracted from a sample, and this is used for AMS measurement of YU-AMS. Sample gasification and gas separation are performed by EA. Sample gas is introduced into GVL and IR-MS at a rate of 90% and 10%, respectively from EA. Since stable isotopic fractionation is not observed associated with change in gas split ratio of 5:5, 8:2 and 9:1, sample gas split ratio between GVL and IR-MS is fixed to 9:1 in order to prioritize graphite production. Stable nitrogen, carbon and sulfur isotopic measurement is performed by IR-MS. GVL carried out carbon dioxide collection for graphite target production, measurement volume of carbon dioxide and hydrogen gas introduction for reduction of carbon dioxide. The collection rate of carbon dioxide in the GVL has been remained stable at approximately 90%, since 2010. Graphite quality prepared from automated system is confirmed by using IAEA reference materials, C1 – C9. The relationship of linearity between measured pMC of graphite prepared from our automated system and consensus values are in agreement for each reference material.

Twenty graphite samples are produced in approximately 25 hours, including the following procedures; iron powder reduction, EA and IR-MS setting, automated 20 samples processing, and heating for carbon dioxide reduction to graphite. Graphite production rate is 60 samples per week. Our automated graphite production system has the major advantages of being able to treat multiple samples, prepare a large number of graphite compared with batch method while maintaining their quality.

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S03-P-046

INCREASING THE RELIABILITY OF SMALL (15-300 μC) SAMPLES BY MINIMIZING AND CORRECTING FOR (MODERN) CONTAMINATION

AERTS-BIJMA A.T., MeIJeR H.a.J., been H.a., ZonneVelD, Van D., PlIcHT Van DeR J., PalSTRa S.

centre for Isotope Research, GRonInGen, neTHeRlanDS

AbstractThe Groningen HVEE 2.5MV Tandetron AMS employs standard size samples of 1.5 mgC. During the last decade, however, there is an increasing demand for smaller samples, like atmospheric trace gases, aerosols, macrofossils and precious materials. The ability to measure small samples with good accuracy is predominantly limited by contamination. We developed a protocol assuming that sample contamination consists of two types, with 14C activities 0% («fossil») and 100% («modern»). These materials are assumed to contaminate the sample with both an absolute amount, and an amount proportional to the sample size. Of the proportional fractions, only the modern part is observable (as «background» for large samples). However, our calibration process eliminates the influence of both proportional fractions. The constant fractions are determined by mass dependent measurements of fossil and modern samples, and are corrected for. We investigated the origin of both contaminations and improved procedures. The most important one is the introduction of iron pellets as catalyst instead of porous powder. This resulted in increased and more stable beam currents through our AMS system. In every measurement batch of 56 targets we determine the modern and fossil contamination contributions using a series of backgrounds and standards with sample sizes ranging 50-1000 μgC.This results in average values of fossil and modern contamination of 1.7 ±0.4 μg and 0.1 ±0.05 μg, respectively, for samples originating as CO2 (e.g. atmospheric samples). For combustion samples these numbers are 1.8 ±0.4 and 0.7 ±0.3 μg, respectively. As the modern contamination is much more important for the dating process (as it effectively limits the maximum determinable age), we have concentrated on this, and we succeeded to reduce it significantly in the last years. The absolute fossil contamination is much less of a problem. We have therefore even allowed this contamination to increase, as this led to lowering the modern contamination: a beneficial trade-off. The contamination in our samples is relatively large, especially for samples below 50 μg. Correction for this contamination using our method decreases the measurement uncertainty of the final result considerably. Possible contamination sources and correction strategies for these microgram scale size AMS samples will be discussed.

ReferencesRooij, van der Plicht, Meijer (2010) Porous iron pellets for AMS 14C analysis of small samples down to ultra-mcroscale size (10-25 µgC). Nuclear Instruments and methods in physics Research B, 268, 947-951.

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S03-P-047

ABA AND ABOx RADIOCARBON CROSS-DATING ON CHARCOAL FROM MIDDLE PLENIGLACIAL LOESS DEPOSITS IN AUSTRIA, MORAVIA AND WESTERN UKRAINE

HAESAERTS P.(1), DaMblon f.(1), nIGST P.(2)(3), HUblIn J.J.(3)

(1) Royal belgian Institute of natural Sciences, bRUSSelS, belGIUM; (2) Department of archaeology and anthropology, University of cambridge, caMbRIDGe, UnITeD KInGDoM; (3) Department of Human evolution, Max-Planck Institute for evolutionary anthropology, leIPZIG, GeRManY

AbstractDuring the last decades long series of radiocarbon dates were recovered on charcoal from Middle Pleniglacial loess deposits in Central and Eastern Europe (Haesaerts et al., 2010; Jöris, Street, 2008; Nigst, Haesaerts, in press). Although most of the results appeared consistent with their stratigraphical distribution, it was necessary to test the quality and reproducibility of the radiocarbon dates for the time window 40-30 ka uncal BP, taking the new methods of pretreatment (ABOx/ABA) into account (Douka et al, 2010). For this purpose 4 charcoal concentrations already dated in the Groningen laboratory were selected from 3 archaeological sites, in particular Molodova V in Western Ukraine (sub-unit 10-1 ca 32.6 ka BP), Willendorf II in Austria (sub-unit C4-2 ca 32.2 ka BP and sub-unit C8-2 ca 38.7 ka BP), and Vedrovice V in Moravia (top of the Bohunice Soil ca 40 ka BP). Each homogenized charcoal sample has been divided in 3 sub-samples submitted to ABA in Groningen laboratory on one side and to ABA and ABOx treatments in the Oxford laboratory on the other side. No mention was made of the origin and the estimated age of the samples. In the present paper we will discuss the results for these 4 sets of 3 dates which will allow a better evaluation of the reliability of the dates for the time window 40-30 ka BP with regard to the pretreatment methods implemented in each laboratory.

Acknowledgments: This research is a contribution to the MO/36/021 research project of the Belgian Science Policy. The radiocarbon dating was funded by the Max-Planck-Society. Excavations at Willendorf II have been funded by the Leakey Foundation, the Max-Planck-Society, the University of Vienna, and the Hugo Obermaier Prize.

References1. Douka, K., Higham, T., Sinitsyn, A.A., 2010. The influence of pretreatment chemistry on the radiocarbon dating of Campanian Ingnimbrite-aged charcoal from Kostienki 14 (Russia). Quaternary Research, 73(3), 583-587. 2. Haesaerts, P., Borziac, I., Chekha, V.P., Chirica, V., Drozdov, N.I., Koulakovska L., Orlova, L.A., van der Plicht, J., Damblon, F., 2010. Charcoal and wood remains for radiocarbon dating Upper Pleistocene loess sequences in Eastern Europe and Central Siberia. Palaeogeography, Palaeoclimatology, Palaeoecology, 291, 106-127. 3. Jöris O., Street, M., 2008. At the end of the 14C time scale--the Middle to Upper Paleolithic record of western Eurasia. Journal of Human Evolution, 55, 782-802. 4. Nigst, P., Haesaerts, P. L’Aurignacien en Basse Autriche: résultats préliminaires de l’analyse technologique de la couche culturelle 3 de Willendorf et ses implications pour la chronologie du Paléolithique supérieur ancien en Europe centrale. L’Anthropologie, in press.

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S03-P-048

MOLECULAR SIEVES IN 14CO2 SAMPLING AND HANDLING: ADVANTAGES AND AVOIDABLE PITFALLS

PALONEN V.(1)(2), TIKKanen P.(1)(2), oInonen M.(3)(2), VeSala T.(1), KeInonen J.(1)(2)

(1) Department of Physics, UnIVeRSITY of HelSInKI, fInlanD; (2) Radiocarbon analytics finland, UnIVeRSITY of HelSInKI, fInlanD; (3) finnish Museum of natural History, laboratory of chronology, UnIVeRSITY of HelSInKI, fInlanD

AbstractMolecular sieves are a promising way to sample and manipulate gaseous samples for radiocarbon analyses. Molecular sieve material can adsorb CO2 selectively, enabling sampling of CO2 from large air volumes in a small amount of adsorbent. The sieves are not caustic and can be regenerated via heating and re-used without removing the sieve material from its container. This results in ease of use and reduced risks of atmospheric contamination.The most common sieve material in use for sampling CO2 is the 13X zeolite. For environmental measurements starting this year, we have studied the properties of 13X zeolites in more detail.

For reliable 14CO2 sampling and results, there are several caveats that should and can be avoided. Firstly, it should be remembered that sorption is still a two-way process, the sieve material releasing some of the sampled CO2 already at room temperature. Secondly, the sieve material can have a memory effect of a few percents if regeneration time is less than two hours. Thirdly, hydrothermal damage to the sieve material should be avoided by applying lower temperatures at the beginning of sample desorption. Fourthly, significant fractionation can occur if sampling time is too long or the release of the sample from the sieve is not done properly.

In this contribution we discuss these caveats and propose technical solutions to optimize the molecular sieve sampling process. This forms a solid foundation for our future work in collecting gaseous samples within broad operational framework of atmospheric and environmental studies.

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S03-P-049

PRETREATMENT ADVANCES IN THE RADIOCARBON DATING OF PALAEOLITHIC REMAINS

DOUKA K.(1), WooD R.(2), bRocK f.(1), HIGHaM T.(1)

(1) oRaU, RlaHa, University of oxford, oXfoRD, UnITeD KInGDoM; (2) Radiocarbon facility, The australian national University, canbeRRa, aUSTRalIa

AbstractThe need for effective decontamination of old material (>35 ka BP) is well known to the radiocarbon and archaeological communities. While pretreatment chemistry has been continuously upgraded, it is only in the last few years that a suite of methodological advances has systematically targeted old samples. These new approaches have improved the chemical and physical cleaning of bone by ultrafiltration, charcoal by ABOx and shell by CarDS, prior to AMS dating. All three methods have been successfully applied in the Oxford Radiocarbon Accelerator Unit in the dating of Palaeolithic-aged material from Europe and the Near East. In this poster, we examine the nature of the technical improvements, present case studies that involve comparisons of carefully cleaned samples with known-age markers, and demonstrate how the application of the new techniques has transformed the understanding of our recent evolutionary past.

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S03-P-050

CAN CONTAMINATION OF CHARCOAL BE CAUSED BY DEGRADATION?

WOOD R.

australian national University, canbeRRa, aUSTRalIa

AbstractDegradation and contamination are closely linked phenomena. It is widely appreciated that as a material is degraded, the contaminant content may grow proportionally. In contrast, this poster aims to assess if and how degradation may cause contamination of charcoal. First, it will examine if contamination is added through oxidation in air, without the addition of humic substances. Second, it will test if differing amounts of contamination are added during the pretreatment of pristine high temperature charcoal and degraded low temperature charcoal. This has implications for the selection of appropriate pretreatment standards and in understanding why the ABA pretreatment protocol does not remove as much contamination as the ABOx-SC pretreatment.

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S03-P-051

BIOAPATITE RADIOCARBON AGE OF GIANT MAMMALS FROM BRAZIL

CHERKINSKY A.(1), DanTaS M.a.T.(2), coZZUol M.a.(2))

(1) University of Georgia, aTHenS, UnITeD STaTeS;(2) Universidade federal de Minas Gerais, belo HoRIZonTe, bRaZIl

AbstractWe have investigated the radiocarbon age and stable isotope composition of bioapatite from bone, enamel and dentine material from three different species of extinct giant mammals in South America. The samples of a giant sloth eremotherium laurillardi (Lund, 1842), a mastodons Toxodon platensis (Owen, 1840) and notiomastodont platensis (Ameghino, 1888) were collected in natural depressions on Neo-Mesoproterozoic litotipes, known as “tanks”, of Sergipe, Bahia and Rio Grande do Norte states. All studied samples have got no collagen which was decomposed in the result of high microbiological activity in this tropical region. So we have analyzed fraction of bioapatite which could be relatively good preserved even in such aggressive conditions.

The mineral fraction does not usually undergo microbiological decomposition, but may be exposed to isotopic exchange with environmental carbonates. The problem thus becomes one of separating the diagenetic carbonates without destroying the bioapatite. We offer a technique for removing the secondary diagenetic carbonates by treatment with diluted acetic acid in vacuum.

We demonstrate that that proper pretreatment of bone and tooth samples permits the separation of diagenetic carbonates from bioapatite, as long as the carbon in these samples has not degraded completely. Both bone or tooth tissue can be used for paleodietary studies and radiocarbon dating.

In two cases we have the bone enamel and dentine samples from the same individuals of n. platensis which were dated between 14 ka and 21 ka. The oldest tissue in both cases was dentine. The dating of the pairs of enamel and dentine did not show the simple results, however more often the dentine material was older.

The oldest data, about 22.5 ka for e. laurillardi, was obtained on bioapatite fraction of dentine. The all dates for T. platensis are between 10 ka and 11 ka radiocarbon years.The comparison with other dating techniques such U/Th and ESR has shown the reliability of the applied treatment and radiocarbon dating on bioapatite fraction in the certain conditions.

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S03-P-052

CARBONATE SAMPLE PREPARATION FOR 14C-DATING USING AN ELEMENTAL ANALYZER

LINDAUER S., KRoMeR b.

curt-engelhorn-Zentrum archaeometrie gGmbH, MannHeIM, GeRManY

AbstractSo far in radiocarbon dating the laboratories usually combust samples either using sealed glass tubes or, in increasing amounts, in an elemental analyser (EA). But for carbonates still the conversion to CO2 using acid is being used predominantly. Several authors (Yoneda et al. 2004, Skrzypek & Paul 2006, Burke et al. 2010, Park et al. 2010) studied the decomposition of calcite to CO2 using an elemental analyser for 13C or radiocarbon, which is more straightforward and faster than the acid dissolution method.

We tested the EA technique on land snails in the age range of 10.000 BP to modern, which had been dated before using the conventional hydrolysis method, and on shells whose age was not known beforehand. Our starting point were five chemical pretreatment steps including two procedures of Burke et al. 2010 and we subsequently focused on three simpler protocols in order to keep the sample preparation as simple as possible but still maintaining efficient decontamination of the samples.

The results are very promising. Our optimized sample preparation protocol involving methanol wash prior to leaching with 1% hydrochloric acid gave dates as obtained previously within error range. For the shells (lacking independent age control), the ages did not differ within errors between the protocols.

References1. Yoneda et al. 2004, Nuclear Instruments andMethods in Physics Research B 223–224:116–23.2. Skrzypek G, Paul D., Rapid Commun Mass Spectrom. 2006;20(19):2915-20.3. Burke et al., Deep-SeaResearchI57(2010)1510–15204. Park et al., Radiocarbon, 52, Nr 2–3, 2010, p 1295–1300

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S03-P-053

A NEW SIMPLE PRE-TREATMENT PROTOCOL TO REMOVE SYNTHETIC RESINS FROM RESTORED ARTWORKS TO BE DATED BY RADIOCARBON

cafoRIo l.(1), FEDI M.(2), lIccIolI l.(1), bRaccI S.(3), ManDo’ P.a.(1), SalVInI a.(4)

(1) Infn Sezione di firenze e Dipartimento di fisica e astronomia dell’Università di firenze, SeSTo fIoRenTIno (fI), ITalY; (2) Istituto nazionale di fisica nucleare, SeSTo fIoRenTIno, ITalY; (3) IcVbc - cnR, SeSTo fIoRenTIno (fI), ITalY; (4) Dipartimento di chimica Ugo Schiff dell’Università di firenze, SeSTo fIoRenTIno (fI), ITalY

AbstractThe issue of contamination in radiocarbon dating is well known. Contamination can affect not only archaeological findings but also artworks. In the latter case, the most common source of contamination is represented by the products used for restorations. In fact, restorers usually use resins of synthetic origin, i.e. extracted from fossil oil and from its by-products (see e.g. the well known Paraloid B72® for consolidating and preserving). In radiocarbon dating, of course, in the case they are not completely removed, these applied resins produce an apparent ageing of the samples. Indeed, the mechanical cleaning using traditional tools and the simple standard pre-treatment ABA protocol are not sufficient to remove them. The use of organic solvents, in particular petroleum solvents and chlorinated hydrocarbons, can allow us to fully remove these resins from the samples. The most widely used protocol in radiocarbon applications is based on the so-called Soxhlet extraction system, which is however very time consuming.

Here we propose a new chemical, more easily operated pre-treatment protocol, developed at INFN-LABEC in Florence. The new protocol is based on the use of chloroform (CHCl3) as solvent at room temperature. It was first tested on wood samples of known age (tree rings) treated on purpose with Paraloid B72. The effectiveness of the new pre-treatement was proven by the AMS-14C measurements and also verified by FTIR analyses prior and after treatment.

The new protocol was also applied on two case studies: the wood frame of an altar piece dated to the Reinassance and a painting on canvas of the early 20th century. For both, the use of synthetic resins with the aim at consolidating the support and the painted layers had been documented in previous technical reports. Also in these cases, the 14C measurements have clearly pointed out how effective is the chloroform-based protocol; here too, the removal of the contaminations was also verified using spectroscopic techniques.

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S03-P-054

THERE’S CARBON IN THE IRON DEAR LIZA, DEAR LIZA*

FALLON S., STRZePeK K., WooD R.e., alfoRD S.

The australian national University, acTon, aUSTRalIa

AbstractSince 2007 the ANU Radiocarbon laboratory has processed >8000 graphite targets for analysis on our SSAMS system. Following the pioneering work of Santos et al., (2007) we tested 3 iron powders (Alpha Aesar-325, Alpha Aesar-200 and Merck 10 micron) all of which had issues for graphitization and carbon content. The AA-325 “graphitized” the quickest ~2 hours with both the AA-200 and the Merck taking 3-4x longer. It was obvious from AMS measurements graphite made from carbon free coal that the AA-325 had the most carbon contamination (background coal gave an age ~46kya). We then added an oxidation step to the Merck iron, then a hydrogen reduction, this sped up the graphitization to ~3 hours and provided better AMS “backgrounds” (~49kya). We then tried Sigma Aldrich Fe2O3, which we reduce with hydrogen. This is now are best iron for graphite, it takes ~2.5 hours to graphitize and 14C free coal now has an AMS background of ~52kya that is also more consistent. We will also detail the current operating procedures for the ANU radiocarbon laboratory.

*H. Belafonte and Odetta – There’s a hole in the bucket (1961)

ReferencesSantos GM, Mazon M, Southon JR, Rifai S, Moore R. (2007). Evaluation of iron and cobalt powders as catalysts for 14C AMS target preparation. nuclear Instruments and Methods in Physics Research b 259(1): 308–15.

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S03-P-055

SAMPLE PREPARATION IMPROVEMENTS AT LABEC: THE CASE STUDY OF AN ETRUSCAN ARTWORK

CAFORIO L.(1), calZolaI G.(1), caRRaReSI l.(1), feDI M.(2), ManeTTI M.(2)

(1) Dipartimento di fisica e astronomia dell’Università di firenze e Infn Sezione di firenze, SeSTo fIoRenTIno (fI), ITalY; (2) Istituto nazionale di fisica nucleare, SeSTo fIoRenTIno, ITalY

AbstractSince the installation of the new accelerator at INFN-LABEC in Florence in 2004, the activity of the radiocarbon dating laboratory has raised, requiring both an increase of the sample preparation throughput and a major versatility in the treated materials.

The “standard” sample preparation line is based on an Elemental Analyser (EA) for the combustion of the pre-treated samples, and on a vacuum line where the CO2 is collected and then converted to graphite according to the well-known Bosch reaction. This line has been recently redesigned maintaining the EA, since this instrument provides us reliable and fast sample combustion and gases separation. In addition, the volumes were optimized and all the mechanical parts, e.g. the fittings, were properly chosen in order to improve the vacuum level and to decrease the possibility of contamination. The number of graphitization reactors was doubled (from 4 to 8) and the therein-installed pressure transducers were substituted with more sensible ones.

In those rare cases involving samples characterized by a complex nearly graphitic structure (e.g. burnt residues), the EA cannot be suitable for a complete combustion. For this kind of samples, we successfully tested the new sample preparation line that has been recently installed at LABEC and that is especially dedicated to aerosol samples,. This line is equipped with a homemade combustion oven, reaching up to 1000°C. The following gases separation is accomplished by both chemical and thermal traps.

As an example, the case of the dating of organic matter collected from an Etruscan bronze statue will be presented and discussed.

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S03-P-056

THE IMPORTANCE OF MEASURING COLLAGEN qUALITY INDICATORS TO OBTAIN ACCURATE RADIOCARBON DATES OF BONES

cafoRIo l.(1), feDI M.(2), SCIRE’ CALABRISOTTO C.(3), boMbaRDIeRI l.(3), ManDo’ P.a.(1)

(1) Dipartimento di fisica e astronomia dell’Università di firenze e Infn Sezione di firenze, SeSTo fIoRenTIno (fI), ITalY; (2) Istituto nazionale di fisica nucleare, SeSTo fIoRenTIno, ITalY; (3) Dipartimento di Scienze dell’antichità dell’Università di firenze, fIRenZe, ITalY

AbstractRadiocarbon dating of bones can be very useful in archaeological contexts, especially when dealing with funerary deposits lacking of material culture, e.g. pottery vessels.

Radiocarbon measurements of bone samples are usually performed on the extracted collagen residue. The content and the quality of collagen can vary a lot, mainly depending on bone preservation and diagenesis. Generally speaking, environmental conditions that can be typical of arid and tropical zones, such as low pH level of soils, high temperatures and percolating ground waters, can affect the conservation of collagen; at the same time, bones recovered in such environments are more likely to be contaminated. Nevertheless, possible contamination of sample can occur also in temperate zones.

While low collagen content is a condition we can not overcome, we can use several chemical and elemental indicators in order to assess the collagen quality. Among these, the C/N atomic ratio can be considered a good parameter for detecting low quality collagen and possibly contaminated samples. The measurement can be easily performed using an elemental analyzer when combusting the sample for graphitization, thus requiring no extra effort (or extra amount of sample) during the preparation procedure. C/N values that fall in the interval between 2.9 and 3.6 identify good collagen quality bone samples; on the other hand, samples resulting in C/N values that fall outside the recommended range should be suspected of contamination and potentially discarded.

Bone samples recently radiocarbon dated at INFN-LABEC in Florence have confirmed the importance of measuring C/N atomic ratios in order to assess the collagen quality. The bone material was collected from two necropolises of the Bronze Age period in Cyprus, an area characterized by environmental conditions that do not favor bone preservation. The data will be discussed underlying the relationship between measured C/N atomic ratios and the collagen quality of the samples, eventually comparing this information with the archaeological evidence.

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S03-P-057

14C AMS DATING OF ANTARCTIC MARINE SEDIMENTS USING LOW-TEMPERATURE COMBUSTION

MORETON S.G.(1), HIllenbRanD c.D.(2), o’cofaIGH c.(3), DoWDeSWell J.a.(4), XU S.(5)

(1) neRc Radiocarbon facility, eaST KIlbRIDe, UnITeD KInGDoM; (2) british antarctic Survey, caMbRIDGe, UnITeD KInGDoM; (3) Durham University, DURHaM, UnITeD KInGDoM; (4) Scott Polar Research Institute, caMbRIDGe, UnITeD KInGDoM; (5) SUeRc aMS laboratory, eaST KIlbRIDe, UnITeD KInGDoM

AbstractThe precise timing of the post-Last Glacial Maximum retreat of grounded ice from the Antarctic shelf is difficult to constrain due in large part to serious problems associated with the radiocarbon dating of Antarctic marine sediments. These problems are mainly caused by three factors. Firstly by the general absence of calcareous microfossils from the continental shelf which, elsewhere, are the most commonly used material for Accelerator Mass Spectrometry (AMS) 14C dating of marine sediments. Secondly,the difficulty of calibrating the radiocarbon ages of Antarctic Shelf sediments to calendar years due to the scarcity of information relating to the spatial and temporal fluctuations of the marine reservoir effect in Antarctic waters. Thirdly, the presence of reworked glacially-derived fossil carbon in the sediments which contributes to the acid-insoluble organic carbon (AIO) fraction of the sediments and leads to radiocarbon ages which are unrealistically old. Here we address the problem of the contamination of AIO AMS 14C measurement by fossil carbon. We prepared carbonate-free samples of marine sediment from three cores recovered from Marguerite Bay, Antarctica by digesting the samples in acid, rinsing, drying and homogenising the samples. Each sample was sub-divided into two aliquots. One group of sub-samples was combusted at high-temperature 900°C (HT) to convert the total AIO in the sub-sample to CO2. The other group of sub-samples was subject to a low-temperature 300°C (LT) combustion technique with the aim of converting the contemporary autochthonous carbon to CO2 but leaving the recalcitrant fossil carbon uncombusted. All CO2 aliquots from both the HT and LT combustions were converted to graphite in the same way and 14C was measured at the Scottish Universities Environmental Research Centre AMS Laboratory. In all instances the LT combustion resulted in a younger radiocarbon age than the equivalent HT combustion of the sample. We investigate and reject the possibility that the younger LT age could be the result of contamination of the LT sample by modern atmospheric CO2

during sample pre-treatment. Instead we conclude that the younger LT ages are the result of exclusion of contaminant fossil carbon by incomplete combustion of recalcitrant fossil material.

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S03-P-058

SAMPLE SPECIFIC PREPARATION—OVERVIEW OF TREATMENT METHODS APPLIED AT 14C LABORATORY ETH ZURICH

HAJDAS I., bIecHele c., bonanI G., MaUReR M., WacKeR l.

laboratory of Ion beam Physics, eTH, ZURIcH, SWITZeRlanD

AbstractAs many other preparation laboratories we are dealing with large spectrum of materials, applications and degree of preservation of samples submitted for analysis. On the top of it the amount of carbon remaining for 14C measurements varies widely. Our protocols follow standard treatment methods such as soxhlet, AAA for most of organic materials, Ultra Filtration of bones. In addition alternative preparation methods such as ABOX, collagen and cellulose separation are being used whenever required. Often two alternative treatments are applied to the same sample for a cross check. Some are performed to clarify problematic 14C ages.

For example, in previous studies of mammoth bones ultra filtration was shown to provide accurate age estimates. However we have also shown that replacement of Ultra filtration with a base step in the treatment of collagen provided comparable results in the case of the mammoth bones from Niederweningen site (Hajdas et al. 2009). Bones of different origin, preservation and age were treated with both methods. We will present results of such comparison performed on bones and other types of material.

ReferencesHajdas I, Michczynski A, Bonani G, Wacker L, and Furrer H. 2009. Dating Bones near the Limit of the Radiocarbon Dating Method: Study Case Mammoth from Niederweningen, Zh Switzerland. Radiocarbon 51: 675-680.

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S03-P-059

RE-EVALUATION OF ULTRAFILTRATION FOR BONE PRE-TREATMENT

FÜLÖP R.H., ReTHeMeYeR J., HeInZe S., KÖnIG S.

University of cologne, coloGne, GeRManY

AbstractWe conducted tests to establish the degree to which ultrafiltration during the pre-treatment of bone samples improve the quality of the obtained radiocarbon age. Three different bone standard materials have been used, namely, Oxford mammoth, Viri-H, and Viri-I, and on selected anthropological samples ranging in age between 200 and 8500 years BP. We tested two different ultrafilters (Sartorius Vivaspin®15 and Pall Macrosep® Advance), and analysed both the >30kD and <30kD size fractions that were collected from above and below the filters, respectively.

The bone samples that were processed using ultrafiltration produced ages that were slightly younger (but overlapping at two sigma) than those obtained from samples processed without ultrafiltration. Further, in the case of ultrafiltration, the <30kD collagen fraction yielded ages that were considerably younger than those obtained from the >30kD fraction. The younger ages obtained for the ultrafiltered samples are most likely due to the incomplete removal of glycerine from the membranes of the ultrafilters. We suppose that the pre-cleaning of ultrafilters by sonication in water, as proposed by Hüls et al. (2007), is not sufficient to completely remove the glycerine on the surface of the membranes. Similarly, the cleaning procedure using 0.1 M HCl proposed by Beaumont et al. (2010) does also leave young C-14 behind.

In our test series, samples pre-treated only with 1M HCl yielded results that were similar or better than those obtained from samples pre-treated with ultrafiltration. For example, the Oxford Mammoth standard, older than 147 kyrs, yielded pMC values of 0.18(0.03, 1sigma) and 0.11(0.03, 1sigma) for pre-treatment without and with ultrafiltration, respectively. Furthermore, the addition of a NaOH treatment step after decalcification does also not improve the results, even when the bone pore space is filled with sediment as in the case of the Oxford Mammoth standard.

Based on our bone pre-treatment test results we adopted the following pre-treatment process that excludes ultrafiltration: the surface of a 2-5 g sample is abraded and cleaned with Milli-Q water in an ultrasonic bath. If necessary, conservation products are removed with a sequence of organic solvents. The dried samples are decalcified with 1M HCl for at least 3 h at room temperature. Insoluble contaminants and humic substances are removed by adding Milli-Q water and thereby increasing the pH to about 3 while the sample is placed in the agitating water bath for 24 h at 60°C. The samples are then converted into gelatine, which is subjected to hot filtration (60°C) through pre-combusted glass fibre filters. Finally the gelatine is freeze-dried, combusted in an EA, and graphitized in excess of hydrogen.

References1. Hüls MC, Grootes PM, Nadeau M-J. 2007. How clean is ultrafiltration cleaning of bone collagen? Radiocarbon,

49(2):193-200.2. Beaumont W, Beverly R, Southon J,Taylor RE. 2010. Bone preparation at the KCCAMS laboratory.NIMB

268:906-909.

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S03-P-060

PRE-TREATMENT PROCEDURES AND qUALITY CONTROL AT THE NERC RADIOCARBON FACILITY-EAST KILBRIDE

BRYANT C.L.(1), cISneRoS-DoZal M.(1), cURRIe M.(1), ellIoTT f.(1), fReeMan S.P.H.T.(2), GaRneTT M.H.(1), GUllIVeR P.(1), MoReTon S.G.(1), MURRaY c.(1), neWTon J.a.(1), ScoTT e.M.(3), XU S.(2)

(1) neRc Radiocarbon facility, eaST KIlbRIDe, UnITeD KInGDoM; (2) aMS laboratory, Scottish Universities environmental Research centre, eaST KIlbRIDe, UnITeD KInGDoM; (3) University of Glasgow, GlaSGoW, UnITeD KInGDoM

AbstractThe NERC Radiocarbon Facility-East Kilbride provides radiocarbon analytical support to Earth and Environmental Scientists over a wide range of science areas, including climate science, biogeochemical cycling of carbon in terrestrial and aquatic systems, and marine, freshwater and polar research. We describe general quality control strategies for assessing accuracy and precision for CO2 and graphite preparation and 14C AMS analysis at the SUERC AMS Laboratory NERC-Recognised Facility. The diversity of sample types and pre-treatments applied in the laboratory has led to a customised approach to the use of process standards, which depends on individual project requirements and the amount and type of sample material available. Internationally recognised (TIRI, VIRI, IAEA) and in-house standard and background materials are used. Standard material may also be provided to external users for testing possible contamination due to sample handling prior to submission of samples to the Facility. We describe the range of pre-treatments and the quality control programme for routine techniques, recently developed methods (eg methane and carbon dioxide sampling and preparation for 14C analysis) and high precision 14C analysis.

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S03-P-061

ALTERNATIVE STORAGE METHOD FOR SEAWATER SAMPLES FOR INORGANIC CARBON ISOTOPE ANALYSIS

BRYANT C.L.(1), HenleY S.f.(2), MURRaY c.(1), GaneSHRaM R.S.(2), SHanKS R.P.(3)

(1) neRc Radiocarbon facility, eaST KIlbRIDe, UnITeD KInGDoM; (2) Grant Institute of Geosciences, University of edinburgh, eDInbURGH, UnITeD KInGDoM; (3) aMS laboratory, Scottish Universities environmental Research centre, eaST KIlbRIDe, UnITeD KInGDoM

AbstractSeawater storage methods were tested for total inorganic carbon (ΣCO2) δ13C and 14C applications. The aim was to overcome the problem of preserving samples when mercuric chloride poisoning could not be used for sample storage. Initial tests with glass bottles, using copper sulphate as biological inhibitor, were unsatisfactory. In comparison to glass bottles, foil bags are lighter, safer, similar in cost and allow sample collection and transfer to hydrolysis vessels without exposure of the sample to the atmosphere. The foil bags were tested as follows:

1. To test for procedural contamination and/or contaminants from the foil bags deionised water was stored for 33 days at +4o C (refrigerated) and -10o C, (frozen) followed by addition of IAEA-C2 14C standard (Rozanski, 1982; consensus value 7135±6 14C yrs BP) before hydrolysis. Results were within 1σ of consensus 14C values.

2. The effect of sample storage on δ13C and 14C results was tested by collecting shallow coastal seawater aliquots (Fife, UK) in foil bags. The samples were stored at +4oC and -10oC for 4-33 days before hydrolysis. Seawater from the same site was collected in evacuated hydrolysis vessels and hydrolysed within minutes of collection (δ13CVPDB‰=0.8). Mean δ13CVPDB for foil bag samples, across all storage times were 0.5±0.1 ‰ (refrigerated n=12) and 0.6±0.03 ‰ (frozen n=6). There was no significant difference (t-test, p=0.01) between refrigerated and frozen δ13C values, but refrigerated results were more variable. Mean Δ14C values for refrigerated samples were 84.6±4.4 ‰ (n=4) and for frozen samples 81.0±1.8 ‰ (n=2).

3. Longer term storage effects were examined using seawater from Ryder Bay, Western Antarctic Peninsula. Samples were collected from various sites and depths and stored either in foil bags, frozen (-10o C) within 2 hours of collection, or in glass bottles with immediate poisoning using copper sulphate. Mean Δ14C of sample pairs (frozen in foil bags and poisoned in glass bottles) were -118.86±2.19 ‰ (sample pair stored for 11 months) and -127.63±4.21 ‰ (sample pair stored for 21 months). The results for each pair overlapped within 1σ analytical error. For the same pairs δ13CVPDB values were 1.1±0.5 ‰ and 1.9±0.2 ‰. Further frozen foil bag samples from two sites were defrosted 11-13 months after collection for hydrolysis, then refrozen and defrosted 20-22 months later for repeat hydrolysis and δ13C and 14C analysis. For the first site mean Δ14C for initial and final hydrolysis was -154.0±0.1 ‰ and for the second site -156.4±1.7 ‰. The results for initial and final hydrolysis at each site overlapped within 1σ analytical error. For the same sites δ13CVPDB values were 0.2±0.2 ‰ and 0.0±0.1 ‰. Under the conditions tested, the foil bags were found to be promising for collection and storage of seawater samples for δ13C and 14C of ΣCO2.

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S03-P-062

BEHAVIORAL VARIABILITY IN THE ABA CHEMICAL PRETREATMENT CLOSE TO THE 14C AGE LIMIT.

SANTOS G.M., oRMSbY K.

University of california, Irvine, IRVIne, UnITeD STaTeS

AbstractA common chemical pretreatment for many of the organic matter samples undergoing 14C dating is the well-known ABA (acid-base-acid) chemical pretreatment, which is often applied to remove contamination by carbonates and humic acids. Although this pretreatment is relatively straightforward, and has been commonly used in most laboratories worldwide, there is no consensus among labs on the strength of the chemical solutions or even the temperature for such chemical digestions. Comparisons between 14C age results obtained by organic samples undergoing ABA against other wet oxidations, such as the acid-base-oxidation followed by stepped combustion procedure (ABOx-SC) or alpha cellulose on wood have sometimes suggested that ABA not always remove all contaminating C. In addition, if not all ABA treatments are the same; can a given ABA pre-treatment protocol be better than others or even compatible with other wet oxidation pre-treatments if rigorously applied? In this work, we compared 14C results on wood samples at or near the limit of 14C dating, pretreated with a standard ABA protocol used at the KCCAMS facility, with those obtained from ABA- and ABOx-SC prepared from aliquots of the same samples performed at ANU in 2001. Secondly, we subjected wood samples ranging from ~15ka yrs BP to 14C-dead to five selected published ABA pre-treatments. Third, we also evaluated the need of a higher strength final acid step of the ABA protocol (particular important for removing CO2 absorption when samples are submerged in alkaline solutions), as raised by Hatté et al. (2001). These tests were carried out to determine any age deviations of known age samples due to different chemical pretreatment strategies, as well as the most adequate ABA chemical pre-treatment to ensure low backgrounds of well-preserve samples. The 14C results of this empirical exercise will be shown and discussed.

ReferencesHatté, C. et al. 2001. Is classical acid-alkali-acid treatment responsible for contamination? An alternative proposition. Radiocarbon 43(2):177-182

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S03-P-063

SAMPLE TYPES AND SIZES WITH THE AUTOMATED SAMPLE TREATMENT FACILITY EA-HASE

PESONEN A.(1), oInonen M.(1), Palonen V.(2)

(1) finnish Museum of natural History, UnIVeRSITY of HelSInKI, fInlanD; (2) Department of Physics, UnIVeRSITY of HelSInKI, fInlanD

AbstractBroad use of radiocarbon methodology in Finland has motivated us to develop Elemental Analyzer (EA) combustion process and automated sample preparation line at the University of Helsinki. The EA combustion process has been compared with the Closed-Tube-Combustion method for liquid fuel samples to improve repeatability, throughput and user-friendliness of biofraction measurements in Finland (Pesonen et al 2012). The Helsinki adaptive sample preparation line (HASE) (Palonen et al 2012) has been previously applied separately for environmental samples and Zn-Fe –based graphitizations of fuel samples.

In this contribution we present the results of the logical extension of the development to combine the EA combustion and the Labview-controlled HASE line for multitude of sample types and sizes. We have performed two sets of measurements. First, radiocarbon concentrations of the selected set of VIRI intercomparison sample materials were measured to compare them with the consensus values. Secondly, we have made a measurement series with VIRI K and liquid fossil fuel materials by using variable sample size aiming to 1 – 0.05 mg AMS target sizes. These comparisons will guide us to confirm the sample material types and sizes to be measured with this particular EA-HASE facility in the future.

References1. V. Palonen, P. Tikkanen, M. Oinonen. HASE - The Helsinki Adaptive Sample Preparation line. 2012. to be

published2. A. Pesonen, M. Oinonen, V. Palonen. Elemental Analyzer combustion of liquid fuel samples for AMS biocarbon

measurements. 2012. to be published

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S03-P-064

APPLYING METHODS FOR MICROGRAM SAMPLES TO COMMON RADIOCARBON DATING MATERIALS

MAIR K.(1), lIebl J.(1), KUTScHeRa W.(1), neelMeIJeR c.(2), neUHUbeR S.(3), ReIcHe I.(4), STeIeR P.(1)

(1) University of Vienna, faculty of Physics, VIenna, aUSTRIa; (2) Institut für Ionenstrahlphysik und Materialforschung, forschungszentrum Dresden-Rossendorf, DReSDen-

RoSSenDoRf, GeRManY; (3) University of Vienna, Department of Geodynamics and Sedimentology, VIenna, aUSTRIa; (4) laboratoire du centre de Recherche et de Restauration des Musées de frances - UMR 171 cnRS, PaRIS, fRance

AbstractA freeze-drying, combustion and graphitization unit capable to treat samples down to 2 μg carbon was developed at the VERA facility for the special applications of dating human DNA [Liebl et al., 2010] and POC filtrates from glacier ice [May et al., 2011]. This setup introduces a carbon background during sample handling, freeze drying, combustion and graphitization of only 0.15 g C. To study the general applicability, we have applied the setup to small samples of materials more commonly encountered in radiocarbon dating: fibers from a transmission string (made of catgut) of an astronomical clock from the 16th century; small pieces of bone samples up to ~40 ka old; and carbonates derived from lacustrine sediments from the Lake Neusiedl, Austria. We generally applied downscaled versions of methods commonly used for larger samples (smaller vials, amounts of reagents, etc.).

The capability to handle µg amounts of carbon was not only useful when the samples were per se small (human DNA) or when the extraction of larger samples would have required disproportionate effort (POC filtrates), but also when a sample had to be divided, either in several aliquots to compare different pretreatment protocols (transmission string), or in several fractions to be measured separately (sediment carbonates from the Lake Neusiedl, Austria). It turned out that in some cases the amount of carbon actually extracted from the samples significantly exceeded the expectations. This allowed to prepare replicas to study the measurement precision.

Samples larger than 10 μg carbon result in a 14C/12C ratio measurement precision of typically 1%. The main drawback is presently a varying yield (either chemical or in ionization) for such small samples, which in some cases increases the uncertainty to up to 3%. In general, a good agreement with expected ages was found. Our study suggests that the common methods of sample pretreatment can be scaled down without disproportionately increasing the background, and that they can be applied to most sample materials.

References1. J. Liebl, R. Avalos Ortiz, R. Golser, F. Handle, W. Kutschera, P. Steier, E. M. Wild. Studies on the preparation of

small 14C samples with an RGA and 13C-enriched material. Radiocarbon 52/2-3 (2010) 1394-1404.2. B. May, C. Spötl, D. Wagenbach, Y. Dublyansky, J. Liebl. First investigations of an ice core from Eisriesenwelt

cave (Austria). The Cryosphere 5 (2011) 81–93.

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S03-P-065

AN ASSESSMENT FOR THE SAMPLE PREPARATION TO IMPROVE THE ACCURACY OF AMS 14C MEASUREMENTS: 14C CONTENTS AND AMOUNTS OF THE CONTAMINATION

TANI S.(1), HonG W.(2), PaRK J.(2), PaRK G.(2), KITaGaWa H.(1)

(1) nagoya University, naGoYa, JaPan; (2) Korea Institute of Geoscience and Mineral Resources (KIGaM), DaeJeon, SoUTH KoRea

AbstractTraditionally 14C data have been obtained by subtracting the measured value of 14C - free samples assuming on the contamination of modern carbon (blank subtraction). The assumption might be reconsidered to improve the accuracy of the 14C measurements because the contamination is not necessarily modern origin. An incorporation of extraneous carbon with a value other than modern carbon results in the uncorrected blank subtraction. Therefore the exact 14C contents of the extraneous carbon may be considered carefully to improve the accuracy of the AMS 14C measurements. Based on a series of the AMS 14C measurements of the samples with the different 14C content prepared from a mixture of 14C-free and modern oxalic acid solutions, 14C contents and amounts of the contamination have been assessed. In addition cellulose with different 14C contents, which was regenerated from a mixture of two dissolved cellulose (14C free and modern), were used for the assessment of the contamination during an acid-base-acid treatment of organic matters. We will discuss how more attention for blank subtraction should be paid when accurate 14C data are needed.

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S03-P-066

A WET OXIDATION METHOD FOR AMS RADIOCARBON ANALYSIS OF DISSOLVED ORGANIC CARBON IN WATER

LEONARD A.(1), KInG S.(1), bURR G.(2), THoMaS J.(3)

(1) University of arizona, TUcSon, UnITeD STaTeS; (2) national Taiwan University, TaIPeI, TaIWan; (3) Desert Research Institute, Reno, UnITeD STaTeS

AbstractWe present a method for the extraction of dissolved organic carbon (DOC) from water. The method is adapted from Burr et al. (2001) using the basic steps: 1) sample filtration, 2) acidification to liberate and remove dissolved inorganic carbon, 3) evaporation of the sample to isolate salts that include trace quantities of carbon, 4) combustion of the salts and 5) purification of CO2. Two significant improvements have been made to the earlier method. The first is to use wet oxidation with potassium permanganate to oxidize the organics and the second is the development of a reduction/oxidation purification procedure to remove sulfur and nitrogen oxides that form during the oxidation step. The advantage of the wet oxidation step is that it occurs at low temperature. The original method required quartz vessels to oxidize the salts at 900ºC. The vessels were expensive and could only be used for a limited number of samples as reactions between the quartz and salts at high temperature degraded their structural integrity. Vessels used for wet oxidation are less expensive and can be used indefinitely.

The blank fraction of carbon f and its mass dependence was determined from repeat analyses of salicylic acid produced from petrochemicals. For samples with a mass m above 0.5 mg, f = 0.0083±0.0011. For samples below 0.5 mg the blank follows a 1/m dependence as described by Donahue et al. (1990). The reproducibility of the method is demonstrated using repeat measurements from a variety of samples, including a sample measured using the previous technique. The virtues of the wet oxidation method are that it is inexpensive, produces a low blank and provides good reproducibility.

References1. Burr GS, Thomas JM, Reines D, Jeffrey D, Courtney C, Jull AJT and Lange T (2001) Sample preparation of

dissolved organic carbon in groundwater for AMS 14C analysis. Radiocarbon 43(2A), 183-190.2. Donahue DJ, Linick TW, Jull, AJT (1990) Isotope-ratio and background corrections for accelerator mass

spectrometry radiocarbon measurements. Radiocarbon 32(2), 135-142.

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S03-P-067

NEUTRAL RESONANT IONIZATION IN THE HIGH INTENSITY SPUTTER ANION SOURCE

VOGEL J., GIacoMo J., DUeKeR S.

Vitalea Science, DaVIS ca, UnITeD STaTeS

AbstractQuantification of absolute carbon isotope ratios with our AMS spectrometer implies a lack of mass bias in the cesium sputter negative ion source. A charge exchange incorporating ionization of sputtered neutral atoms with desorbed neutral cesium through neutral resonant ionization may describe some forms of the Middleton high intensity ion source used in AMS (1984). The excited states of Cs promote anion production at lower collision energies than the ground (6s) state atom. Cesium evaporated in front of a sample is initially promoted to the 6p and the metastable 5d states by primary ions and secondary electrons, with energy pooling to higher states. The blue plasma in sample pits noted by Middleton and Klein (1999) and observed in many AMS at high ion output can arise form ionized 6p cesium. The emitted photons are appropriate for promoting ground state 6s atom to a 7p state, where the ionization potential of the Cs atom is resonant with the electron affinity of carbon. We explore the mechanism of Cs neutral resonant ionization of sputtered atoms to produce anions with lower mass bias than the universally assumed surface ionization and suggest how this mechanism explains other behaviors of Cs sputter ion sources typically used in AMS that have heretofore resisted comparisons to SIMS sources.

References1. Middleton R. (1984) A review of ion sources for AMS. Nuc Inst Meth. B 5: 193.2. Middleton R, Klein J. (1999) Production of metastable negative ions in a cesium sputter source: Verification

of the existence of N2- and CO-. Phys Rev A 60: 3786.

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S03-P-068

14C/12C VARIATION OF BACKGROUND SAMPLE EXPOSED IN AIR ACCORDING TO GRAPHITE STRUCTURE AND AIR TEMPERATURE

PARK J., HonG W., PaRK G., SUnG K.

KIGaM, DaeJeon, SoUTH KoRea

AbstractBackground samples which had various graphite structures for example, filament, nanotube, graphene, were used for knowing how those sample exposed in air vary according to graphite structure and air temperature. Carbon filament structure is popular because when CO2 is reduced using an H2 and Fe catalyst for AMS measurement, produced carbon structure is carbon filament structure. When carbon filament exposed in cold air (3-4 degree) and in room temperature during 12h, their 14C/12C become high and 14C/12C of carbon filament exposed in cold air (3-4 degree) become very high (>1×10-13). Additionally when they put in oven (200 degree) during 12h, their 14C/12C becomes low. However when carbon nanotube and graphene exposed in air of cold (3-4 degree) during 12h, their 14C/12C doesn’t become high. This phenomenon is very useful when we develop reservation method of graphite sample made by reduction reaction of CO2 and improve the reduction procedure of graphite sample for AMS measurement.

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S03-P-069

ULTRA SMALL-MASS GRAPHITIZATION BY SEALED TUBE ZINC REDUCTION METHOD FOR AMS 14C MEASUREMENTS

XU X.(1), Gao P.(1)(2), SalaManaca e.(1)

(1) Keck carbon cycle aMS laboratory, Department of earth System Science, University of california, IRVIne, UnITeD STaTeS;

(2) Department of Geography, Peking University, beIJInG, cHIna

AbstractPrevious work has demonstrated that 0.015 to 0.1 mg C size of samples can be successfully graphitized by the sealed tube Zn reduction method for AMS 14C measurements at the Keck Carbon Cycle AMS facility at the University of California, Irvine [1]. A modified method based on [1] has been developed to prepare ultra small samples ranging from 0.005 – 0.015 mgC. In this method, reagent TiH2 is removed while the amount of Zn and Fe powder remain the same. The volume of the sealed reactor is further reduced by ~40% to ~0.75 cm3. Graphite targets produced by this method generally yield 12C+1 currents of about 0.5 μA per 1μgC, similar to methods reported by [1,2]. Change of Fe powder to Sigma-Aldrich (400 mesh) has yielded further improved backgrounds over Fe powder of Alfa-Aesar (325 mesh) used previously. Methods for both modern and dead carbon background corrections are adopted from [2]. Modern C background from combustion and graphitization is estimated to be 0.25±0.15 µgC, and dead C background is 0.17±0.15 μgC. The accuracy and precision of ultra small-mass samples prepared by this method are size and 14C content dependent, but is usually ± 4 to 5% for the smallest sample size of ~0.005 mgC, based on duplicate measurements of primary and secondary standards. AMS online δ13C measurement that allows for correction of both graphitization and machine-induced isotopic fractionation is the key for applying sealed tube Zn reducing method to ultra small-mass sample graphitization.

References[1] Khosh M.S., Xu X., Trumbore S.E. (2010) Small-mass graphite preparation by sealed tube zinc reduction

method for AMS 14C measurements. Nucl. Instr. and Meth. in Phys. Res. B 268: 927–930.[2] Santos G.M., Southon J.R., Griffin S., Beaupre S.R. and Druffel E.R.M. (2007) Ultra small-mass AMS 14C

sample preparation and analyses at KCCAMS/UCI Facility. Nucl. Instr. and Meth. in Phys. Res. B 259, 293–302.

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S03-P-070

STEPPED-PYROLYSIS 14C DATING OF TOTAL SOIL ORGANIC MATTER (SOM) IN LOESS-PALEOSOIL

CHENG P., lU X.

Institute of earth environment,chinese academy of Science, XI’an, cHIna

AbstractRadiocarbon dating of loess-paleosoil is notoriously problematic due to its heterogeneous mix of multiple organic fractions, each of which may have a different radiocarbon age. The onerous chemical extractions for SOM (soil organic matter) fractions do not always produce satisfactory 14Cdates. Thus, this paper aims at confirming the very fraction that can be used to decide the real age by a method in which pyrolysis-combustion is carried out to partition SOM into pyrolytic volatile (Py-V) and pyrolytic residue (Py-R) fractions at different pyrolytic temperatures. First, the known age palesoil samples are used to get the appropriate pyrolytic temperature condition. The preliminary results show that the reliable fraction can be obtained from the Py-V at 600℃-800℃. However, affected by penetration and subsequent decomposition of rootlets and/or translocation/percolation of soluble organic substances,most of the young carbon in the Py-V fractions is extracted at 0℃-200℃, 200℃-400℃, 400℃-600℃, while the oldest carbon in the Py-R fraction is extracted at 800℃, in which the old parent and detrital materials may contain. In addition, we also find that fraction age is proportional to temperature, while the ages of Py-V fractions are younger than those of the Py-R fractions. Finally, with guidance of this method, we successfully established thechronological framework of Luochuan loess-paleosoil sequence since the last 25,000 years. This application of temperature-stepped-pyrolysis approach will provide us with a new way to improve the accuracy of 14C dating of loess-paleosoil.

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S03-P-071

A RAPID METHOD FOR PREPARING HIGH CONCENTRATION CH4 GAS SAMPLES FOR 14C ANALYSIS BY AMS

XU X., PacK M., STIllS a., cZIMcZIK c.

Keck carbon cycle aMS laboratory, Department of earth System Science, University of california, IRVIne, UnITeD STaTeS

AbstractSources of methane (CH4) gas, such as peatlands, clathrates, biogas and natural gas can be distinguished via their radiocarbon content and stable carbon and hydrogen isotopic signatures. Radiocarbon analysis of CH4 is generating increasing interest for constraining the global CH4 budget and in evaluating the effect of global warming on CH4 emissions from peatlands in the Polar Regions. Gas samples from peatlands may have high CH4 concentrations to provide adequate CH4-carbon for 14C-AMS analysis in <100 mL samples.

We have developed a rapid method for preparing high concentration CH4 gas samples for 14C analysis by AMS. It is a continuous ultra high purity (UHP) zero air flow-through combustion system. Samples are injected by syringe into the airflow and are carried through a series of traps for purification and combustion. At first carbon monoxide (CO) is converted to carbon dioxide (CO2) by a 300°C CuO furnace, followed by a liquid nitrogen trap to separate all CO2 (i.e. both CO+CO2 fractions). After that, non-condensable CH4 is combusted to CO2 by a CuO furnace at 900°C (Lindberg/Blue M Tube Furnace, Thermo Scientific). The resulting CO2 and H2O from CH4 combustion are further separated cryogenically on the vacuum line and the purified CO2 is graphitized by the sealed tube Zinc reduction method [1]. A flow meter is utilized to control the carrier gas flow rate in order to ensure complete separation and combustion. Preliminary tests on mixtures of CO2 (combusted from OX1) and dead CH4 show satisfactory yields. Consistent 14C results of standards and acceptably low blanks (better than 44,000 14C yr) confirm good separation and recovery of the gases in our rapid flow-through procedure.

References[1] Xu, X., Trumbore, S.E., Zheng, S., Southon, J.R., McDuffee, K.E., Luttgen, M., Liu, J.C. (2007). Modifying a

sealed tube zinc reduction method for preparation of AMS graphite targets: Reducing background and attaining high precision. Nucl. Instr. and Meth. in Phys. Res. B 259: 320–329.

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S03-P-072

RAPID SAMPLE PREPARATION OF DISSOLVED INORGANIC CARBON (DIC) IN NATURAL WATERS USING A HEADSPACE-EXTRACTION APPROACH FOR RADIOCARBON ANALYSIS ON AMS

Gao P.(1), XU X.(2), ZHoU l.(1), PacK M.a.(2), GRIffIn S.(2), SanToS G.M.(2), SoUTHon J.R.(2), feRGUSon J.(2)

(1) Department of Geography, Peking University, beIJInG, cHIna; (2) Keck carbon cycle aMS laboratory, Department of earth System Science, University of california, Irvine, IRVIne,

UnITeD STaTeS

AbstractWe have established a high throughput method for preparing DIC samples for high precision 14C analysis by AMS, using a headspace-extraction approach based on Molnár et al. [1]. Briefly, 30 mL aliquots of seawater, under ultra high purity He atmosphere, are acidified by injecting 0.5 mL of 85% H3PO4. Then, the samples are maintained at 75°C for two hours, and the CO2 gases (~0.3-0.5 mg of carbon) in the headspace is then taken using a 60 mL syringe and cryogenically purified on a vacuum line. Readily available 60 mL I-Chem septum-sealed screw cap vials (Fisher # 05-719-432) are used for sample acidification, fitted with an additional black viton septum (Sigma Aldrich # 27355). Extensive tests have shown that the extraction procedures do not introduce 14C-free organic compounds that can bias the 14C results.

DIC waters prepared by dissolving calcite, an internal laboratory coral standard, and IAEA C-2 in acid-stripped seawater were processed and measured to evaluate the procedure. The 14C results for standards are consistent with the consensus values. Large numbers of duplicate measurements have established a precision of 1.7 ‰ for modern samples and an average background of 43,000 radiocarbon years for sample sizes larger than 0.3mg C. In addition, aliquots of 18 seawater samples collected from Newport Beach, Southern California were processed using the headspace-extraction method. The 14C results obtained are in excellent agreement with published values obtained with conventional DIC stripping (≤±2σ) [2]. Coupled with the sealed tube Zn reduction method [3], 20 water samples can be prepared and graphitized in less than 10 hours.

References[1] Molnár, M., Wacker, L., Synal, H., Janovics, R., Rinyu, L., Veres, M., Hajdas, I. (2011). 14C analysis of

groundwater down to the milliliter level, abstract SAM#8 in AMS12, Wellington, New Zealand.[2] Santos, G.M., Ferguson, J., Acaylar, K., Johnson, K.R., Druffel, E. and Griffin, S. (2011). Δ14C and δ13C of

seawater DIC as tracers of coastal upwelling: A 5-year time-series from Southern California, Radiocarbon 53(4): 669-677.

[3] Xu, X., Trumbore, S.E., Zheng, S., Southon, J.R., McDuffee, K.E., Luttgen, M., Liu, J.C. (2007). Modifying a sealed tube zinc reduction method for preparation of AMS graphite targets: Reducing background and attaining high precision. Nucl. Instr. and Meth. in Phys. Res. B 259: 320-329.

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S03-P-073

TESTING IRON POWDERS FOR CARBON GRAPHITIZATION FOR 14C-AMS

HÜLS C.M., RaKoWSKI a.Z., RIecK a., DReVeS a., naDeaU M.J.

leibniz-laboratory for Radiometric Dating and Isotope Research, KIel, GeRManY

AbstractA critical point to obtain good 14C-AMS results is graphitization, transforming the CO2 of a variety of materials into solid graphite targets. In many laboratories iron powder is used as a catalyst for the reduction from CO2 with H2 to solid graphite.

The quality of the produced graphite-iron mixture strongly depends on the properties of iron powder (grain size, grain form or/and purity), and parameters of the reactions (temperature, iron-carbon ratio). Since the old supply of iron powder (Alfa Aesar -325 mesh, >98% purity) used for graphitization in the Leibniz Labor for the last 15 years is almost gone, we started looking for a new suitable powder. We have tested 10 different iron powders from three different companies (Alfa Aesar, Sigma Aldrich, and Goodfellow) to determine the most suitable product for our reduction system and ion source. Pure and conditioned iron, and final iron-graphite mixtures were analyzed with SEM. Surprisingly, supposedly similar iron powders show quite different physical properties such as grain size and grain shape which have a significant influence on the ability to press the final product into target holders. The different iron powders were then tested with different iron-carbon ratios and varying temperatures to determine the most optimal parameters for this reaction with respect to performance in the AMS system (beam current stability, isotope fractionation). The results of these tests will be presented.

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S03-P-074

STATUS REPORT OF AMS GRAPHITIZATION LINES IN ATOMKI, HUNGARY

RINYU L.(1), KIMÁK Á.(2), oRSoVSZKI G.(2), oRSoVKSZI J.(2), VeReS M.(3), MolnÁR M.(1)

(1) Institute of nuclear Research of the Hungarian academy of Sciences, DebRecen, HUnGaRY; (2) University of Debrecen, DebRecen, HUnGaRY; (3) Isotoptech Zrt., DebRecen, HUnGaRY

AbstractDuring the last year a MICADAS type accelerator mass spectrometer was installed in Hertelendi Laboratory of ATOMKI. In this report we would like to present the status of our graphite preparation lines and how we have employed and tuned them to serve our new MICADAS system. An essential criterion for the good and reliable radiocarbon mass spectrometry measurements is the quality of the prepared solid graphite target. We have deployed and improved two different graphitization methods in our new AMS facility and tested them in the past few years.

One based hydrogen reduction was aimed to have higher precision and better blank, with better reproducibility but higher costs. The applied hydrogen reduction graphitization method using our test line was validated internationally on different types of AMS systems [1,2]. Nowadays we developed our routinely applicable high throughput system, which enables the handling of 20 parallel reactors. We will also introduce the performance test of the improved capacity hydrogen reduction graphitization system.

Beside the hydrogen reduction system we have also adopted the sealed tube graphitization method [3]. The rapid output and the low cost are the main advantage of this method whereby we are capable to handle numerous biomedical and environmental samples per day. After we carried out the first successful test measurements on the ETHZ MICADAS AMS we have developed a gas handling line, which is capable to routinely handle eight independent sealed tube reaction units simultaneously.

We have studied the influence of the graphite sample size on the important parameters of the AMS measurements, like the blank level, 12C- ion current and the scattering of standard values. The carbon content of the investigated samples was changed in the wide range from 0.15 to 1.0 mg on both systems.

This paper will represent a comprehensive study about the two different graphitization method applied in connection of a novel type (MICADAS) AMS system. Special features related to the specific AMS setup will be also discussed.

References[1] L. Rinyu, I. Futó, Á.Z. Kiss, M. Molnár, É. Svingor, G. Quarta and L. Calcagnile, Radiocarbon, 49 (2) (2007) 217.[2] M. Molnár, L. Rinyu, T. Nagy, É. Svingor, I. Futó, M. Veres, A.J.T. Jull, G.S. Burr, R. Cruz and D. Biddulph, Nucl.

Instr. and Meth. B, 268 (2010) 940.[3] L. Rinyu, M. Molnár, I. Major, T. Nagy, M. Veres, Á. Kimák, L. Wacker, H.-A. Synal, Nucl. Instr. and Meth. B,

(2012) in press.

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S03-P-075

IS ULTRAFILTRATION EFFECTIVE FOR ACCURATE 14C-DATING OF FOSSIL BONE EXCAVATED IN JAPAN?

MINAMI M., naKaMURa T.

nagoya University, naGoYa, JaPan

AbstractUltrafiltration can effectively remove low-molecular-weight (LMW) contaminants from bone gelatin to extract high-molecular-weight (HMW) protein that isderived from original bone collagen. Therefore, proper ultrafiltrationcan be effective for more accurate 14C dates of bones. However, we reported that 14C ages, δ13C and δ15N values of unfiltered gelatins were good agreement with the values of HMW gelatins for some well-preserved VIRI bone samples, suggesting that it is possible that unfiltered gelatins extracted from well-preserved bones could be enough to obtain accurate14C dates (Minami et al. in revison). To study the effects of ultrafiltration on 14C age for relatively poorly-preserved bones, we analyzed 14C ages of HMW gelatins and compared with the ages of unfiltered gelatins for some human bones excavated from medieval archaeological sites in the Yuigahama area, Kamakura, Japan, and some animal fossil bones collected from the Awazu submarine archaeological site, Shiga, Japan.

The Yuigahama human bones had more than 1% extractable gelatins. The unfiltered gelatins were dated to 700-800 BP, while HMW gelatins using ultrafiltration tended to show 0-50 yr-younger 14C than the ages of unfiltered gelatins.The younger ages in the HMW gelatins could not be caused from contamination during ultrafiltration but removal of extraneous carbon introduced during burial from the unfiltered gelatins, because ultrafiltration of gelatin is suspected to make 14C ages older by contamination of the ultrafilter of Vivaspin™ 6 used in this study (Minami et al. in revision). The Yuigahama archaeological site exists at a beach that faces the Pacific sea, and therefore old carbon in seawater could have penetrated into the fossil bones during burial, bringing older ages than true ones.

Minami and Nakamura (2000) reported that the Awazu animal bones had less than 1% extractable gelatins and were dated to around 4300 BP for unfiltered gelatins. The XAD-purified hydrolysates showed older 14C ages than those of the unfiltered gelatins. We will present the 14C results of HMW gelatins of the animal bones for comparison with the ages for the unfiltered gelatins and XAD-purified hydrolysates, and discuss about whether utrafiltration is effective for accurate 14C-dating of fossil bone excavated from archaeological sites in Japan.

References1. Minami M, Nakamura T. 2000. AMS radiocarbon age for fossil bones by XAD-2 chromatography method.

nuclear Instruments and Methods in Physics Research B172: 462-468.2. Minami M, Yamazaki K, Omori T, Nakamura T. Radiocarbon dating of VIRI bone samples using ultrafiltration.

nuclear Instruments and Methods in Physics Research (in revision)

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S03-P-076

BONE DIAGENESIS IN A NATUFIAN SITE: THE CASE OF RAqEFET CAVE (ISRAEL)

REBOLLO N.(1), baRZIlaI o.(2)(1), YeSHURUn R.(3), bocQUenTIn f.(4), naDel D.(3), BOARETTO E.(1)

(1) Weizmann Institute of Science, ReHoVoT, ISRael; (2) Israel antiquities authority, JeRUSaleM, ISRael; (3) University of Haifa, MoUnT caRMel, ISRael; (4) cnRS in Jerusalem, JeRUSaleM, ISRael

AbstractOne of the main difficulties to date the Natufian culture is the low collagen percent in bones (≤ 2wt% yield) and specially the scarcity of macroscopic charred botanical remains that characterizes this period. In order to improve the absolute chronology of this important transitional period from hunting-gathering to village life in the South Levant, it is necessary to better assess the quality of samples dated, based on measurable parameters independent of the Radiocarbon date itself. This study is part of a long-term research project that involves a broad survey of human and animal bones from different Natufian sites in Israel, with the aim to re-assess the chronology of this period using Radiocarbon dating.

For the present study, samples were taken from skeletons recovered during the excavations at Raqefet Cave [1,2], a site located in the North of Israel. The human burials include typical Natufian funerary practices as well as artifacts such as flint implements and stone tools; the analyzed animal bones were recovered from within the burials or adjacent settings. A charcoal sample was obtained and dated from the sediment around one of the skeletons. The samples were pre-screened using Fourier Transform Infra-red (FTIR) spectroscopy for bone mineral crystallinity (Splitting Factor SF [3]), collagen content (wt% yield) and purity as well as for possible previous exposure to fire or oxidation [4]. Only samples with low SF and good quality collagen were prepared for Radiocarbon Dating.

In addition, an assessment of the microenvironment around the bones was made to better understand the most likely diagenetic processes. For this purpose, the sediments attached to the bones as well as sediments collected from their immediate vicinity were analyzed with FTIR spectroscopy. For selected cases where authigenic minerals derived from bone mineral dissolution were found both in bones and the surrounding sediments, cross sections of bones were prepared for microstructural and elemental analyses with SEM-EDX microscopy.

In this work, the relation of bone collagen preservation and mineral composition in sediments is discussed in the frame of possible active dissolution processes around the bones according to their spatial distribution in the cave. Also, the differences in diagenesis observed in human and animal bones are discussed.

References1. Nadel D. et al., Journal of the Israel Prehistoric Society (2009) vol. 39 p.212. Nadel D. et al., Journal of the Israel Prehistoric Society (2008) vol. 38 p.593. Weiner S. and O. Bar-Yosef. Journal of Archaeological Science (1990) vol. 17 p.1874. Shahack-Gross R. et al. Journal of Archaeological Science (1997) vol. 24 p.439.

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S03-P-077

BLANK ASSESSMENT FOR 14C SAMPLE PREPARATION AT THE NEW COLOGNEAMS CENTER

RETHEMEYER J.(1), fÜlÖP R.(1), HÖfle S.(1), WacKeR l.(2), PaTT U.(1), HeInZe S.(1), DeWalD a.(1)

(1) University of cologne, coloGne, GeRManY; (2) eTH Zurich, ZURIcH, SWITZeRlanD

AbstractThe new Cologne AMS facility is based on a 6 MV tandetron AMS system (High Voltage Engineering Europe; the Netherlands), which has been accepted in July 2010. Since then, the Radiocarbon group has performed numerous tests to assess and reduce sample contamination with exogenous carbon during the different steps of sample processing as well as the machine background.

We tested the standard acid-alkali-acid (AAA) extraction procedure of organic samples with different 14C-free and modern materials and found that no significant contamination is introduced here. Results for different sample handling and cleaning procedures indicate that care should be taken, e.g. when using pressurized air and organic solvents for the removal of contaminants, which seem to add old carbon. More detailed tests have been performed since our first report (Rethemeyer et al., in press) to determine the combustion-graphitization blank of organic samples with an automated graphitization system (Wacker et al., 2010). The contamination derived from the sample containers during combustion in the elemental analyzer (EA) depends on the container size and material (silver, tin). New data show that lowest blank values can be achieved with small tin boats (54,000 yrs BP; 4x4x11 mm) and capsules (3.5x9x0.1 mm), while blank levels were higher for larger tin boats (51,000 yrs BP; 8x8 x15 mm) and silver boats (50,000 yrs BP, 4x4x11 mm). We will also present results for a blank size series down to 50 µg C, which is performed to determine the size dependency of the contamination introduced during the combustion-graphitization procedure. Further tests of the graphitization procedure and quality of the AMS measurement include the conditioning of iron prior to sample graphitization, the Fe:C ratio and the effect of graphite storage.

Our laboratory is also performing gas chromatography based compound-specific 14C analyses. To determine blank levels of the isolation of individual organic compounds with a preparative gas chromatography more precisely, we performed additional tests to our first evaluation (Rethemeyer et al., in press) with dated GC standards as well as natural (modern) plant and (dead) sediment samples. The latter has the advantage that all steps of sample processing including solvent extraction and column chromatography are considered.

References1. Rethemeyer, J. et al., in press. Status report on sample preparation facilities for 14C analysis at the new

CologneAMS center. Nucl. Instr. and Meth. B.2. Wacker, L., Němec, M., Bourquin, J., 2010. A revolutionary graphitisation system: Fully automated, compact

and simple. Nucl. Instr. and Meth. B 268, 931-934.

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S03-P-078

BONE: TO POWDER OR NOT TO POWDER?

FERNANDES R.(1)(2), boUDIn M.(3), Van STRYDoncK M.(3), HÜlS M.(1), naDeaU M.J.(1), GRooTeS P.M.(1)

(1) leibniz-laboratory for Radiometric Dating and Isotope Research, KIel, GeRManY; (2) Graduate School Human Development in landscapes, KIel, GeRManY; (3) Royal Institute for cultural Heritage, bRUSSelS, belGIUM

AbstractRadiocarbon dating or isotopic analysis performed on bone collagen is today a well established practice providing, in most cases, reliable and useful information. Extraction of bone collagen is usually performed using variants of the gelatinization method proposed by Longin (1971). Longin’s collagen extraction method involved bone dissolution in a concentrated HCl solution followed by solubilisation in a hot dilute HCl solution. Later updates to the method included the introduction of a post-dissolution alkali step to remove humic acid contaminants (DeNiro and Epstein 1981). To remove atmospheric CO2 dissolved in the high pH solution, an extra acid step is often introduced prior to solubilisation. The sequential acid-alkali-acid (AAA) steps have become a standard practice.

Currently, most extraction methods involve the dissolution of small bone grains (dimensions around 1 mm), while in Longin’s method dissolution was performed on fine bone powder. Dissolution of bone grains, usually associated with a less concentrated acid solution, requires much longer treatment times (often days) to achieve full demineralization. In contrast, full demineralization using Longin’s method is achieved in 20 minutes, providing an optimal collagen yield. Thus, faster dissolution rates would certainly constitute an appealing methodological improvement. However, different workers have reported that the use of bone powder resulted in much lower collagen yields. These contrasting results are linked with the introduction of AMS radiocarbon dating methods and the lowering of required sample amounts. Sample losses occurring during the different treatment steps will have a larger impact on small sized samples (typically under 1 gram of bone) when compared with sample amounts reported by Longin (50 grams).

Here, we review the possibility of using fine bone powder in a standard AAA collagen extraction procedure, with rinsing steps performed under high speed centrifugation. Bone samples in different preservation state (assessed through Fourier transform infrared spectroscopy) and with varying collagen content were selected for comparative analysis. Comparison of collagen yields using a normal grain based method and a powder method indicate that the use of bone powder can maintain or even increase collagen yields. For both methods, analytical results will also be presented on comparative measurements of stable isotopes (δ13C and δ15N), and carbon and nitrogen contents.

The proposed bone powder method has the advantage of allowing for a fast AAA treatment (less than 3 hours) and also provides the possibility of performing parallel batch treatments.

References1. Longin, R., 1971. New method of collagen extraction for radiocarbon dating. nature 230, 241-242.2. DeNiro, M.J., Epstein, S., 1981. Influence of diet on the distribution of nitrogen isotopes in animals.

Geochimica et cosmochimica acta 45, 341-351.

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S03-P-079

EXTRACTION OF DISSOLVED INORGANIC CARBON (DIC) FROM SEAWATER SAMPLES AT CEDAD

MACCHIA M., D’elIa M., Gaballo V., bRaIone e., QUaRTa G., calcaGnIle l.


AbstractA dedicated sample processing line for the extraction of dissolved inorganic carbon (DIC) from seawater for AMS (Accelerator Mass Spectrometry) 14C analysis has been developed at CEDAD, the Center for Dating and Diagnostic of the University of Salento, Lecce. DIC is extracted from water sample as gaseous CO2 on a vacuum line almost entirely built in Pyrex™ in order to minimize the parts to be replaced because of corrosion processes due to salt water vapors. Seawater is sampled on site, poisoned and stored in glass bottles until processing and laboratory analysis is performed. The bottle is attached to a stripping probe which is then connected to a vacuum line in which a vacuum pressure of ~10-3 mbar is obtained by a rotary pump, vacuum pressure is monitored by thermocouple vacuum gauge. After pumping out atmospheric air, DIC is extracted and CO2 released by adding phosphoric acid through a Septa sealed tube. The released CO2 is then frozen into a liquid nitrogen trap while water vapors are frozen in a -80°C cold trap. No carried gas is used during the process and the complete extraction procedure is carried out in static vacuum conditions. The extracted gas pressure is measured by pressure transducer in a calibrated volume allowing the accurate estimation of the extraction yield. Gaseous CO2 is then transferred to the existing lines for the catalytic reduction to graphite for AMS analysis. The background of the line was estimated, by dissolving IAEA C-1 standard in MilliQ deionised water, to be of the order of 0.25 pMC. Tests were also carried out by dissolving in DI water IAEA C-2 standard and carbonates whose age was previously determined by standard procedures. Preliminary tests were also carried out by processing seawater sampled at different locations along the Ionian and Adriatic coasts and the system performances are presented in terms of functionality, background and samples throughput.

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S03-P-080

ADVANCES IN HANDLING ULTRA-SMALL RADIOCARBON SAMPLES AT THE LABORATOIRE DE MESURE DU CARBONE 14 IN SACLAY, FRANCE

DELQUÉ-KOLIC E., MoReaU c., coMbY c., DUMoUlIn J.P., caffY I., SoUPRaYen c., VIncenT J., QUIleS a., baVaY D., HaIn S., SeTTI V.

lMc14, GIf SUR YVeTTe, fRance

AbstractThe Artemis facility installed in Saclay, France in 2003, is dedicated to 14C measurements for researchers in the fields of quaternary geology, environmental sciences and archaeology. The whole preparation process developed at the origin for samples containing 1 mg of carbon has been tested in the recent years for smaller carbon contents. In particular, background and reference samples of carbonates and organic matters in the range of 1 to 0.01 mg of carbon have been prepared and measured to establish the limitation of our protocols and the improvements needed. We could observe that, down to 0.2 mg of carbon, satisfactory graphitization yields (80% and above) and low background values were obtained.

For less than 0.2 mg of carbon, the graphitization yield becomes erratic which induces changes. Smaller reactors (5 ml) have been tested and the reduction parameters (H2 pressure and temperature) have been adapted to this new configuration.

To lower the pollution by modern carbon, we have particularly paied attention to the combustion step by changing the proportion of CuO and the volumes of the combustion tubes. Furthermore, tests have been performed to evaluate the influence of our routine AAA pretreatment on 14C-free organic samples.

To limit the dead carbon pollution, which is generally considered to be introduced during the graphitization step, we have investigated another iron preparation before graphitization and compared it with our routine outgassing process at 600°C under vacuum.

In this presentation, we will expose the radiocarbon results obtained for micro-samples of background and standard samples prepared with our modified protocol. We will detail the changes realized all along the preparation and measurement process for the very small samples.

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S03-P-081

STATUS REPORT OF THE NEW AMS C-14 SAMPLE PREPARATION LAB OF THE HERTELENDI LABORATORY OF ENVIRONMENTAL STUDIES, DEBRECEN, HUNGARY

MOLNÁR M.(1), JanoVIcS R.(1), oRSoVSZKI J.(2), GÖncZI R(1), VeReS M.(3), leonaRD a.G.(4), KInG S.(4), lanGe T.(4), WacKeR l.(5), HaJDaS I.(5), JUll a.J.T.(4)

(1) MTa aToMKI, DebRecen, HUnGaRY; (2) Unviersity of Debrecen, DebRecen, HUnGaRY; (3) Isotoptech ZRt, DebRecen, HUnGaRY; (4) nSf-arizona aMS laboratory, TUcSon, aZ, UnITeD STaTeS; (5) eTHZ, ZÜRIcH, SWITZeRlanD

AbstractIn the case of AMS C-14 measurements demanding small amount of sample, the sample preparation technique is more critical because the amount of sample needed is at least a hundred times less than for the traditional counting technique. Thus, the accidental contamination and fractionation effects on the sample have major importance. The essence of these sample-preparation procedures is to get pure (uncontaminated) CO2 gas sample from the small amount of starting materials having various chemical compounds and properties.

In the Hertelendi Laboratory of Environmental Studies (Debrecen, Hungary) a new MICADAS type C-14 AMS (developed by ETHZ, Zürich) was installed in the summer of 2011. Therefore it needed a well established sample preparation laboratory. Preparations and laboratory space building construction were started in 2006 with special respect on AMS technique requirements. Sample preparation methods were learnt from NSF Arizona AMS facility (Tucson, USA) and ETHZ C-14 laboratory (Zürich, Switzerland). Main preparation equipment and lines were developed and built up according the philosophy and practice applied in the NSF and ETHZ labs.

An overview on the results for different type test samples (organic, bones, carbonates, groundwater, oxalic acid) are presented in this paper, like chemical yield, combustion/hydrolyses yield, throughput, mass dependent background and repeatability. Real samples (earlier measured in the NSF and ETHZ labs) and IAEA C-14 SRM reference materials (C-1 to C-9) were applied like control samples to test the performance of the whole AMS C-14 preparation chain in the new Hungarian laboratory. All the prepared test targets were measured in the new AMS system (EnvironMICADAS) of the Hertelendi Laboratory, Debrecen, Hungary.

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S03-P-082

STARCH EXTRACTION FROM WOOD FOR 14C MEASUREMENTS

STEINHOF A., alTenbURG M., MacHTS H., RaeSSleR M.


AbstractStarch is used in many kind of trees as energy storage for time spans of a few years. Therefore precise 14C measurements should be able to improve the understanding of this storage mechanism. There are already many procedures for the extraction of starch from plant materials, but many of these are made for plants with a high-starch content. Some procedures would be applicable to the starch extraction from wood also, but due to modification of the starch during the extraction process they don’t allow precise 14C measurement. We present a procedure for starch extraction dedicated to the starch extraction of wood and to 14C measurements.

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S03-P-083

REDUCTION OF THE BACKGROUND IN 14C MEASUREMENTS AT THE JENA AMS SYSTEM

STEINHOF A., alTenbURG M., MacHTS H.


AbstractThe reduction of the background in 14C measurements is investigated by heating the capsules for the samples in air and by oxidation with subsequent reduction of the iron used as catalyst for the graphitization. Furthermore the dependence of the increase of the background on the storage conditions is looked into. The progress made will be reported.

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S03-P-084

HOW ACCURATE ARE RADIOCARBON DATES FROM BIOAPATITE? DATING NEW KINGDOM AND NUBIAN BURIALS AT AMARA WEST, SUDAN

MEADOWS J.(1)(2), MIllaRD a.(3), bInDeR M.(3), SPenceR n.(4)

(1) Zentrum für baltische und Skandinavische archäologie, Stiftung Schleswig-Holsteinische landesmuseen, Schloss Gottorf, ScHleSWIG, GeRManY;

(2) leibniz-labor für altersbestimmung und Isotopenforschung, christian-albrechts-Universität zu Kiel, KIel, GeRManY;(3) Durham University Department of archaeology, DURHaM, UnITeD KInGDoM; (4) british Museum, Department of ancient egypt and Sudan, lonDon, UnITeD KInGDoM

AbstractAmara West, in Kush, or Upper Nubia, northern Sudan, was an important New Kingdom administrative centre from the reign of pharaoh Seti I until the end of Egyptian rule in this region (c. 1294–1069 BC). Inscriptions and cartouches allow precise dating of some public buildings from the pharaonic period. New Kingdom burials, if undisturbed, can be dated by their grave goods.

Archaeological dating becomes far less precise beyond the end of Egyptian control, although the town continued to be occupied, perhaps for another 2–3 centuries. The buildings can be dated by radiocarbon, as the mudbricks contain straw temper, but the chronology of the cemeteries is more challenging. Archaeological dating of post-pharaonic burials is problematic: undisturbed graves either lack grave goods, or only contain artefacts with a broad date range. Burials are also frequently disturbed, and any grave goods may not date the latest inhumation. Radiocarbon dating could be attempted, but a programme of stable isotope research has found that human bone collagen is rarely preserved. Furthermore, most burials cannot be unambiguously associated with fragments of textiles or plant remains.

However, given previous radiocarbon results on bone bioapatite from arid regions (reviewed by Zazzo and Saliège, 2011), we suspect that the mineral fraction of bones from Amara West may give reliable radiocarbon dates for these burials. Before embarking on a major dating programme, we are conducting a pilot study, using only burials whose dates can be confirmed independently of bioapatite preservation. Our project includes two individuals from a closed tomb, which has an inscription dating it to the mid-13th century BC; one individual from a later phase, with some skin and a linen shroud; and two unaccompanied burials with some collagen preservation. We also consider the structural and chemical properties of the bone samples, in order to explain why, or why not, the bioapatite radiocarbon results agree with the historical dates and control samples.

ReferencesZazzo, A., and Saliège, J.-F., 2011 Radiocarbon dating of biological apatites: a review. Palaeogeography, Palaeoclimatology, Palaeoecology.310(1–2): 52–61.

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S03-P-085

RADIOCARBON DATING OF WOOD SAMPLE PENETRAITED BY OIL FOUND DURING THE EXCAVATION IN AZERBAIJAN

ABBASOVA D.

Institute of Radiation Problems of aznaS, baKU, aZeRbaIJan

AbstractRadiocarbon dating is the dominant technique for organic samples of the last 40 000 years— wood (and charcoal), bone, peat, seeds, cloth, etc; it is important both in archaeology and in recent geology [1]. Different type of samples required special sample preparation procedure. One of the special samples is wood penetrated by oil which was found in Azerbaijan during archaeological excavation.

Sample preparation and radiocarbon dating analysis have been done in the Radiocarbon and Tritium Laboratory Rudjer Boškovic Institute in Zagreb.

At first oil extraction by solvents was provided by special scheme. After that sample was prepared and proceed to benzene synthesis for radiocarbon dating. Counting was done by Perkin Elmer equipment Quantulus.

Was identified that wood sample age is more than 55000 BP (<0.1 pMC).

References[1]. M J Aitken 1999 Archaeological dating using physical phenomena, Rep. Prog. Phys. 62 (1999) 1333–1376

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S03-P-086

CARBON BLANK INVESTIGATION ON qUARTZ FILTERS: A POTENTIALLY CRITICAL ASPECT FOR HIGH PRECISION MEASUREMENTS OF 14C IN PARTICULATE ORGANIC CARBON (POC)

STILLS A.(1), XU X.(1), ZenG f.(2), SanToS G.M.(1), SoUTHon J.R.(1), aDaM Z. c.(3), GRIffIn S.(1), RUacHo M.(1)

(1) Department of earth System Science, University of california, IRVIne, UnITeD STaTeS; (2) naSa/GSfc, GReenbelT, UnITeD STaTeS; (3) environment and natural Resources Institute, University of alaska, ancHoRaGe, UnITeD STaTeS

AbstractRadiocarbon analysis of particulate organic carbon (POC) has a variety of applications in carbon cycle studies. In most POC 14C methods, pre-baked quartz filters are often used to collect fine particulate fraction. Upon arrival at the laboratory, quartz filters loaded with samples are converted to CO2 by combustion and the yielded CO2 gas is either reduced to graphite or injected into a gas ion-source for 14C-AMS analysis. On the regular performance of 14C-AMS analysis, the quantification of blank is an integral part of the sample preparation procedure. Unfortunately, researchers have noticed that the magnitude and variability of the extraneous carbon found in processed quartz filters subjected to similar POC collection procedures can be large. As a result, filter blank has become one the biggest obstacles in preventing high precision measurements of POC 14C-AMS, when the amount of expected POC is small [1, 2]. However, the importance of having a good filter blank for small POC samples is often overlooked. Therefore a more thorough investigation of quartz filter blanks is necessary. In this study, several commonly used binder-free quartz filters, such as Whatman, SKC, Millipore, Pallflex and Sartorius QMF were investigated systematically for their C blanks and variations after different pre-baking regimes (from 500°C-900°C and different baking durations). Preliminary results show C blank of all filter brands ranges from 0.13 to 0.6 µgC/cm2, with ~30% to 50% variation in each brand, immediately after baking. No significant difference in C blank was found between baking temperatures of 500ºC and 900°C. 14C values of these pre-baked filter blanks were determined and vary from 0.5 to 0.8 (Fm). Potential sources of contaminations during filter preparation and processing and storage effect on filter blanks were investigated and will be discussed and presented.

References[1] Steier, P, Drosg, R, Fedi, M, et al. (2006). Radiocarbon determination of particulate organic carbon in non-

temperated, Alpine glacier ice. Radiocarbon, 48(1), 69-82.[2] Zeng, F. (2011). The Effects of Land Use and Human Activities on Carbon Cycling in Texas Rivers. UMI

Dissertation Services.

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S03-P-087

PERFORMANCE EVALUATION OF THE NEW DIRECTAMS GEOCHRONOLOGICAL SAMPLE PREPARATION LABORATORY

ADLER J., cHaTTeRS J., ZoPPI U., aRJoManD a.

accium bioSciences, SeaTTle, UnITeD STaTeS

AbstractThe Accium BioSciences AMS facility has been in operation since 2006. Over 27,000 targets have been measured thus far, the vast majority of which have been in support of contracted biomedical research. In early 2011, Accium launched the DirectAMS business unit to provide AMS services to the broader scientific community, particularly geochronological applications. The resulting influx of samples necessitated the build-out of a dedicated facility. This lab now features over 140 m2 of lab space dedicated to the pretreatment and graphitization of wood, charcoal, sediment and shell samples. Expansion of services to include bone and other sample types is ongoing.

In this paper we present results of a series of quality control samples of known age, including standards and geochronological charcoal and shell samples analyzed by other laboratories. Particular emphasis is placed on the characterization of the extraneous carbon introduced during sample preparation.

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286

S03-P-088

ARE CORAL CLASTS FROM A TURBID NEAR-SHORE REEF ENVIRONMENT A SUITABLE MATERIAL FOR RADIOCARBON ANALYSIS?

GULLIVER P.(1), PalMeR S.(2), PeRRY c.(3), SMITHeRS S.(4)

(1) neRc Radiocarbon facility (east Kilbride), eaST KIlbRIDe, UnITeD KInGDoM; (2) University of West Indies, KInGSTon, JaMaIca; (3) college of life and environmental Sciences, University of exeter, eXeTeR, UnITeD KInGDoM; (4) School of earth and environmental Sciences, James cook University, ToWnSVIlle, aUSTRalIa

AbstractThe use of massive corals, which are usually interpreted to be in-situ, to determine coral reef growth histories is well established. However, not all core records that are recovered contain in-situ, massive taxa, but may be volumetrically dominated by branched coral rubble (much of which may be ‘in-place’ (deposited in the environment in which it grew), rather than strictly in-situ. Recently there has been increasing awareness of the significance of reefs that occur in more marginal marine environments such as turbid-zone, inner-reef environments, which are characterised by episodes of elevated turbidity, low light penetration and periodic burial. These turbid-zone reefs can be considered to be of ecological and geological significance as they often exhibit high live coral cover and species diversity combined with a distinctive setting which has analogues in modern and palaeo-environments. However, from a chronological reconstruction perspective, the internal structure of these reefs are often dominated by coral clasts and rubble. This raises the question, how reliable are such rubble samples for date-based growth history reconstructions? In addition to the recognised effects of diagenesis or algal encrustations on the radiocarbon signature of coral samples, the high energy sedimentary environment of these reefs could potentially affect the deposition of the clasts resulting in different age populations being present in the same horizon. In order to test this, 5 replicate, samples from separate coral clasts were taken from two horizons of a core collected at Paluma Shoals, an inshore turbid-zone reef located in Halifax Bay, central Great Barrier Reef, Australia. Results show that where care is taken to screen the clasts for skeletal preservation, primary mineralogical structures and δ13C values indicative of marine carbonate, then reliable dates can be recovered from coral clast samples.

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SESSION 4

SPECIFIC COMPOUNDS: TOWARDS NEW APPLICATIONS

ConvenersYS Huang (USA), G. mollenhauer (DEU), S. Szidat (CHE)

DescriptionSince its first introduction in 1996, the technique of compound-specific radiocarbon analysis (CSRA) has been applied by a growing number of researchers to a diverse field of topics, including questions regarding carbon cycling in the natural environment and in a changing climate, anthropogenic pollution of the environment, and carbon source apportionment. With the growing number of applications, more and more different compounds and compound-classes are targeted. We invite contributions discussing both the technical challenges associated with preparation of CSRA samples as well as the applications of the technique to all of the above mentioned fields of research.

KeywordsCSRA, sample preparation, carbon cycling, source apportionment

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S04-P-089

RADIOCARBON DATING BONES USING THE AMINO ACID HYDROXYPROLINE: A VALIDATION OF THE METHOD

MAROM A., MccUllaGH J.S.o., HeDGeS R.e.M.


AbstractArchaeological bones are usually dated by radiocarbon measurement of extracted collagen. However, low collagen content, contamination from the burial environment or museum conservation work have previously lead to inaccurate results frustrating the dating of important archaeological sites, especially when old. We describe a method to date collagen hydroxyproline (Hyp, ~10% of collagen carbon) as a bone specific biomarker which removes impurities, thereby improving dating accuracy and confidence. Our method for the separation and isolation of Hyp from bone collagen, described at the last Radiocarbon conference [1], uses a mixed-mode (i.e. ion-exchange combined with hydrophobic mechanisms), semi preparative HPLC. The amino acids do not require derivatisation, and no organic solvents are used, thereby avoiding addition of carbon. Here we present data validating the applicability of the method. By dating known age bones we are able to show that our method does not add significant amounts of background carbon. On average we calculate that 3.3±1.4μg of contaminant carbon are added to each Hyp sample. We also demonstrate that both a deliberately contaminated bone and a ‘naturally’ contaminated archaeological bone, yielding erroneous dates when dated using the normal pretreatment method, can be dated accurately using this method. Finally, we demonstrate how a reliable date can be obtained from a bone with too little surviving collagen to be dateable by the bulk collagen method. We conclude that the method is suitable for dating archaeological bones suspected of being contaminated and low collagen bones. Application of the method can be used to obtain reliable radiocarbon determinations where previously this has been impossible.

References[1] McCullagh, J. S. O., A. Marom, R .E. M Hedges (2010). «Radiocarbon dating of individual amino acids from

archaeological bone collagen.» Radiocarbon 52(2): 620-634.

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289

S04-P-09O

EVALUATION OF MODERN AND OLD CARBON CONTAMINATION IN THE MEASUREMENT OF SMALL SAMPLES FOR CSRA

CISNEROS-DOZAL L.M.(1), bRYanT c.(1), PeaRSon e.J.(2), DUnGaIT J.(3), ellIoTT f.M.(1), aScoUGH P.(4)

(1) neRc Radiocarbon facility-east Kilbride, GlaSGoW, UnITeD KInGDoM; (2) newcastle University, neWcaSTle UPon TYne, UnITeD KInGDoM; (3) Rothamsted Research-north Wyke, DeVon, UnITeD KInGDoM; (4) SUeRc aMS facility, eaST KIlbRIDe, UnITeD KInGDoM

AbstractAt the NERC Radiocarbon Facility-East Kilbride we are working towards in-house preparation and analysis of specific compounds or groups of compounds, which invariably involves the technical challenges of minimizing contamination during chromatographic isolation and subsequent preparation of 14C targets from small samples (down to 100 µgC or less). We have been performing various tests towards the optimisation of these procedures for the isolation and preparation of compounds of terrestrial origin, in the first instance n-alkanes. Results showing some of the challenges are presented, including the degree of carbon contamination from modern and fossil carbon associated with compound isolation by preparative capillary gas chromatography, combustion and graphitisation processes. Preliminary results show modern contamination ≥1.0 µg C and 0.2 µg C from combustion and graphitisation respectively. Our tests include radiocarbon background materials used routinely at the facility (Iceland Spar Calcite, Bituminous coal) as well as known age materials we are developing as long term standards for compound-specific work. The latter include single year growth modern grass collected locally in 1984 with a known 14C value (previously used as a radiometric standard at the NERC Radiocarbon Facility). Whilst testing materials and processes for in-house standards, a concomitant goal is to establish materials suitable for wider use for radiocarbon analysis of n-alkanes of terrestrial origin, which would contribute to ongoing international efforts to establish 14C reference materials for CSRA.

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290

S04-P-091

RADIOCARBON AGES OF LAKE SEDIMENT CELLULOSE FROM LAKE BIWA, CENTRAL JAPAN

NAGASAWA S.(1), KITaGaWa H.(1), HonG W.(2), HaYaSHIDa a.(3), TaKeMURa K.(4)

(1) nagoya university, naGoYa, JaPan; (2) Korea Institute of Geoscience and Mineral Resources (KIGaM), DaeJeon, SoUTH KoRea; (3) Doshisha university, KYoTo, JaPan; (4) Kyoto University, bePPU, JaPan

AbstractLake Biwa is located in the central Japan. The surface area of the lake is 674 km2, and its drainage basin has an area of 3,850 km2. The lake sediments preserve valuable information of past climate and tectonic activity since the late Pleistocene. The establishment of precise age-depth model makes it possible to use full information preserved in the lake sediments. An age-depth model for the upper sediment (<50 ka) has been constructed based on the radiocarbon ages of terrestrial macrofossils and known-ages of widespread tephra. To discuss short-term climate change with reliable time scales, we need more high-resolution age-depth model. However there is a difficulty to improve the age-depth model because few macrofossils remain in the sediments. We focused on the cellulose fraction separated from the lake sediments (Lake Sediment Cellulose: LSC) as a potential material for radiocarbon dating. It is considered that LSC is aquatic origin, being less affected by the old carbon from the drainage basin. If the age-offset between atmospheric CO2 and LSC is minimized or constant, radiocarbon ages of LSC may be useful to improve the age-depth model of lake sediments. We compared two age-depth models generated by radiocarbon ages of terrestrial macrofossils and LSC in the lake sediment core (BIW08B). Furthermore we discuss the age-offset between them using the geochemical data sets (δ13C of TOC and LSC and C/N ratio).

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291

S04-P-092

CONTEMPORARY FRACTION OF BIS(2-ETHYLHEXYL) PHTHALATE IN STILTON CHEESE AND BUTTER BY ACCELERATOR MASS SPECTROMETRY

ONDOV J.(1), NELSON M.(1), VanDeRVeeR M.(2), bUcHHolZ b.(3)

(1) University of Maryland, colleGe PaRK, UnITeD STaTeS; (2) US food and Drug administration, UnIVeRSITY STaTIon, UnITeD STaTeS; (3) lawrence livermore national laboratory, lIVeRMoRe, UnITeD STaTeS

AbstractINTRoDUCTIoNEnormous quantities of bis (2-ethylhexyl) phthalate (DEHP), are produced annually for use as softening agents for plastics, fiber lubricants, fixing agents in cosmetics, and solvent for oil-soluble dyes and lacquers. DEHP is classified as a “priority hazardous substance” by the EU, a probable human carcinogen by the US EPA, and is suspected to be a human estradiol endocrine disrupter. Food is thought to be an important source of phthalate exposure to the general public, owing largely to its levels in fat-containing foods, particularly cheese, butter, and meat. Sources of DEHP in food include contamination by industrially synthesized DEHP (i.e., from packing materials, food-processing equipment, bioaccumulation of environmental contamination) and synthesis by bacteria (e.g., penicillium), mold, and algae (now a ubiquitous constituent in the world food supply). Despite the efforts to ban certain phthalate uses, DEHP levels of 0.2 to 2 mg/kg remain in cheese and butter analyzed in our laboratory.

SAmPLES AND ANALYSIS mETHoDSDEHP (0.17 mg/kg) was extracted from five 1.5-kg samples of Stilton Cheese and the extract purified with a sequence of flash (silica-Gel), size-exclusion, and C18 high-performance liquid chromatography steps with an overall yield of ~30% and DEHP purity of 92.5±2.7%. Most (96.6±0.8%) of the remaining carbon mass coeluted with DEHP (i.e. coelution blank) was attributed to natural components of the cheese of contemporary carbon composition. The remainder was comprised of D38-DEHP used as an internal standard, dibutylphthalate, and an unidentifiable compound.13C fractionations (δ13C, relative to VPDB) were determined for one Stilton Cheese extract, raw cheese, a petrochemically-derived DEHP standard (99.8±0.1% pure); pure D38-DEHP, and one purification blank (0.15±0.04 μg C) prepared by processing the 9.3 L of solvents in the same manner as samples. The remaining amount of the Stilton extract, equivalent to 92 μg carbon was converted to graphite after solvent evaporation, combustion and it’s 14C/13C ratio determined. In addition, two aliquots each, of the unlabeled DEHP and D38-DEHP internal standards; and two aliquots of the raw Stilton Cheese were analyzed.

RESULTSExtracted DEHP had an F14C of 0.2835±0.0042 after correction for combustion and graphitization blanks. Corresponding values of F14C for the labeled and unlabeled DEHP standards averaged 0.0012±0.0042 as expected for petrochemical origin. Fraction modern for the raw Stilton Cheese was 1.0413±0.0030.The F14C of DEHP was corrected for the sample purification and coelution blanks, and fractionation during purification, and then normalized to the F14C of the whole cheese to estimate the fraction of carbon attributed to contemporary carbon (fc) sources. The resulting value, 0.350±0.0067, suggests that the majority of the DEHP is of petrochemical origin.

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292

S04-P-093

14CH4, 14CO AND 14CO2 BY GAS CHROMATOGRAPHY AND CONTINUOUS-

FLOW AMS

MCINTYRE C., McnIcHol a., RobeRTS M., Von ReDen K., JenKInS W.

WHoI, WooDS Hole, UnITeD STaTeS

AbstractMethane, carbon monoxide and carbon dioxide are non-permanent, trace atmospheric gases that have major roles in the global carbon cycle, pollution and climate change. Carbon dioxide is the most important greenhouse gas (next to water) and the main agent of ocean acidification. Methane is a potent greenhouse gas with 25 times the warming potential of CO2 on a per-mole basis. Carbon monoxide is an indirect greenhouse gas that sequesters photochemically derived hydroxyl radicals that normally attenuate methane and ozone. Radiocarbon analysis is used to constrain the sources, apportionment and timescales of processes involving these gases and therefore new methods that facilitate its measurement are of interest.

Carbon dioxide is a readily condensable gas and it is relatively easy to prepare for 14C analysis. Cryogenic trapping and conversion to graphite is routinely performed in AMS laboratories. However, methane and CO are not condensable at liquid nitrogen temperatures, and their preparation is more elaborate. Typically, a vacuum line is arranged to sequentially cryogenically trap and oxidize these components. CO2 and contaminants such as N2O and volatile organic compounds (VOCs) are first trapped with liquid nitrogen. CO and CH4 are then sequentially catalytically oxidized to CO2 and trapped. CO can be selectively oxidized using a catalyst such as Sofnocat™ 423, whereas methane is typically oxidized in furnace over a platinized catalyst. With such an arrangement, three distinct fractions are prepared and analyzed by conventional graphite or gas accepting AMS systems. High precision radiocarbon values can be obtained on samples containing >100 µg of C.

At NOSAMS we have a novel gas-accepting microwave-plasma ion source coupled to an AMS system which is capable of making 14C measurements from a continuously flowing stream of CO2 gas. We have interfaced a unique gas chromatograph-combustion system to the ion source allowing us to make online compound specific radiocarbon measurements. The gas chromatograph has been optimized for gaseous samples and can separate CH4, CO and CO2 from permanent gases in 2 minutes. We verified the performance and accuracy of the system using landfill biogas which was a mixture of N2, CH4 and CO2. A single CH4 peak containing 20 ug of carbon yielded a precision of 5% and Fm value of 1.10. In order to increase the precision of measurements, we performed rapid sequential injections so that the data could be summed prior to the calculation of ratios. Over 20 minutes, ten injections of CH4 totaling 200 ug of carbon gave a precision of 1.5%. The 14C values fell within error of those obtained from conventional AMS analysis using graphite.

We will present details and the latest results from this work including system optimization, characterization and validation. With modification of the injector, we anticipate analyzing real- world seawater samples taken from oceanic ridge systems for CH4 and CO2 simultaneously.

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293

S04-P-094

MOLECULAR-SCALE RADIOCARBON DATING OF PYROGENIC CARBON

SMITTENBERG R.(1), GIeRGa M.(2), WIeDeMeIeR D.(3), ScHMIDT M.(3), DITTMaR T.(4), nIGGeMann J.(4), beRnaSconI S.(2), WacKeR l.(5), HaJDaS I.(5)

(1) Stockholm University, STocKHolM, SWeDen; (2) eTH Zurich, Geological Institute, ZURIcH, SWITZeRlanD; (3) University of Zurich, ZURIcH, SWITZeRlanD; (4) Max Planck Research Group for Marine Geochemistry, IcbM, University of oldenburg, olDenbURG, GeRManY; (5) eTH Zurich, laboratory of Ion beam Physics, ZURIcH, SWITZeRlanD

AbstractPyrogenic Carbon, also often referred to as ‘Black Carbon’ (BC), consists of graphitic-aromatic organic structures with sizes that range from a macroscopic (charcoal) to molecular scale. BC is known for its persistence in the environment and thus forms a significant part of the long-term global carbon cycle. For instance, the mass of BC can make up to 30% of total organic carbon in certain environments that experience regular wildfires. From both a carbon cycle and an archaeological perspective radiocarbon (14C) dating of BC is highly desirable, yet proven difficult on a molecular scale. One method to analyze the amount of BC and its degree of aromaticity - a proxy for charring temperature, consists of nitric acid digestion and subsequent analysis of the resulting benzenepolycarboxylic acids (BPCAs) by gas chromatography (GC) or liquid chromatography (HPLC) (Schneider et al. 2011). Previous attempts to perform 14C analysis of BPCAs using preparative GC proved doable but difficult (Ziolkowski et al. 2010). Here we present an HPLC-based method to separate and collect individual BPCAs for subsequent 14C dating on a MICADAS, equipped with a gas ion source. This new method opens up novel ways to determine the age of BC from various matrices like soils, sediments, dissolved organic matter, or archeological artifacts like pottery. Results obtained from oceanic dissolved organic matter are presented, together with ongoing work on BC from other matrices.

References1. Schneider MPW, Smittenberg RH, Dittmar T, Schmidt MWI (2011). Comparison of gas and liquid

chromatography for the determination of benzenepolycarboxylic acids as molecular tracers of black carbon. Org. Geochem 42, 275

2. Ziolkowski, LA, Druffel, ERM (2010). Aged black carbon identified in marine dissolved organic carbon. Geophys. Res. Lett. 37. doi:10.1029/2010GL043963

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294

S04-P-095

INVESTIGATION OF THE ORIGIN OF ENVIRONMENTAL COMPOUNDS FROM INDOOR AIR SAMPLES VIA ACCELERATOR MASS SPECTROMETRY.

KRETSCHMER W., ScHInDleR M., KRITZleR K., ScHaRf a., STUHl a.

erlangen University, eRlanGen, GeRManY

AbstractMany organic environmental compounds are potentially dangerous due to their allergic or carcinogen impact on humans. For an effective program to reduce their concentration in houses, their sources have to be detected. Our investigation is focussed on aldehyde compounds since their indoor concentration is relatively high and since they originate from biogenic or anthropogenic sources. Both types of sources can be distinguished by their different 14C content which can be measured via accelerator mass spectrometry (AMS).

For the collection and separation of these gaseous substances they have to be converted into liquid or solid phase by derivatization. This leads to the incorporation of up to six additional carbon atoms into the derivatized sample and hence to a reduced 14C content and to an increased uncertainty for the deduced 14C concentration. To reduce the number of additional carbon atoms and to optimize the efficiency, different derivatization compounds and methods have been tested with acet- and formaldehyde of known 14C content.

The 14C concentration of the calibration samples and from various indoor air samples have been determined by AMS, the corresponding results are discussed with regard to potential sources of aldehydes.

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295

S04-P-096

RADIOCARBON DATING OF INDIVIDUAL LIGNIN PHENOLS: A NEW APPROACH FOR ESTABLISHING CHRONOLOGY OF LATE qUATERNARY LAKE SEDIMENTS

HUANG Y.

brown University Providence, RHoDe ISlanD, UnITeD STaTeS

AbstractThe reliability of chronology is a prerequisite for meaningful paleoclimate reconstructions from sedimentary archives. The conventional approach of radiocarbon dating bulk organic carbon in lake sediments is often hampered by the old carbon effect, i.e., the assimilation of ancient dissolved inorganic carbon (DIC) derived from carbonate bedrocks or other sources. Therefore, radiocarbon dating is ideally performed on organic compounds derived from land plants that use atmospheric CO2 and rapidly delivered to sediments. We demonstrate that lignin phenols isolated from lake sediments using reversed phase high performance liquid chromatography (HPLC) can serve as effective 14C dating materials for establishing chronology during the late Quaternary. We developed a procedure to purify lignin phenols, building upon a published method. By isolating lignin from standard wood reference substances, we show that our method yields pure lignin phenols and consistent ages as the consensus ages and that our procedure does not introduce radiocarbon contamination. We further demonstrate that lignin phenol ages are compatible with varve counted and macrofossil dated sediment horizons in Steel Lake and Fayetteville Green Lake. Applying the new method to lake sediment cores from Lake Qinghai demonstrates that lignin phenol ages in Lake Qinghai are consistently younger than bulk total organic carbon (TOC) ages which are contaminated by old carbon effect. We also show that the age offset between lignin and bulk organic carbon differs at different Lake Qinghai sedimentary horizons, suggesting a variable hard water effect at different times and that a uniform age correction throughout the core is inappropriate.

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SESSION 13

RADIOCARBON AS A TRACER OF SOURCES, FLUXES AND TIME IN CONTINENTAL WATER

ConvenersP. Aggarwal (IAEA), A. Aureli (UNESCo), L. Bouchaou (mAR), J.L. michelot (FRA)

DescriptionThis session is dedicated to the applications of radiocarbon measurements in inorganic and organic, dissolved or particulate, compounds in continental water: surface water (lakes, rivers, estuaries) and groundwater. These applications include the tracing, quantification and modelling of natural and anthropogenic carbon fluxes in continental water, as well as the interpretation of radiocarbon measurements in terms of water dynamics in a reservoir (e.g. water “dating” and its implications on assessment and management of water resources).

Keywordssurface water, groundwater, tracing, dissolved and particular C fluxes, dating, water resources

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S13-P-098

A NEW 14C GROUNDWATER DATING APPROACH, APPLIED TO AN AqUIFER IN NORTH-WEST INDIA

WIESER M.(1), foHlMeISTeR J.(2), DeSHPanDe R.D.(3), HaJDaS I.(4), aeScHbacH-HeRTIG W.(1), GUPTa S.K.(3)

(1) Institute for environmental Physics, University of Heidelberg, HeIDelbeRG, GeRManY; (2) Heidelberg academy of Sciences, HeIDelbeRG, GeRManY; (3) Physical Research laboratory, aHMeDabaD, InDIa; (4) eTH Zurich, ZURIcH, SWITZeRlanD

Abstract14C is the only dating tracer to estimate groundwater ages ranging from several hundred years up to 40 ka. However, radiocarbon dating of dissolved inorganic carbon in groundwater implies some major complications due to open or closed system equilibration with soil CO2

and related isotope fractionation, as well as calcite dissolution during infiltration or later. Numerous models exist to estimate the resulting so-called hardwater effect using different physical perspectives. Some models constrain open or closed system situations, while others neglect crucial effects such as carbonate exchange with the aquifer matrix. These influences, when considered incorrectly, may lead to misinterpretation of older radiocarbon ages by several thousand years.

Here we introduce a new correction approach for the hardwater effect in groundwater, by transferring a model that has been developed for the study of cave dripwater (Fohlmeister et al., 2011). It is applied along with several established models to account for the hardwater effect to a multitracer palaeoclimate study of a groundwater aquifer in North-West India. The new model simulates a mixed open and closed system equilibration based on hydrogeochemical correlations. Advantages and shortcomings of the used models are compared and discussed. Furthermore, a quantitative method to consider matrix exchange for the new as well as for traditional models is applied. Finally, the resulting 14C ages are calibrated with the IntCal09 database to obtain calibrated ages also for the groundwater archive. Thus, the variable input curve of 14C in the atmosphere is considered, which is not the case in most hydrologic age records, misinterpreting old radiocarbon ages by up to 3000 years.

Applying this approach to the example from India, a groundwater age scale is established. Its age reaches from recent to late Pleistocene times, enabling palaeoclimatic reconstruction of the information contained in the archive.

ReferencesFohlmeister, J., et al. (2011), Modelling Carbon Isotopes of Carbonates in Cave Drip Water, Geochimica et Cosmochimica Acta, 75(18), 5219 -- 5228, doi:10.1016/j.gca.2011.06.023.

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298

S13-P-099

CARBON ISOTOPES IN DISSOLVED CARBON AS TRACERS OF PROCESSES IN THE KARST WATERS

SIRONIC A.(1), HoRVaTIncIc n.(1), KRaJcaR bRonIc I.(1), GUllIVeR P.(2)

(1) Rudjer biskovic Institute, ZaGReb, cRoaTIa; (2) natural environment Research council (neRc), Radiocarbon facility - environment, Scottish enterprise Technology

Park, eaST KIlbRIDe, UnITeD KInGDoM

AbstractDissolved inorganic carbon (DIC) in spring waters of karst region originates mainly from dissolution of carbonate minerals by CO2, generated from root respiration and decomposition of organic matter in the catchment area. In downstream flow the processes of photosynthesis and isotope exchange of carbon between atmospheric CO2 and DIC can play important role in the 14C and 13C composition of DIC.

We used the Plitvice Lakes, Croatia, as a case study area for carbon isotope distribution in karst springs, lakes and tributary waters. PlitviceLakesconsist of 16 karst lakes at different altitudes connected by waterfalls and streams and characterized by intense calcium carbonate precipitation in form of tufa and lake sediments. Measurements of 14C and δ13C of DIC have been made on 15 points downstream from springs including lakes and tributaries along a distance of approximately 12 km. In two biggest lakes, Kozjak and Prošće, the 14C and δ13C in DIC were measured along the water depth profile down to 10 and 30 m water depth. Additionally, a14C and δ13C of dissolved organic carbon (DOC) were measured at 4 points.

14C DIC values increase from 60 and 80 pMC in the two main springs to 85 pMC in the Korana River which issues from the lakes. δ13C values range from -12.5 ‰ in springs to -9 ‰ in Korana River. The largest change/increase of both values was noticed at the waterfalls area showing stronger influence of exchange process between DIC and atmospheric CO2. In the lake areas slight decrease or steady values of 14C and δ13C indicate that biological component/photosynthesis dominates. Higher 14C values of DIC and more negative values δ13C for two tributaries indicate higher influence of organic matter decomposition. 14C values in the water depth profile showed significant increase of 4 pMC from the surface to the bottom at the thermocline level and at the same time a decrease of δ13C. 14C values of DOC are 1 - 3 pMC higher than those of DIC and δ13C values of DOC range from -24 to -21‰ for the lakes and from -28 to -26‰ for tributaries.

The results of 14C and δ13C of DIC of Plitvice Lakes waters measured in 2011 were compared with the values measured 30 years ago (Srdoč et al, 1986). A decrease of between 3 and 9 pMC in the lakes and streams and less then 2 pMC in springs can be seen in the 2011 data in comparison with the 1981 data. The 2011 14C values are slightly higher (2 - 4 pMC) than those predicted by a prebomb-semiempiric model (Srdoč et al., 1986). No difference in δ13C values was observed in the last 30 years.

Acknowledgement: This research was supported by the Scientific Project with Plitvice Lakes National Park and the Ministry of Science, Education and Sports of the Republic of Croatia (Projects: 098-0982709-2741, 119-1191309-1305, 119-0362975-1226)

ReferencesSrdoč D, Krajcar Bronić I, Horvatinčić N, Obelić B. 1986. Radiocarbon 28:515-521.

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299

S13-P-100

RADIOCARBON DATING OF GROUNDWATER IN THE GRANITE FRACTURES IN ABUKUMA PROVINCE, NE JAPAN

TAKAHASHI H.A.(1), naKaMURa T.(2), TSUKaMoTo H.(1), KaZaHaYa K.(1), HanDa H.(1), HIRoTa a.(1)

(1) Geological Survey of Japan, aIST, TSUKUba, JaPan; (2) nagoya University, naGoYa, JaPan

AbstractThe present study discusses radiocarbon age of groundwater in the fractures of crystalline rock sampled from drilling boreholes in the Abukuma granitic province, Fukushima Prefecture, northeast Japan. The information of age is essential for an investigation of a long–term stability of groundwater. Three boreholes were drilled in the same rock body at two sites: Miharu and Shirasawa. To obtain groundwater in crystalline rock with minimal artificial interference, single and doublepacker methods were used for in–situ sampling immediately aftergranite fracturedetection. The groundwater sampling was carried out at the 7-11 depths of the respective boreholes. The bottoms of the boreholes were reached 140m, 230m and 306m from ground surface, respectively.

Radiocarbon concentration of dissolved inorganic carbon (DIC) was analyzed by AMS system (model 4130-AMS, HVEE) at the Center for Chronological Research, Nagoya University, Japan. The stable carbon isotopic values of DIC were measured by a continuous flow IR-MS with a Gas Chromatography system (Delta-V Advantage and GasBench II, Thermo Fisher Scientific Inc.). The alkalinity was measured by the acid titration method immediately after sampling to determine HCO3

− concentration.

Although stable carbon isotopic compositions were identical between the two boreholes at Miharu, differences were apparent between the two sites. Shirasawa represented the almost identical values with shallow groundwater ranged from -19.0 to -14.4 per-mil, which areequilibrated with CO2 derived from soil organic matter. Thus, groundwater has been scarcely affected by an external carbon input after the equilibrium of soil CO2 at the groundwater recharge.It can be considered that radiocarbon concentration indicate groundwater age at Shirasawa. The range of radiocarbon age is ca. 10,000-16,000 yr BP at the depth below 60m from ground surface. On the other hand, the vertically increasing trend of stable carbon isotope was found. The value is ca. -8 per-mil at the bottom of boreholes at Miharu. Chemical and isotopic compositions suggested that calcite dissolution with geogenic CO2 supply is occurred at Miharu. It is considered that carbon supplied to Miharu was 14C-free. The corrected radiocarbon concentration using the isotopic mass balance at Miharu indicated to be almost identical radiocarbon age with that at Shirasawa. Therefore, the present study represented that groundwater transportation through a fracture network of crystalline rock in natural condition was discovered to be significantly slow.

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S13-P-101

EFFECT OF RIVER AND SPRING WATER IN LIMESTONE AREA ON CARBON SOURCE AT LAKE BIWA, JAPAN

MIYATA Y.(1), aRaMaKI T.(2), MInaMI M.(1), oHTa T.(1), naKaMURa T.(1)

(1) center for chronological Research, nagoya University, naGoYa, JaPan; (2) center for environmental Measurement and analysis, national Institute for environmental Studies, TSUKUba, JaPan

AbstractWe measured carbon isotopes (13C and 14C) of river and spring water samples in limestone area to verify the effect them on the carbon source at Lake Biwa in Japan. It was because the Lake Biwa water may be affected by old carbon in the point of view of radiocarbon dating for lake water, sediment core, living animal & plants, organic components and archaeological reminds so far. Possibly major sources of lower 14C content in the lake water were the organic matter flowed into Lake Biwa, the re-resolution of organic matter in the upper sediment and retention of old carbon in peat layers formed by plants such as the ditch reeds that grow along the shore of the lake. On the other hand, higher sources were atmosphere and younger organic matter affected by bomb-14C.

River and spring water samples were collected in Ane River flowing into Lake Biwa. Dissolved inorganic carbon (DIC) in the samples was evolved as CO2 gas and collected cryogenically by purging with pure N2 gas in the vacuum system. Their carbon isotopic ratios were measured by gas source mass spectrometry and accelerator mass spectrometry.

The preliminary result of D14C value of the river water was about -250‰, sampled in the summer of 2009. In contrast, D14C values of DIC in water samples collected at four locations and from several depths in Lake Biwa were from +10 to +80‰, sampled from the spring of 1995 to the winter of 1996. The difference in apparent age offsets between the river and lake waters indicated that the river and spring waters were likely to be affected by dissolved old carbon originated from carbonate rocks such as Mt. Ibuki and Mt. Ryouzen around Lake Biwa and be one of source of lower 14C content (old carbon) in Biwa Lake water system. In this paper, we will discuss the budget of carbon isotopes of multiple end members at Lake Biwa to evaluate the contribution of the river and subsurface water of limestone districts to carbon source in the Lake Biwa water system.

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S13-P-102

INVESTIGATION OF GROUNDWATER RECHARGE WITH RADIOCARBON TRACER: CASE OF THE AqUIFER SYSTEMS OF CENTRAL TUNISIA

ZOUARI K.

enIS, SfaX, TUnISIa

AbstractIn semi-arid areas, delineation of the spatial distribution of old groundwater can provide an important contribution to the evaluation of long-term resource sustainability. Carbon 14, as a tool of dating past recharge conditions, can also be used to estimate groundwater flow direction and velocities, recharges rates as well as to improve flow models based on hydraulic data.

Nowadays, recharge of groundwater are not only related to infiltration of precipitation, but may also be induced by surface water conservation works on the basins. Several studies had proven that groundwater is often recharged by the leakage of dam storage reservoirs or by the diversions of stored water in the river. Today, isotopes of water molecule (2-H, 18-O, 3-H ) are the most commonly tracers used to identify and quantify groundwater recharge, if water masses fingerprints are well distinguished. Carbon 14 may also be used as a recharge tracer. In semi-arid areas, high activities, indicating that water equilibrated with the atmosphere has reached the aquifer, recorded in the vicinity of the recharge area, decrease along the flowpath by mixing processes and in situ decay process.

The present study concerns aquifer systems of the plain of Kairouan (Central Tunisia) where three great dams and several harvesting features have been built in order to regulate streamflow and runoff. This plain is submitted to a semi-arid climate and marked by high spatial and temporal variability. Carbon 14 measurements on dissolved inorganic carbon were used to provide information on the apparent ages of groundwater from various locations within the basins. Carbon 14 data (ca. 290 points) are extracted from the database of the Laboratory of Radio-Analyses and Environment (Sfax, Tunisia) where analyses are made according to the standard liquid scintillation protocol.

The spatial distribution of carbon 14 activities in deep groundwater shows that youngest waters (>50 pMC) are located north and northwestern the basin and at the mountain foothills. While, lowest activities (<30 pMC), observed south and southeastern and near sebkhas in the discharge area of aquifers, could be explained by longer residence time of groundwater. In shallow aquifers, high activities, 60 to 100 pMC, are recorded in the north and northwest zones, in the vicinity of great dams diversions and decrease along the groundwater flowpath. Carbon 14 data demonstrated the presence of a significant actual recharge of groundwater flowing in this area. Stable isotopic compositions of groundwater sampled at different location of the region are marked differently according to recharge modes, and thus provide excellent indicators of the mixing process. This tracing approach based on water molecule isotopes and carbon 14 tracing has been applied to delineate spatial influences of natural and artificial recharge, to calculate recharge rates and to attempt estimation of flow velocity insight groundwater.

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302

S13-P-103

RADIOCARBON DATING OF GROUNDWATER IN THE ARID ZONE OF ISRAEL

YECHIELI Y., bURG a.

Geological Survey of Israel, JeRUSaleM, ISRael

AbstractThis study deals with dating of groundwater in several aquifers in the Arava Valley of southern Israel, which is part of the Negev desert area. This arid area receives less than 50 mm of annual rain while the potential evaporation is very high (~3-4 meters), thus most of the current recharge to the shallow unconsolidated aquifers is coming from flash floods that flow from the mountains rising on both sides of the valley.

There are several aquifers in the Arava Valley and its surrounding, some of which are deep (deeper than 500 meters) and contain mainly fossil water, while others are much shallower (50-200 meters) and are supposed to contain historical to recent waters.

The deep and regional aquifers are the Upper Cretaceous Judea Group Aquifer, which is built of carbonate rocks (limestone, dolomite and marl) and the Lower Cretaceous Kurnub Group, which is built mainly of sandstones. The groundwaters in these deep aquifers have low 14C values (usually below 5 pMC) implying on old ages (apparent ages > 20,000 years). The old ages in the Kurnub aquifer are well correlated to those found in the correspondent aquifer in the Sahara desert. As expected, groundwaters in the regional aquifers do not contain tritium, except in one borehole which receives part of its water from lateral younger aquifer.

The shallow and more local aquifers are those of the Neogenic Hazeva Formation, which is built mainly of sandstone and clayey layers and the Quaternary Alluvium, which is built mainly of conglomerates and pebbles. Groundwater in these aquifers has relatively high 14C values (30-60 pMC) implying on younger ages and faster groundwater flow (recent recharge) than those in the deeper ones. This is also supported by the presence of tritium in most of the samples.

The large gaps between the 14C values that characterized the regional aquifers in the Arava Valley (e.g. the Kurnub aquifer versus the Alluvial aquifer) can be used to enhance our understanding of the underground flow regime and rates, particularly the complex connections between different aquifers.

It is interesting to note that groundwater dating may be possible (although not very accurately) even in this very arid environment where almost no vegetation occur and thus the processes that effect the carbon cycle are expected to be different and less pronounced than in temperate areas.

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S13-P-104

VARIATION IN Δ14C AND δ13C VALUES OF DISSOLVED HUMIC AND FULVIC ACIDS IN THE TOKACHI RIVER SYSTEM IN NORTHERN JAPAN

NAGAO S.(1), aRaMaKI T.(2), fUJITaKe n.(3), KoDaMa H.(4), TanaKa T.(5), ocHIaI S.(1), UcHIDa M.(2), SHIbaTa Y.(2), YaMaMoTo M.(1)

(1) low level Radioactivity laboratory, Institute of nature and environmental Technology, Kanazawa University, noMI, JaPan;

(2) national Institute for environmental Studies, Japan, TSUKUba, JaPan; (3) Graduate School of agricultural Science, Kobe University, Kobe, JaPan; (4) analytical Research center for experimental Science, Saga University, SaGa, JaPan; (5) aomori Research and Development center, Japan atomic energy Institute, MUTSU, JaPan

AbstractRadiocarbon is a useful tracer for distinguishing the relative importance of different aged dissolved organic carbon sources. The determinations have been performing for diooslved organic matter (DOM) in arctic rivers, US rivers, and small rivers in forested and wetland catchments. Δ14C values of DOM show a wide range from –158‰ to +364‰, indicating different turnover time, sources, etc. Dissolved humic substances (humic and fulvic acids) are ubiquitously abundant in aquatic environments and account for 40–60% of the DOM at aquatic systems. These substances influence carbon cycling and ecosystem dynamics. Therefore, it is important to understand characteristics and migration behavior of humic substances in river systems. This study reports a pair of Δ14C and δ13C values of dissolved humic and fulvic acids from the uper to the lower Tokachi River in Hokkaido Iskland, northern Japan. We will discuss the dynamics of humic substances in river basin from their carbon isotopic signatures.

Humic substances were isolated using XAD extraction method from the river waters at three sites in the upper (Tomuraushi site), the middle (Kyouei site) and the lower Tokachi River (Moiwa site) and one site in its tributary, Urikari River, on June in 2004 and 2005. Stable carbon isotopic ratio of a sample and the VPDB standard used for normalization were made by analyzing sub-samples of CO2 gas generated during graphite production using a triple collector mass spectrometer with a precision of ± 0.05‰. Radiocarbon was determined using accelerator mass spectrometry at the National Institute for Environmental Studiesand Japan Atomic Energy Agency. Radiocarbon values were reported as Δ14C corrected for sample δ13C with absolute error less than 10‰.

δ13C values range from –27.5 to –26.5‰ for the humic acid and –27.8 to –27.3‰ for the fulvic acid at the middle and lower Tokachi River and its tributary. On the other hand, the humic and fulvic acids from the upstream site have the δ13C values of -24.5 and -26.4‰, respectively. The Δ14C values of humic acids are –159‰ at the upper site, –71‰ at the middle site and –172‰ at the lower site. The fulvic acids has the Δ14C values of –55‰ at the upper site, +41‰ at the middle site and –40‰ at the lower site. The averaged Δ14C value is –148 ± 70‰ for the humic acid and –30 ± 65‰ for the fulvic acid. The difference is suggested that the residence time of fulvic acid in the watershed is shorter than the humic acid. The variation pattern of carbon isotopic ratios indicate that the pathway and sources of humic substances are different from each watershed in the Tokachi River.

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S13-P-105

DENSITY SEPARATION COUPLED WITH Δ14C AND δ13C TO TRACE DEPOSITION PROCESSES OF ORGANIC MATTER IN THE RHôNE RIVER DELTA (GULF OF LION, FRANCE)

TOUSSAINT F., TISnÉRaT- laboRDe n., caTHaloT c., RaboUIlle c.

laboratoire des sciences du climat et de l’environnement (lSce), GIf SUR YVeTTe, fRance

AbstractDespite its relatively modest surface area, coastal zones play a crucial role in the biogeochemical cycles of carbon because they receive large inputs of terrestrial organic matter (OM) by rivers, and appear as a large biogeochemical reactor. The terrestrial OM inputs can be buried or mineralized depending of physical and biological processes. Improved understanding of the fate of organic carbon and its distribution in River-dominated ocean margins is necessary to predict evolution of carbon in this system impacted by human disturbances and climate change.

The Rhône River is the main source of freshwater and terrigenous particles including organic carbon to the Mediterranean Sea. Previous studies based on bulk 14C analysis of surface sediment of Rhône delta have shown an aging of the OM from the River mouth to the continental shelf (Cathalot et al., 2008). The distribution of OM is stable along years (without flood) with a decreasing proportion of terrigenous OM with increasing distance of the river. Yet, the processes leading to this distribution are still being investigated: degradation, size or density sorting, petrogenic carbon accumulation…

In order to better understand the origin and the distribution of matter in condition without flood, we measure radiocarbon and δ13C in the different fractions of sample sediments obtained by density separation. Surface sediment of 3 sites located on a transect offshore (A, C and E) was sampled in April 2007. Bulk sediment was separated in 4 fractions with sodium polytungstate using the same methods that Wakeham et al. (2009) (<1.6, 1.6-2, 2-2.5 and >2.5 g cm-3). The main contribution fraction for organic carbon is the mesodensity: 1.6-2.5 g cm-3. After decarbonation, samples were combusted to transform the OM in CO2

and reduced to graphite. Then radiocarbon measurements were obtained by Artemis accelerator mass spectrometer at LMC14 and stable carbon isotopes measurements by EA-IRMS Mass Spectrometer (ThermoFinigan Delta+XP) at LSCE. δ13C of low density fraction (1.6-2 g.cm-3) is characterized by a terrestrial signature (-27.7 and -25.4‰) and the highest density fraction is between –24.1 and -24.8‰ which constitutes a mix of terrigenous and marine OM. Δ14C measurements show that the OM of sediment is differentially distributed among density fraction. For each station we observe an enrichment of Δ14C with increase of density which indicates younger particles in larger density fractions. Similarly to bulk analysis, each density fraction shows lower Δ14C on the gradient offshore.

References1. Cathalot, C. et al. (2008): Devenir et impact des apports fluviaux sur les marges continentales: importance

biogéochimique et environnementale du recyclage dans les sédiments du prodelta du Rhône. Thèse de l’UPMC

2. Wakeham, S. et al. (2009): Partitioning of organic matter in continental margin sediments among density fractions. Marine Chemistry, 115(3-4): 211-225

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S13-P-106

RADIOCARBON AND OTHER ENVIRONMENTAL ISOTOPES IN GROUNDWATER OF SITES FOR PLANNED NEW NUCLEAR POWER PLANT IN LITHUANIA

MAŽEIKA J.(1), MaRTMa T.(2), SKURaToVIČ Ž.(1), PeTRoŠIUS R.(1), JaKIMaVIČIŪTĖ-MaSelIenĖ V.(1)

(1) nature Research centre, VIlnIUS, lITHUanIa; (2) Tallinn University of Technology, TallInn, eSTonIa

AbstractGroundwater characterization is an important issue in the siting process of new nuclear power plants (NPP) and in decommissioning of the old NPPs. In this respect, a rather challenging situation is observed in Lithuania where the sites for the new Visaginas NPP and the industrial site of the shut down Ignalina NPP are in close neighborhood. The assessment of construction sites for the new Visaginas NPP, including groundwater characterization, took place in the last few years. For better understanding of groundwater system, the studies on carbon-14, tritium, stable isotopes of hydrogen, oxygen and carbon and helium content were fulfilled in the sites of the new NPP, i.e. the Western site and the Eastern Site.

The two aquifer systems of main concern at both sites have been characterizedwith different groundwater residence time and having slightly different stable isotope features and helium content. The first aquifer system consists of unconfined aquifer and semi-confined aquiferattributed to a depth up to 30 m. The second aquifer system is related to the Quaternary and Devonian succession at adepth up to 130–150 m.

Groundwater residence time in the first flow system based mainly on tritium data ranges from 10 to 60 years. Theseaquifers are the most important in safety assessment and may be particularly considered as a potential radionuclide transfer pathway in safety case. Groundwater residence time in the belowoccurring Quaternaryaquifers (50–90m depthinterval) is severalthousand years and in someintervalsup to 10,500 years. Stable isotopes are tracing groundwater recharge in colder climate cycle. The groundwater residence time in the Devonian aquifer system in some cases is even less than in the aquifers above. It can reach up to 4,500 or 8,200 years, depending on the geochemical model, but the value of 4,500 years is more presumptive. Such groundwater“age inversions” may be related to lower hydraulic conductivity of the Quaternary aquifers comparedwith the Devonianaquifers and to the presence of “preferential flow paths” in aquitards.

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S13-P-107

GROUNWATER RADIOCARBON DATING IN NORTH AFRICA (THE ALGERIAN EXPERIENCE SINCE MORE THAN 30 YEARS)

GUENDOUZ A.(1), MoUlla a.(2)

(1) blida University algeria, blIDa, alGeRIa; (2) nuclear Research centre, alGIeRS, alGeRIa

AbstractThe first analyses by the radiocarbon technique were initiated in North Africa (Algeria, Tunisia) by the UNESCO in 1972, in the framework of the ERESS project (Study of Water Resources in the North-western Sahara). Hence, thirty samples were collected by the IAEA over the whole of the North-western Saharan basin (over a surface area = 600,000 km2).

In Algeria, the Centre for Nuclear Research based in Algiers was already equipped with a laboratory for radiocarbon dating and isotope hydrology. It allowed performing carbon-14 analyses (at the beginning by gas proportional counting and later on and up to present time by liquid scintillation counting of benzene). Several studies have been conducted and implemented throughout the country both by the research team at the centre most of the time in association with the university (Mounts of Saida, Mounts of Tlemcen, Ain-Oussera plain, Chott Ech-Chergui, Mounts of Constantine, Hodna, Hoggar and most of them in the Saharan basin). A database of comprising more than 400 groundwater results in C-14 (the activity of which ranged between 0 and 120 pmc) and more than 150 others in C-13 (whose contents varied from -1 ‰ to-14 ‰ vs. PDB) was thus built.

The aim of this paper is to expose and discuss the radiocarbon results obtained since thirty years on different aquifers along a south to north axis beginning from the arid zone of the Saharan basin and going through the semi-arid area of the high plateaus up north to reach the coastal areas on the Mediterranean Sea.

The ages and the residence times which were determined from measured carbon-14 activities for the whole of the investigated aquifers varied between modern and several thousand of years. Groundwaters of the Saharan aquifer system enabled low resolution (±1000 a) characteristics of past climates to be determined, specifically palaeo-temperature, air masses’ origins, humid/arid transitions and rainfall intensities. Results from Saharan groundwaters (CI aquifer) indicate the predominance of a westerly Atlantic air flow during the Late Pleistocene. An intensification of the African monsoon during the Early Holocene is apparent from isotopically light groundwaters found especially over Libya.

The results indicate as well the non-renewability of many groundwater sources now being exploited across the Saharan basin and the high plateaus. Extreme events in the past, noted from such a groundwater record, may have lessons to teach and implications for an adaptation of water management policies with regard to future potential climate changes.

KeywordsRadiocarbon, Isotopes, Sahara, Groundwater, North-Africa; Palaeowaters.

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S13-P-108

CONTRIBUTION OF RADIOCARBON TO THE INVESTIGATION OF AN AqUIFER SYSTEM UNDER ARID CLIMATE: THE CASE OF THE SOUSS-MASSA BASIN (SOUTHERN MOROCCO)

BOUCHAOU L.(1), MIcHeloT J.l.(2), MaSSaUlT M.(2), beRaaoUZ e.H.(1)

(1) Ibnou Zohr University, faculty of Sciences, aGaDIR, MoRocco; (2) UMR «IDeS», cnRS - Université Paris-Sud, oRSaY, fRance

AbstractTo contribute to a sustainable water-resource management program for the Souss-Massa aquifer system, carbon-isotope measurements (A14C and δ13C) of dissolved inorganic carbon (DIC, mainly HCO3-) were used to provide information on the apparent residence time of groundwater. Three sampling campaigns were carried out within the area [2001 (n=15), 2005 (n=18) and 2008 (n=11)] for D14C and δ13C measurement. The analytical results showed very variable values depending on whether the samples were collected in the unconfined or confined parts of the Souss plain system or even from the geothermal system in the south of the basin. The δ13C values varied between –10.0‰ and –1.8‰ vs. V-PDB with an average of -8.7 ± 1.1‰. This range suggests that DIC in the system derived from: (i) dissolution of limestone/dolomite in the Atlas Mountains (δ13C =0‰) and (ii) conversion of soil CO2 (δ13C =-25‰) to dissolved bicarbonate. The 14C activities ranged from 1.3 (deep aquifer) to 93.3 pMC (Ifni spring in the High Atlas). The thermal water showed low D14C (6 pMC) and high δ13C (-5.7‰ V-PDB).

Consequently, we modeled the DIC isotopic variations as resulting from a mixing between (1) DIC originated from soil CO2 and conversion to HCO3- with modern D14C = 100 pMC and δ13C ~-15‰; and (2) DIC originated from dissolution of the Early Cambrian limestone and/or dolomite with D14C ~0 pMC and δ13C ~0‰. In order to calculate the apparent residence time of the groundwater, we used the 14C decay equation corrected for the mixing model. In spite of some divergence between the different used models, the water “ages” ranged from 0 to 20 ka. They ranged from 0 to 200 a in the recharge areas (close to the Atlas Mountains, mainly). A large part of the collected water samples showed a mixing between modern and old recharge (800 to 5000 a). The oldest groundwaters (10 to 20 ka) were found within the deep Turonian aquifer in the Souss plain and in the geothermal system in the bordering parts. However, the results suggest a contribution of relatively old groundwater (a few thousands of years) to the sampled springs and wells, particularly in the southern part of the basin and in the downstream area. The thermal water in the southern part of the Lakhssas Plateau, originating from a much more 2H and 18O depleted recharge, has a significant higher radiocarbon age of 10-15 ka BP, depending on the used model. This is consistent with what is known about the return to wetter conditions in Northern Africa during the last deglaciation period.

The data generated in this study provide the framework for a comprehensive management plan in which water exploitation should shift toward the eastern part of the basin, where current recharge occurs with young and high quality groundwater.

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308

S13-P-109

OLD APPARENT 14C AGES OF A PEAT CORE FROM RISHIRI ISLAND, NORTHERN JAPAN

Kono M.(1), MINAMI M.(1), TanIMIZU M.(2), aSaHaRa Y.(1), HoSono T.(3), naKaMURa T.(1)

(1) nagoya University, naGoYa, JaPan; (2) Japan agency for Marine-earth Science and Technology, KocHI, JaPan; (3) Kumamoto University, KUMaMoTo, JaPan

AbstractSediment cores collected from peat bog are useful to evaluate anthropogenic input history of heavy metals over the past hundreds or thousands years because organic matter in peat generally has low contents of heavy metals and is retentive of the polluted heavy metals. Depositional age of the peat sediment core is usually determined by 14C dating method because of high carbon contents. A peat core (40 cm length) collected in 2009 from Otadomari Pond in Rishiri Island, northern Japan, was used in this study to reveal impact of transboundary lead emission from the Eurasian continent to Japanese Islands and the Pacific Ocean over the past several hundred years. Here, sedimentation rate and age were determined by radiocarbon age from the peat samples and plant remains after conventional AAA-method treatment. In addition, 137Cs and 210Pb dating was performed to check the 14C ages.

The upper parts of the peat core at 0.0–10.5 cm depth show constant ages of 890 to 1230 BP. The uppermost layer does not show present 14C age, and 14C bomb-effect is not found in the upper part. 14C age at 11.0–17.0 cm depth fluctuates between 1650–3480 BP, and that at the deepest layer (40.0 cm depth) is 5050 BP. Based on the 14C age of the deepest part, the sedimentation rate is estimated at 0.07 mm/year on an average. Meanwhile, depositional ages of the peat core were also determined with 210Pb and 137Cs dating. Excess 210Pb is detected from the uppermost part to 16.5 cm depth, and this means that the upper part in the peat was deposited in the past one or two hundred years. Based on 210Pb decay, the sedimentation rate of the upper part is 0.9 mm/year, and is ten times larger than the rate estimated from 14C. In addition, 137Cs peak corresponding to 1960’s is detected at 3.5–4.0 cm depth. The sedimentation rate estimated from the timing of the drastic 137Cs rise is 0.8 mm/year, and is consistent with the rate from the excess 210Pb. These two sedimentation rates are almost consistent with those reported previously in this island (0.6 to 1.5 mm/year). Therefore, it is obvious that the 14C ages from the AAA-treated peats are 1000 to 3500 years older than the 210Pb and 137Cs ages, meaning that the 14C ages do not show actual depositional ages.This age difference is possibly caused by inflow of old 14C-age soil from the surrounding area of the pond or by addition of old 14C-age component derived from diagenetic origin in the downside peat. In the presentation, we will thoroughly discuss the causes of the large age difference and depositional environment based on data for 14C ages of plant remains in the peat, suspended organic matter in the pond, carbon in HCl/NaOH-leachate fractions, and CHN composition and 13C isotope in the peat.

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S13-P-110

A PRELIMINARY STUDY ON THE TIME SCALE OF GROUNDWATER FLOW IN THE NAKANO-SHIMA ISLAND, OKI-DOZEN, JAPAN

KUSANO Y.(1), ToKUnaGa T.(1), aSaI K.(2), aSaI K.(2), MoRIKaWa n.(3), YaSUHaRa M.(3), TaKaHaSHI H.a.(3)

(1) The University of Tokyo, KaSHIWa cITY, JaPan; (2) chikyu Kagaku Kenkyusho Inc., naGoYa cITY, JaPan; (3) Geological Survey of Japan, TSUKUba cITY, JaPan

AbstractResidence time of groundwater is essential information to discuss groundwater flow system in the coastal area. In this paper, end-member waters with different residence times are clarified, and the formation of groundwater and hot spring water in the Nakano-shima Island, Japan, are discussed.

The Nakano-shima Island was formed by volcanic activities which erupted alkali basalt lava c.a. 6Ma (Tiba et al., 2000). Thickness of the lava is about 300 to 400m. The lava overlies the sedimentary rocks of which deposition ages were Lower to Middle Miocene (Tiba et al., 2000).

Groundwater samples were collected from springs, water-supply wells (screen depth: GL-10 to -100m) and a hot spring well (screen depth: GL-560 to -870m). All samples were analyzed for CFCs, 3H, SF6, and stable isotopes of oxygen and hydrogen. Samples from four water-supply wells and the hot spring were analyzed for 14C and isotopic ratios of He.

Stable isotopic ratios of oxygen and hydrogen of all samples were plotted on or near the meteoric water line. The values of the hot spring were lower than other samples. 14C value of the hot spring was 17pMC, and CFCs and 3H concentrations of the water were generally lower than those of the water samples taken from other wells. The 14C concentrations of two water-supply wells containing lower CFCs and 3H ranged from 57 to 77pMC, while that from another water-supply well containing higher CFCs and 3H was 96pMC. The noble gas analysis (3He/4He and 4He/20Ne) suggested that mantle-derived fluid isadded to groundwater, and hence, pMC values of groundwater should be higher than those measured.

Groundwater containing lower CFCs and 3H and the hot spring water are considered to be the mixture of young groundwater containing CFCs and 3H and old groundwater free of CFCs and 3H. Lower δD and δ18O values of the hot spring suggest that the hot spring water might be recharged in colder climate, and this result is consistent with lower pMC value of the hot spring water. It is considered that fresh groundwater recharged during the last glacial period still remains in the aquifers. Further consideration is needed for understanding the formation process of such long-term groundwater flow system in the island, with the focus on the effect of sea level changes and the paleo-topography of the island and its surroundings.

ReferencesTiba, T., Kaneko, N., and Kano, K.. Geology of Urago district. Geological survey of Japan, 74p, 2000.

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S13-P-111

CARBON CYCLE AND ORGANIC RADIOCARBON RESERVOIR EFFECT IN A MEROMICTIC CRATER LAKE (LAC PAVIN, PUY-DE-DôME, FRANCE)

ALBERIC P.(1), JeZeQUel D.(2), beRGonZInI l.(3), cHaPRon e.(1), VIollIeR e.(2), MaSSaUlT M.(3), MIcHaRD G.(2)

(1) Univ. orléans, oRlÉanS, fRance; (2) Univ. Paris 7 & IPGP, PaRIS, fRance; (3) Univ. Paris Sud, oRSaY, fRance

AbstractA data set describing the contemporary distribution of dissolved and particulate radiocarbon pools into the water column of the meromictic crater lake Pavin is presented. The objective is to address value of the present day reservoir effect associated to organic 14C dates of bulk sediment. Possible seasonal or secular variation of the reservoir effect is discussed according to different past limnological conditions.

Several C compartments were analysed: dissolved inorganic (DIC) and organic C (DOC), plankton, suspended particulate organic C (POCsusp), sinking POC (POCsink), and bottom sediment organic C (SOC). Laminated buried sediment samples (mainly organic rich diatom deposits) and terrestrial vegetal macrorests picked in several cores were used to evaluate the variation of the reservoir effect with time, since the formation of the lake (7000 y calBP).

Δ14C values of DIC ranged from -750‰ in the monimolimnion (from chemocline at 60 m depth to bottom at 92 m depth) to atmospheric values in lake surface waters and in the spring inlet waters. Monimolimnion DIC Δ14C profiles can be explained at quasi steady state conditions by eddy diffusion in the water column of different C sources, i.e. from the bottom sediment and from depth stepped several inputs of mineral or underground radiocarbon free waters, especially just below the chemocline at 68 m depth. Although primary production in the surface waters may potentially sustain on variable DIC radiocarbon composition due to seasonal variations of the mixing of the water column through the first 60 m (mixolimnion) and atmospheric inputs, production export to the bottom seems to settle with a rather constant radiocarbon composition at the time scale of several years. A range of Δ14C values comprised between -200 and -300‰ was found for superficial POCsusp, POCsink, SOC and DOC. This rather uniform radiocarbon offset of the exported organic production from the surface waters to the bottom leads to a present day reservoir effect of about 2000 y. Δ14C values of POCsusp below 60 m depth (< -400‰) may reflect deep bacterial production.

Sediment layers sampled only a few tens cm deeper in the short cores may give ages older. In this case, differences between Δ14C values of bulk sediment and terrestrial plant remains sampled in the same layers ranged between -400 to -500‰. However layers with a Δ14C difference back to -250‰ (similar to present day reservoir effect) were observed around 1300 y calBP. Moreover almost zero reservoir effect was inferred from the sediment layers deposited just above the volcanic bedrock at the early flooding time of the crater.

At the current stage of the study which has almost focussed on the present day cycling of C into the water column, a more extensive effort of radiocarbon dating of the laminated sediment sequence would be necessary to avoid repeating past misinterpretation of bulk sediment 14C data.

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S13-P-112

DISCUSSION AROUND OUR NEW CO2 EXTRACTION LINE FROM DISSOLVED INORGANIC CARBON (DIC) AT LMC14 ARTEMIS LABORATORY IN SACLAY, FRANCE

DUMOULIN J.P., SoUPRaYen c., baVaY D., caffY I., coMbY c., DelQUÉ-KolIc e., HaIn S., MoReaU c., SeTTI V., VIncenT J.

lMc14, SaclaY, fRance

AbstractSince 2003, the LMC14, installed in Saclay, France, prepares and measures 14C samples for researchers in the fields of quaternary geology, environmental sciences and archaeology. While manual and automatic preparation lines have been developed for carbonated and organic samples, a water extraction line for dissolved inorganic carbon (DIC) was built few months ago. This new equipment will be able to handle both seawater and freshwater and will be a useful tool for researchers working with the LMC14. The analysis of the seawater is helpful to study carbon cycle and dynamics of ocean circulation. For the groundwater and rivers studies, 14C helps to build models on the transit and the residence time of water.

In this presentation, we will detail the geometry of this manual line and its functioning. 14C results obtained with this new line will be presented: background samples made from IAEA-C1 carbonate and a bicarbonate sample (NaHCO3/Acros). They will be compared to classical carbonate extractions from these same samples (Tisnérat-Laborde et al., 2001). We will also compare the advantages and inconveniences to work in a dynamic way (under He flux) or in a static way (cryogenical displacement of the CO2). Furthermore, two methodological approaches are commonly used: some labs used to poison water samples with HgCl2 whereas others use to measure DIC on non-poisoned but 4°C-refrigerated water. We will discuss results we obtained in both of the configurations.

ReferencesTisnérat-Laborde N.,Poupeau J.J., Tannau J.F. and Paterne M. (2001) Development of a semi-automated system for routine preparation of carbonate samples. Radiocarbon, 43 (2A), 299-304

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312

S13-P-113

NEW DEVELOPMENTS OF GROUNDWATER DATING WITH 14C ON DISSOLVED ORGANIC CARBON

MOULE Y., MaSSaUlT M., MIcHeloT J.l.

Université Paris Sud, cnRS, oRSaY, fRance

AbstractIn hydrogeology, the carbon-14 dating method is widely used to determine groundwater residence times in aquifers, from measurements performed on dissolved mineral compounds of carbon (Total Dissolved Inorganic Carbon, TDIC).

The radioactive-decay signal, from which residence time may be computed, is very often disturbed by different processes that lead to contamination by “dead” carbon (dissolution of rock matrix carbonates, oxidation of organic matter…). To take into account these disturbing effects, different correction models can be applied for determining water “ages”. Most of theses models are based on 13C/14C balances to quantify the contribution to TDIC from different sources, according to the aquifer characteristics. Thus, a perfect knowledge of aquifer parameters is required to minimize 14C dating uncertainties.

Another dating method of groundwater is based on the 14C contents of some of the dissolved organic compounds of carbon: the most condensed molecules of DOC (Dissolved Organic Carbon), which come mainly from soils during recharge. Previous studies compared the 14C groundwater “ages” determined by using TDIC and DOC methods and showed that the results were sometimes significantly different. Some of these studies suggested that DOC dating method could be the most accurate. However, the major problem encountered when using this method is related to the large size of the needed water samples, because the resins that were used to concentrate DOC have weak efficiency rates.

To solve this sampling problem, we propose to use other techniques. In particular, the technique of tangential-flow ultrafiltration, which was already applied to analyse DOC in marine water, seems well adapted for separating and concentrating the heaviest molecules (humic substances), which constitute a major fraction of DOC in groundwater.

Some preliminary results are shown, concerning the development of an experimental protocol adapted for groundwater dating by the 14C /DOC method with a sample size as small as possible (about 1 litre), and its first application to natural groundwater samples.

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313

S13-P-114

RADIOCARBON RESERVOIR AGES AS FRESHWATER-BRINE MONITORS IN LAKE LISAN - DEAD SEA SYSTEM

STEIN M.(1), GolDSTeIn S.(2), laZaR b.(3)

(1) Geological Survey of Israel, JeRUSaleM, ISRael; (2) lamont-Doherty earth observatory, columbia University, neW YoRK, UnITeD STaTeS; (3) Institute of earth Sciences, The Hebrew University of Jerusalem, Givat Ram, JeRUSaleM, ISRael

AbstractA continuous and high-resolution record of the radiocarbon reservoir age (=RA) is recovered from the primary aragonites that were deposited at the last glacial Lake Lisan. The RA is calculated as the difference between the measured (“apparent”) radiocarbon age in the aragonite and the atmospheric radiocarbon age at any particular calendar (aragonite U-Th) age. The RA shows temporal decrease during the time intervals of ~30 to 17.4 ka. This behavior is attributed to continuous input of high HCO3

- runoff freshwater with relatively high pMC to the Ca-chloride brine in the lakes having much lower HCO3

- and pMC. The mixing of these two water types resulted in precipitation of aragonite with pMC values higher than those of the original lake’s brine. The continuous long-term input of fresh runoff water is reflected by continuous increase of the lake’s pMC and decrease of the RA. The runoff-brine mixture in Lake Lisan is also reflected by the Sr/Ca ratios that are positively correlated with the RA. Thus, we can use the independently analyzed Sr/Ca ratios in the aragonite to calculate the RA and corrected radiocarbon ages of the Lisan aragonites. The RA corrected radiocarbon ages of the Lisan aragonites display good agreement with corals and Cariaco basin data confirming the validity of the Lisan aragonites as reliable atmospheric radiocarbon chronometer.

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314

S13-P-115

ASSESSING GROUNDWATER RECHARGE IN A COMPLEX MULTI-LAYER AqUIFER IN TRANSITORY CONDITIONS

BAUDRON P.(1), baRbecoT f.(2), GaRcIa-aRoSTeGUI J.l.(3), MaRTIneZ-VIcenTe D.(4), noReT a.(2), TRaVI Y.(5), leDUc c.(6)

(1) Institut de Recherche pour le Développement, eSPInaRDo, MURcIa, SPaIn; (2) Paris Sud University, UMR IDeS 8148, oRSaY, fRance; (3) Geological Survey of Spain (IGMe), MURcIa, SPaIn; (4) fundacion Instituto euromediterraneo del agua, MURcIa, SPaIn; (5) avignon University, UMR eMMaH 1114, aVIGnon, fRance; (6) Institut de Recherche pour le Développement, MonTPellIeR, fRance

AbstractUnder semi-arid climate, intense agricultural activity can strongly influence groundwater on both qualitative and quantitative aspects. When the studied groundwater systems present clear transitory conditions, with a hard to define pre-anthropogenic situation (long-term groundwater abstraction, overexploitation, irrigation return-flow, mixing through boreholes), one of the main difficulties that are faced for the interpretation of radiocarbon time tracers is the difficulty to assess a reliable referential. Combining environmental tracers (14C, 13C, 2H, 18O, 3H) and high-resolution temperature logging, a methodology is proposed, and applied to a type area for transitory conditions: the Campo de Cartagena multi-layer aquifer in South Eastern Spain. Despite of the hamper of a complex background, the combination of both techniques allows a reliable interpretation of the geochemistry and provides a better understanding of the groundwater flow pattern. Temperature loggings help to define inside-well mixing processes for both abandoned and active boreholes. These mixing processes are confirmed by geochemical evidences, together with a clue for the determination of the local or regional scale of these contaminations. Temperature loggings also increase the reliability of geochemical and hydrodynamic interpretation by accurately identifying the origin of the samples. Radiocarbon time tracers and other environmental tracers are then optimised and provide specific clues on recharge processes, highlighting the main features of the pre-anthropization recharge regime and allowing a quantification of groundwater recharge to the different aquifer layers.

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315

SESSION 16

ANTHROPOGENIC IMPACTS

ConvenersS. Ledizes (FRA), A. Pazdur (PoL)

DescriptionAnthropogenic impacts on the environment are a major cause of recent and significant changes in isotopic composition of carbon in modern atmosphere and biosphere. For example, human activities are changing the isotopic composition of atmospheric carbon mainly from burning fossil fuels, which increase the amount of stable carbon dioxide, and nuclear weapon tests, which are sources of additional 14C. Increased concentrations of stable and radioactive CO2 could also have a significant impact on the change of specific carbon activity in plants, even without climate change. Scientific characterization based on both field studies and laboratory experiments to measure 14C activity in terrestrial environmental samples and/or modeling approaches is crucial to understanding how such anthropogenic changes impact ecosystems. This session includes a wide range of CO2 and radiocarbon measurement techniques and/or modelling approaches used to determine the increased 14C activity caused by humans. Of particular interest are presentations that focus on the impacts of human activities resulting from fossil fuel and nuclear facilities - including reprocessing plants - that contribute to the increased 14C activities in atmosphere and biosphere. This theme, more commonly discussed in the context of plant physiology, agro-meteorology, soil sciences, hydrology and climatology, will be discussed with experts on isotope studies and 14C modelling (radio-ecology, model calibration and validation) allowing different scientific communities to exchange knowledge, data acquisition and/or modelling approaches.

Keywords14C activity, environment, human impact, modelling, data acquisition methods

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316

S16-P-116

14C SIGNATURE OF ATMOSPHERIC AEROSOL CLOSE TO A NUCLEAR POWER PLANT

PERRON N., GeoRGIaDoU e., GenbeRG J., STenSTRÖM K.

lund University, lUnD, SWeDen

AbstractQuantifying the contributions of fossil and non-fossil sources of atmospheric carbonaceous aerosol using radiocarbon has now become usual in aerosol source apportionment studies [1]. This method relies on the existence of two sources of 14C only: natural, cosmogenically-produced 14C, which is continuously produced in the upper atmosphere and then assimilated by vegetation as CO2; and artificial “bomb-14C”, which peaked in 1963 due to the 1950s-60´s atmospheric nuclear tests and has led up to now to global excess 14C concentrations, compared to pre-bomb times.

However, other anthropogenic sources of radiocarbon also exist. For example, some research laboratories and industries produce or use 14C for labelling purposes, whereas the nuclear power industry is known to release atmospheric 14C as CO2 [2]. Very little though is known about their impact on the 14C content of particulate matter, even if warnings start to appear in the literature [3,4].

We investigate in this study the potential release of 14C-enriched aerosols by the nuclear power plant of Ringhals, located on the Swedish western coast. 14C measurements of particulate matter sampled close to the plant and at a background station will be presented and compared with results from parallel CO2 samplings at those two locations.

References[1] Szidat (2009) Science 323, 470.[2] Molnár et al. (2007) Radiocarbon 49, 1031.[3] Levin et al. (2008) Sci Total Environ 391, 211.[4] Bench et al. (2007) J Geophys Res 112, D10205.

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317

S16-P-117

14CO2 DISPERSION AROUND TWO PWR NUCLEAR POWER PLANTS IN BRAZIL

MELAZO DIAS C.(1), STenSTRÖM K.(2), VenTURa SanToS R.(3), GoMeS nÍcolI I.(1), SKoG G.(4), eKSTRÖM P.(2)

(1) national commission of nuclear energy (cneM), bRaSÍlIa, bRaZIl; (2) Department of Physics, Division of nuclear Physics, lund University, lUnD, SWeDen; (3) Institute of Geology, brasilia University, bRaSIlIa, bRaZIl; (4) Radiocarbon Dating laboratory, Geobiosphere Science centre, lUnD, SWeDen; (5) national commission of nuclear energy (cnen), GoIanIa, bRaZIl

AbstractAtmospheric air samples were taken within 3 km from power plants encompassing five different distances and wind directions. Samples were taken between 2002 and 2005 aiming to evaluate the environmental 14C enrichment due to the operation of Brazilian nuclear power plants. The sampling system consisted of a pump connected to a trapping column filled with a 3 M NaOH solution. The trapped CO2 was analyzed for 14C by using a single stage accelerator mass spectrometry (SSAMS).

All sampling sites revealed measurable 14C excess values. The maximum excesses were of 15 and 14 mBq/m3 for sampling sites placed at NE of the power plants, which is the main wind direction in the area. The mean excesses values were 12 mBq/m3 to the NE direction, 8 mBq/m3 to the E, 10 mBq/m3 to the N, 8 mBq/m3 to the WNW and 7 mBq/m3 to the W direction (increasing distances from NE to W). Compared to other LWR’s data, these means values are significantly higher than the average worldwide reported value of 3 mBq/m3. Available data indicate that the observed values are not related to 14C emission by the power plants vent stack. Other factors, such as topography, seem to have an important role because it affects wind dispersion thus favoring 14C accumulation in the sampled area. Moreover, the high elevations around the power plants enhance the chances to measure high values of 14C since the plume can be intercepted before it is drawn to the ground. Modeling of the plume has shown that its dispersion does not follow a Gaussian model and that agreement between atmospheric CO2 and vegetation 14C activities occurs only for sampling sites placed at NE of the power plants.

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318

S16-P-118

FOSSIL AND BIOGENIC CO2 FROM WASTE INCINERATION BASED ON A YEARLONG RADIOCARBON STUDY

MOHN J.(1), SZIDaT S.(2)(3), ZeYeR K.(1), eMMeneGGeR l.(1)

(1) laboratory for air Pollution & environmental Technology, empa, DUebenDoRf, SWITZeRlanD; (2) Department of chemistry and biochemistry, University of bern, beRn, SWITZeRlanD; (3) oeschger centre for climate change Research, University of bern, beRn, SWITZeRlanD

AbstractSolid waste or solid recovered fuels (SRF) contain resources that can be recovered as material or energy. Although re-use and recycling should be favored as they lead to reduced energy use and less environmental impact, combustion of mixed or non-recyclable material streams in efficient waste-to-energy (WTE) plants is part of an integrated waste management system. While fossil CO2 emissions are non-renewable and have to be included in the national greenhouse gas inventory, heat and electricity production from the incineration of biogenic waste is considered as a renewable energy source. As a consequence of these regulations and their financial implications, there is a growing interest in analytical techniques for the determination of the share of biogenic and fossil carbon in SRF. The 14C measurement of flue gas from WTE plants is a powerful method for the determination of the fossil fraction of the incinerated SRF [1]. We describe the first long-term implementation of the radiocarbon (14C) method to study the share of biogenic and fossil (%Fos C) carbon in combustion CO2. At five Swiss WTE plants, 24 three-week measurement campaigns were performed over one year. 14C was analyzed in temporally averaged bag samples by the accelerator mass spectrometer (AMS) MICADAS. The samples were introduced into the system as CO2 using the direct gas inlet and a gas-capable ion source [2, 3]. Significant differences between the plants were observed in the share of fossil CO2. Based on our dataset, an average of 48 ± 4 %Fos C was determined for waste incineration in Switzerland. No clear annual trend was observed for four of the monitored incinerators, with fluctuations within the uncertainty of the analytical results. One incinerator, however, shows considerable variations in the share of fossil and biogenic CO2, which are likely due to the storage of waste with high biogenic carbon that is incinerated during winter to increase the plant’s heat production. Significant and persistent differences in %Fos C throughout the year between the plants are consistent with the waste composition of the respective WTE incinerators.

References[1] J. Mohn et al., Bioresour. Technol. 99, 6471-6479 (2008).[2] M. Ruff et al., Radiocarbon 49, 307-314 (2007).[3] M. Ruff et al., Nucl. Instrum. Methods Phys. Res. B268, 790-794 (2010).

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319

S16-P-119

LOCAL SUESS EFFECT IN THE GäVLE AREA (SWEDEN)

SANTOS-AREVALO F.J.(1), GoMeZ-MaRTIneZ I.(1), HolM e.(2), GaRcIa-TenoRIo R.(3)

(1) centro nacional de aceleradores (Universidad de Sevilla, cSIc, Junta de andalucia), SeVIlla, SPaIn; (2) norwegian Radiation Protection authority, oSTeRaS, noRWaY; (3) Dpto. de fisica aplicada II, eTSa, Universidad de Sevilla, SeVIlla, SPaIn

AbstractTree-ring samples from Norway Spruce (Picea abies) have been used to study local Suess effect in the area of Gävle, Sweden, 61.0°N, 17.0°E. The fallout of 14C from nuclear tests during 1950s and 1960s has superimposed with an increased use of fossil fuels by industries and also locally by transports and heating of domestic buildings. Also the nuclear accident in Chernobyl in 1986 had a contribution in the area, although the 14C/12C ratio in this case is unclear since it was a graphite moderated reactor and the graphite was burning. Samples have been collected in 2011 with a hand drill in five different specimens in a nearby area. Year-resolution samples have been prepared and analyzed by AMS at the Centro Nacional de Aceleradores (CNA), Seville, Spain.

Wood samples results are compared with a peat core sampled in 2008 in the same area, which was previously dated using the 210Pb method, giving a growth rate of 0.15 mm/yr. The top 21 cm have been analyzed for radiocarbon content, using 0.5 cm samples, thus getting information about the last 140 years with resolution better than 4 years. Results show a clear depletion of F14C levels in the area.

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320

S16-P-120

FOSSIL FUEL-DERIVED CO2 CONTRIBUTION TO CITY ATMOSPHERE BY 14CO2 OBSERVATION IN GUANGZHOU, SOUTH CHINA

DING P.(1), SHen c.(1), YI W.(1), WanG n.(2), DInG X.(3), fU D.(3), lIU K.(3)

(1) Guangzhou Institute of Geochemistry,chinese academy of Sciences, GUanGZHoU, cHIna; (2) Department of earth Science, Hongkong University, HonGKonG, cHIna; (3) State Key laboratory of nuclear physics and Technology, Peking University, beIJInG, cHIna

AbstractAtmospheric 14CO2 observations are used to quantify fossil fuel-derived CO2 concentrations at a regional polluted site. In order to evaluate the fossil fuel-derived CO2 amount in Guangzhou, South China, about one year long atmospheric 14CO2 and as well the CO2 concentration observations were carried out at every week in a typical residential district from October, 2010 to December, 2011. The mean annual atmospheric 14CO2 Δ14C value is -16‰, and the average amount of fossil fuel-derived CO2 contributed to Guangzhou atmosphere was about 11 ppm calculated following the method proposed by Levinet al (2003). Although the city atmospheric 14CO2 Δ14C value fluctuated significantly from 30‰ to -80‰ which mainly appeared at haze weather, the monthly mean atmospheric 14CO2 Δ14C values range from 0‰ to -40‰. Apparently seasonal changes of atmospheric 14CO2 Δ14C value have been also observed. The relative high Δ14C values about -8‰ appeared in summer and autumn, while in spring and winter, they decline to about -35‰. Correspondingly, the amounts of fossil fuel-derived CO2 were about 8 ppm and 18 ppm, respectively. During Spring Festival of 2011, the atmospheric 14CO2 Δ14C value increase to 5‰, and the fossil fuel-derived CO2 contribution to the city atmosphere declined to about 3 ppm. The sharp decrease of the contribution was linked to the 90% reduce of the vehicle use and also the close up of most factories around the city. The observed atmospheric CO2 concentration in monthly mean value fluctuated between 550 ppm to 470 ppm, displaying a reverse seasonal change with that of Δ14C values. However, when the haze weather occurred, the atmospheric CO2 concentration increased to more than 600 ppm rapidly due to the lower atmosphere diffusion rate.

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321

S16-P-121

CARBON 14 INPUTS FROM THE RHôNE RIVER TO THE WESTERN MEDITERRANEAN SEA DURING FALL 2010 AND SPRING 2011

FONTUGNE M.(1), Jean-baPTISTe P.(1), foURRÉ e.(1), benTaleb I.(2), DeZIleaU l.(3), cHaRMaSSon S.(4), anTonellI c.(5), MaRanG l.(6), SIcleT f.(6)

(1) cea, GIf/YVeTTe, fRance; (2) ISeM University of Montpellier, MonTPellIeR, fRance; (3) laboratoire Géeoscience University of Montpellier, MonTPellIeR, fRance; (4) IRSn- DeI/SeSURe/leRc base IfReMeR, la SeYne/MeR, fRance; (5) IRSn- DeI/SeSURe/leRc centre etude cadarache, ST PaUl leZ DURance, fRance; (6) eDf R& D Dept. lnHe, cHaToU, fRance

AbstractRadiocarbon in the Rhône River are linked to the strong presence of the civil and military nuclear industry. Rhône River discharge in the Mediterranean Sea may therefore be a potentially significant source of carbon 14 to coastal areas. During fall 2010 and spring 2011, 14C activities were measured in suspended organic matter, in dissolved inorganic carbon (DIC) of the Rhône River, coastal lagoon brackish waters and Mediterranean Sea waters. The distribution of this radionuclide along the Mediterranean coast from Cassis (43.2°N; 5.55°E) to St Cyprien (42.6°N; 3°E) is presented.

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322

S16-P-122

VARIATIONS OF ANTHROPOGENIC CO2 IN SENEGAL URBAN AREA DEDUCED BY RADIOCARBON CONCENTRATION IN TREE LEAVES

NDEYE M.

Ifan, DaKaR, SeneGal

AbstractRadiocarbon in atmospheric CO2 was measured over Senegal urban area by using tree leaves collected by botanist from 1900 to 2003 during several excavations. The delta 14C of atmospheric CO2 over this region remain almost constant from 1900 to 1952 and represent the pre-bomb component, from 1952 to 1963 the testing and use of nuclear devices produced enough 14C to cause atmospheric concentrations of CO2 to almost double 180.87‰ (E.Drufell and Hans Suess).The delta 14C of atmospheric decreased from 767+/- 4‰ in 1964 to 86+/-5‰ in 2003 consistent with the global exponential decreasing trend. Radiocarbon concentration in urban area is naturally lower due to the contribution of the carbon dioxide emission from fossil fuel combustion. The phenomena is known by Suess effect it express a contamination of clean air with non radioactive carbon. That amount of carbon can be evaluated by comparing to those from areas of clean air. The method of calculation deduced from in simple mathematical model developed by Levin et al (2003) suggest that the use of leaves of trees to obtain secular variations of 14C concentrations of atmospheric CO2 can be useful and efficient for environmental monitoring and modeling of the carbon distribution in local scale.

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323

S16-P-123

RADIOCARBON FOR FUELS, PACKAGING AND FOOD qUALITY CONTROL

PAZDUR A., PaWlYTa J., PIoTRoWSKa n., SenSUla b., TUDYKa K.

Institute of Physics, GaDaM centre of excellence, Silesian University of Technology, Krzywoustego 2, GlIWIce, PolanD

AbstractA growing demand for biocomponents control in solid, liquid and gas biofuels and lubricants can be expected in the next few years. In Poland and other EU countries the introduction of the bio-component is the most common way to fulfil the obligation to reduce CO2 emissions to the atmosphere. According to the European Union strategy, biomass is considered neutral in terms of CO2 emissions and therefore a CO2 emission index of zero is applicable to the biomass. For materials containing both fossil and biomass carbon, a weighted index based on the percentage of fossil carbon in total carbon content in the fuel is used. The EU Regulation in the group of methods applicable to determine the biomass fraction of the fuel the analysis of the radioactive carbon isotope 14C is listed. The absence of 14C isotope in fossil fuels and its high and known content in contemporary biosphere allow to determine the ratio of old carbon to the modern carbon. The standard “ASTM D6866 - 11 Standard Test Methods for Determining the Biobased Content of Solid, Liquid, and Gaseous Samples Using Radiocarbon Analysis” wasadopted in 2011 by Poland for biocomponent determination in solid fuels, and allows using all measurement techniques used for 14C content determination.

A gradual depletion of global supply of fossil fuel – the raw material for the production of classic plastic, as well as the requirements to reduce the greenhouse gases emission, have influenced the scientific community to search for alternative material sources. Packaging materials produced from plant based sources are characterised by a “carbon footprint” more favourable for the environment. At the same time they do not require the non-renewable raw materials containing so-called “old carbon” to be used in their production. The development of new technologies to produce packaging materials requires the investigations of the renewable material content, and the radiocarbon method can be used to answer this question.

One of the most important problems of food industry is quality control. The GADAM Centre developed a method of determining the source of raw materials used for vinegar production with use of 14C method. The measurement of the concentration of 14C in vinegar or pickle sample allows the determination whether the vinegar was produced in the process of fermentation or whether it was obtained from vinegar concentrate produced from coal or oil and burnt lime, i.e. state with high certainty whether vinegar was produced from plant material or in synthetic processes, even in cases where mixtures are used. Such measurements are of great importance for vinegar producers and for controlling bodies.

The present cooperation of the GADAM Centre with industrial institutions and fuel manufacturers will result in adaptation of the radiocarbon measurement procedures applied in the Gliwice Radiocarbon Laboratory to the needs of industrial applications.

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S16-P-124

DENDROCHRONOLOGICAL POTENTIAL OF FRAXINUS UHDEI AND ITS USE AS BIOINDICATOR OF FOSSIL CO2 EMISSIONS

beRaMenDI-oRoSco l.(1), GONZALEZ-HERNANDEZ G.(2)

(1) Instituto de Geologia, UnaM, MeXIco Df, MeXIco; (2) Instituto de Geofisica, UnaM, MeXIco Df, MeXIco

AbstractDendrochronological studies are limited in tropical regions because not many tree species form annual growth-rings. In this work we present an evaluation ofthe dendrochronological potential of tropical ash (fraxinus uhdei) and its use as bioindicator of the Suess Effect in urban areas, by means of radiocarbon analysis on growth-rings. We analysed a cross section of a tree that grew during the period 1932 - 2007 in San Luis Potosí (22.11°N 101°W, 1890 m.a.s.l.), one of the most industrialised cities in Mexico. The cross section was surfaced with a belt sander and with sandpaper of progressively finer grain until wood structure was clearly visible and rings could be counted. Individual rings, presumably corresponding to the 1950 – 1970 period, were sectioned with a stainless steel chisel, solvent extracted with Ethanol:Toluene (2:1 v/v) for 24 hours, and milled in a vibratory ball mill. Radiocarbon concentrations were determined at the Radiocarbon Laboratory of the National University of Mexico,by ultra low level liquid scintillation spectrometry using a Quantulus 1220 spectrometer with 3 mL Teflon vials. The Δ14C values obtained follow the same variation pattern as the calibration curve of the Northern Hemisphere (NH) zone 2 (Hua and Barbetti, 2004), with the peak centred in 1964 and a value of 680.02 ± 2.33 ‰, 124 ‰ lower than the NH zone 2 calibration curve. The close correspondence between the variation patterns indicates that this species does form annual growth-rings, and the lower values can be attributed to the 14C-dilution caused by fossil CO2 emissions. The Suess Effect was calculated using the NH zone 2 data as the background 14C, and the fossil CO2 concentrations were estimated using the mean CO2 concentrations reported for Mauna Loa station (Keeling et al., 2009) and reconstructed from Antartic ice cores (Etheridge et al., 1996). The magnitude of the Suess Effect varied between -6.9% and -0.5% (mean of -3.6%), equivalent to fossil CO2 concentrations ranging between 21.9 and 1.5 ppmv, respectively (mean 7.6 ppmv). The values have significant variations with no apparent monotone increasing trend, suggesting that the CO2 emissions have diverse sources; however, we are analysing the entire tree-ring sequence in order to evaluate the emissions history of San Luis Potosi. We conclude that fraxinus uhdei has potential for dendrochronological studies in tropical areas because its growth-rings are formed annually and, furthermore, it can be used as bioindicator of atmospheric 14C variations and Suess Effect in urban areas.

References1. Etheridge DM, Steele LP, Langenfelds RL, Francey RJ (1996). Journal of Geophyisical Research, 101, D2: 4115

– 4128.2. Hua Q, Barbetti M (2004). Radiocarbon, 46 (3): 1273–1298.3. Keeling RF, Piper SC, Bollenbacher AF, Walker SJ (2009) http://cdiac.ornl.gov/ftp/trends/co2/maunaloa.co2.

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S16-P-125

COMPLEMENTING CORAL Δ14C FROM ENEWETAK ATOLL DURING THE 1950S WITH MEASUREMENTS OF OTHER BOMB-PRODUCED ISOTOPES, PLUTONIUM AND URANIUM-236

FIFIELD K., TIMS S., fallon S.

australian national University, canbeRRa, aUSTRalIa

AbstractThe Δ14C history of surface waters in and around Enewetak Atoll (RMI) in the tropical western Pacific during the period of nuclear weapons testing is being reported elsewhere in this conference. Here, we report complementary measurements of other bomb-produced radioisotopes, and in particular isotopes of plutonium and uranium-236. Measurements were performed on the same Porites coral as that used for the radiocarbon measurements. Enewetak Atoll was a major nuclear test-site during the 1940-50s and the 1957 Oak H-bomb test was conducted only 2 km west of the coral site. We will present plutonium and 236U data from pre-bomb years to 1984 encompassing the bomb testing period, and compare with the radiocarbon record.

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326

S16-P-126

CARBON-14 IN RADIOACTIVE WASTE FOR DECOMMISSIONING OF IGNALINA NUCLEAR POWER PLANT

MAZEIKA J.(1), VaITKeVIcIene V.(1), SKURaToVIc Z.(1), MoTIeJUnaS S.(2), VaIDoTaS a.(2), oRYSHaKa a.(3), oVcHInIKoV S.(3)

(1) nature Research centre, VIlnIUS, lITHUanIa; (2) Radioactive Waste Management agency, VIlnIUS, lITHUanIa; (3) Ignalina nuclear Power Plant, VISaGInaS, lITHUanIa

Abstract

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327

S16-P-127

MEASUREMENTS OF 14C TO EVALUATE THE INFLUENCE OF NUCLEAR FACILITIES IN THE ENVIRONMENT

anTonellI c.(1), BOULET B.(2), coSSonneT c.(2), GonTIeR G.(3), GURRIaRan R.(2), le coRRe c.(2), MaRo D.(4), MoReaU c.(5), RenaUD P.(1), RoUSSel-DebeT S.(1)

(1) IRSn, SaInT-PaUl-leZ-DURance, fRance; (2) IRSn, oRSaY, fRance; (3) eDf, lYon, fRance; (4) IRSn, cHeRboURG-ocTeVIlle, fRance; (5) cea, SaclaY, fRance

AbstractAmong its missions, IRSN studies the radionuclide distribution and transfer processes in the various components of natural and man-made ecosystems. In this context, measurements of 14C are performed with two methods by IRSN: liquid scintillation after benzene synthesis and accelerator mass spectrometry (AMS). These techniques, originally used for 14C dating, are perfectly suitable for environmental measurements. Their complementarity will be described and examples showing the influence of present nuclear facilities will be presented.

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S16-P-128

RADIOCARBON FINGERPRINT OF PAKS NPP IN A NEARBY TREE

JANOVICS R.(1), KeRn Z.(2), baRnabÁS I.(3), VeReS M.(4), GÜTTleR D.(5), WacKeR l.(5), MolnÁR M.(1)

(1) Institute of nuclear Research of the Hungarian academy of Sciences, DebRecen, HUnGaRY; (2) Institute for Geological and Geochemical Research Hungarian academy of Sciences, bUDaPeST, HUnGaRY; (3) Public limited company for Radioactive Waste Management, PaKS, HUnGaRY; (4) Isotoptech co. ltd., DebRecen, HUnGaRY; (5) Swiss federal Institute of Technology, ZÜRIcH, SWITZeRlanD

AbstractA part of C-14 isotope emitted by Paks Nuclear Power Plant (NPP) goes to the atmosphere as inorganic CO2 gas, furthermore, a part of the hydrocarbons emitted in a higher quantity is oxidised to CO2 in the environment. Trees mostly cover their carbon demands by the uptake of atmospheric CO2 via photosynthesis. Normally cellulose is not reutilised by the metabolism once generated, therefore, the changes in the atmospheric C-14 activity concentration can possibly be fingerprinted by the measurements of the radiocarbon activity in the tree rings.

We collected tree ring series representing the past 10 years from the vicinity of the nuclear power plant and from a background area (B24 at Dunaföldvár). Measurements were performed by high-precision AMS 14-C method at ETHZ Zürich. The tree ring radiocarbon activity concentration data of the surrounding tree rings were compared to the background ones for each year. The C-14 activity concentration of the atmosphere has been continuously decreasing since the nuclear weapon tests in 1965. The decreasing trend can also be observed in case of the samples collected by the atmospheric C-14 sampling units operating at the monitoring stations of Paks NPP (Molnár et al. 2007). This decreasing trend can also be observed both in the results of the annual rings of trees in the background and in the vicinity of the NPP. The C-14 activity concentration of the tree rings was decreasing by nearly 4 pMC in the course of the last 10 years. The age of the sample trees is around 10 years. As they were planted saplings, the data of the first three years after 2000 for the Paks tree ring samples can be considered to be background values. In 10th April 2003 a malfunction occurred at the block no. 2 of Paks NPP, and a small amount of radioactive material was emitted to the environment. The tree rings of 2003 and 2004 of the Paks samples have higher C-14 activity concentrations that might indicate the excess C-14 emission due to the malfunction in the NPP. To interpret the slight increase in 2007 further research is made using the data of the emissions of the Interim Spent Fuel Storage Facility (ISFSF) and Paks NPP.

NPP and ISFSF published C-14 emission data based on stack air monitoring will be compared to the measured tree ring C-14 signal.

ReferencesM Molnár, T Bujtás, É Svingor, I Futó, I Světlík MonIToRInG of aTMoSPHeRIc eXceSS 14c aRoUnD PaKS nUcleaR PoWeR PlanT, HUnGaRY; RADIOCARBON, Vol 49, Nr 2, 2007, p 1031–1043

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S16-P-129

FOSSIL CARBON IN CITY AIR: ONE YEAR SYNCHRONIZED AEROSOL AND CO2 OBSERVATION IN DEBRECEN, HUNGARY

MAJOR I.(1), fURU e.(1), RInYU l.(2), VoDIla G.(2), KeRTÉSZ Z.(2), MolnÁR M.(2), HaJDaS I.(3)

(1) University of Debrecen-MTa aToMKI, DebRecen, HUnGaRY; (2) MTa aToMKI, DebRecen, HUnGaRY; (3) eTHZ, ZÜRIcH, SWITZeRlanD

AbstractAtmospheric fossil CO2 observations have been running in Debrecen, Hungary since the autumn of 2008 (Molnár et al., 2010). From the winter of 2010 synchronized aerosol sampling and C-14 analyses started to compare the aerosol fossil carbon content to the fossil carbon-dioxide results in the same time period and the same location. Integrated bulk aerosol PM2.5 samples were collected on prebaked quartz filers with 10 L/min flow rate over the months. Normally 1-2 weeks integrated samples were collected on a filter and those periods were combined to be synchronized with the parallel monthly atmospheric CO2 observations. The collected total aerosol mass and its carbon content was determined by the weight increasing of the applied filter and the amount of CO2 produced after its combustion in the AMS C-14 sample preparation line.

Atmospheric fossil CO2 measurements were done using the ATOMKI gas proportional counting based C-14 dating facility. C-14 measurement of the tiny aerosol bulk samples was done using the EnvironMICADAS (from ETHZ Zürich) AMS in ATOMKI, Debrecen. The applied sample pretreatment steps were tested by multiple pretreatment of different sections of several real samples. Test results showed very good reproducibility for the applied aerosol sample preparation and AMS C-14 analyses.

During the year from November 2010 to November 2011 in Hungary several times there were very high PM concentrations in the city air, particularly during the winter of 2011. Our results showed that not fossil but biogenic carbon was causing the elevated PM concentrations in Debrecen city. This effect was the opposite C-14 signal what we have seen in the CO2 fossil contribution. These results clearly show the very different fossil/biogenic contribution in the atmospheric aerosol comparing the carbon-dioxide fraction. Our results are in good agreement with other published city fossil aerosol results (etc. from Zürich) (Szidat et al., 2004). To help the source apportionment of the collected city aerosol samples also δ13C stable isotope ratio of the combusted carbon fraction was measured using a Finningan Delta XP plus stable isotope mass spectrometer.

References1. M. Molnár, L. Haszpra, É. Svingor, I. Major, I. Svetlik. atmospheric fossil fuel co2 measurement using a field

unit in a centraleuropean city during the winter of 2008/09. Radiocarbon 52 (2010) 2-3: 835-8452. S Szidat, T.M Jenk, H.W Gäggeler, H.-A Synal, R Fisseha, U Baltensperger, M Kalberer, V Samburova, S

Reimann, A Kasper-Giebl, I Hajdas. Radiocarbon (14c)-deduced biogenic and anthropogenic contributions to organic carbon (oc) of urban aerosols from Zürich, Switzerland. Atmospheric Environment, Volume 38, Issue 24, August 2004, Pages 4035-4044

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S16-P-130

14CO2 LEVELS IN MEXICO CITY REVEAL A COMPLEX MIXTURE OF EMISSION SOURCES

BERAMENDI-OROSCO L.(1), GonZaleZ-HeRnanDeZ G.(2), SolIS-RoSaleS c.(3)

(1) Instituto de Geologia, UnaM, MeXIco Df, MeXIco; (2) Instituto de Geofisica, UnaM, MeXIco Df, MeXIco; (3) Instituto de fisica, UnaM, MeXIco Df, MeXIco

AbstractRadiocarbon concentrations in atmospheric CO2 have been monitored in Mexico City with monthly resolution since March 2009. CO2 integrated samples (continuous for period March 2009 – August 2010, and daytime-only since August 2010) are collected by pumping air through an alkaline solution for a period of 15 – 30 days at a well ventilated area inside the National University’s Campus at the south of Mexico City. Samples are transformed to benzene and analysed by ultra low level Liquid Scintillation Spectrometry in a Quantulus 1220 spectrometer with 3 mL Teflon vials, at the Radiocarbon Laboratory of the National University of Mexico. Δ14C values present high variability. For 2009, values range between -275.39 ‰ and +76.34 ‰ (mean +5.87 ‰) with the lowest value found for September and the highest values for July. For 2010, values range between -285.34 ‰ and +44.98 ‰ (mean -58.78 ‰); as for the previous year, the lowest value corresponds to September and the highest value to July. Samples for 2011 are presently being analysed.

When comparing the obtained radiocarbon data with mean background values reported for Niwot Ridge, Colorado (Turmbull et al., 2008) we find that most of the samples are significantly depleted in 14C, as a result of the high volume of fossil fuels burned in the biggest megacity in North America; however, there are periods with Δ14C values unexpectedly high, up to 35 ‰ higher than background values for July 2009 and 5 ‰ for July 2010. High Δ14C values have been previously reported for Mexico City and its metropolitan area in the scope of the March 2006 MILAGRO campaign by Vay et al. (2009). The results from both studies make evident the complexity of the emission sources in the area, with either important contributions from CO2 containing 14C concentrations slightly higher than natural levels such as biogenic CO2 or biomass burning; or small contribution from enriched “hot” 14C sources such as medical and hazardous waste incinerators (Vay et al., 2009), that cancel-out the 14C dilution derived from fossil fuels burning. In order to explain the Δ14C variability observed and the anomalously high values, we are now comparing our record with other atmospheric parameters (CO, PM10 and PM2.5) that are monitored by the Automatic Ambient Air Monitoring Network Mexico City (SMADF, 2012).

References1. SMADF (Secretaría del Medio Ambiente del Distrito Federal). http://www.calidadaire.df.gob.mx/calidadaire/

index.php?opcion=2&opcioninfoproductos=22. Turnbull JC, Lehman SJ, Miller JB, Tans PP (2008). Radiocarbon Composition of Atmospheric Carbon Dioxide

(14CO2) from the NOAA ESRL Carbon Cycle Cooperative Global Air Sampling Network, 2003-2007, Version: 2008-10-24. Consultado en: ftp://ftp.cmdl.noaa.gov/ccg/co2c14/flask/event/. (accessed January 2012)

3. Vay SA, Tyler SC, Choi Y, Blake DR, Blake NJ, Sachse GW, Diskin GS, Singh HB (2009). Sources and transport of Δ14C in CO2 within the Mexico City Basin and vicinity. Atmospheric Chemistry and Physics, 9, 4973-4985.

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SESSION 17

14C TRACER OF LIFE

Convenersm.J.I. Briones (ESP), J. Vogel (USA)

DescriptionThis session seeks papers and discussions of the use of 14C and other isotopes, natural or anthropogenic, to the study of current living members of the plant and animal kingdoms, from humans to fungi. The primary connection among possible topics is use of isotopic signals to distinguish the metabolic paths and compositional sources within living systems. In particular we welcome those studies investigating the ecology of organisms in soils and sediments, nutrient sources in extremophile environments, regeneration of physiological isolates («bomb pulse» dating) and tracing isotope labeled compounds in humans, animals and plants. Distinct isotopic sources include the Earth’s surface biosphere, isotope-depleted reservoirs, anthropogenic isotope excursions, and intentionally isotope-labeled products (e.g. quantification of nutrient or pharmaceutical metabolism and distinction of natural versus manufactured components).

Keywordsecology of dwelling organisms, living system, metabolism, nutrient, regeneration, extremophile, pharmaceutical, isotope-labeled

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S17-P-131

RADIOCARBON DATING OF A TERTIARY RELICT SPECIES IN SPAIN

SANTOS-AREVALO F.J.(1), GoMeZ-MaRTIneZ I.(1), MeJIaS J.a.(2), aRRoYo J.(2)

(1) centro nacional de aceleradores (Universidad de Sevilla, cSIc, Junta de andalucia), SeVIlla, SPaIn; (2) Dpto. de biologia Vegetal y ecologia, Universidad de Sevilla, SeVIlla, SPaIn

AbstractRhododendron ponticum is a Tertiary relict lauroid shrub that represents a vestige of evergreen rainforest that thrived during the Tertiary in many areas of Europe. Currently, natural populations can only be found in small areas of southern and western Iberian Peninsula and the Black Sea Basin (where a differentiated subspecies has been recognized). Due to its biogeographical importance, it is protected by law and under normal circumstances only harmless studies for the plant can be carried out. This makes very difficult to estimate important life-history parameters such as longevity, which is of extreme interest to analyse population dynamics and viability. Adult plants commonly bear a developed lignotuber from which many branches arise; however such branches are useless for estimating age because plants resprout vigorously, with a replacement of them along the life of the plant (note that a single branch may show up to 130 annual growth rings). Taking advantage of the recent death of several specimens, probably due to drought, wood fragments from the lignotubers have been sampled in order to date them by radiocarbon AMS and obtain an estimate of the age. Due to the difficulty in visualizing rings because of the irregular growing pattern of the lignotuber, several samples are needed to get a useful value. Results are expected to improve the knowledge of population biology and persistence of this endangered species in Spain.

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S17-P-132

CARBON ISOTOPIC COMPOSITION OF STEROID HORMONES IN ORAL CONTRACEPTIVE PILLS

GRIFFITH D.(1), eGlInTon T.(2), WacKeR l.(3), GScHWenD P.(4)

(1) MIT/WHoI, caMbRIDGe, UnITeD STaTeS; (2) Geological Institute, eTH-Zurich, ZURIcH, SWITZeRlanD; (3) Ion beam Physics, eTH-Zurich, ZURIcH, SWITZeRlanD; (4) civil and environmental engineering, MIT, caMbRIDGe, UnITeD STaTeS

AbstractThousands of studies have focused on the concentration and toxicity of steroid hormones in sewage-impacted aquatic environments, yet few have attempted to characterize the relative contributions from synthetic versus natural sources. In this study, we characterize the 13C and 14C signatures of ethynylestradiol (EE2) and progestins in oral contraceptive pills and synthetic standards to determine whether carbon isotope data can be used to elucidate the sources, transport, and transformations of these hormones in complex environmental systems. Carbon isotope data suggest that EE2 (Δ14C = -189 ± 18 ‰) is synthesized primarily from C3 plant-based steroidal starting materials such as stigmasterol and β-sitosterol. The observed magnitude of 14C depletion is consistent with both ethynyl carbons in EE2 originating from petrochemical sources. Synthetic endogenous estrogens (such as estrone and estradiol) contained exclusively modern carbon (Δ14C = 48 ± 2 ‰). And, although most progestins are distinctly 14C depleted (Δ14C = -992 ± 13 ‰), others, including synthetic progesterone, have modern 14C signatures. Together, these data suggest that approaches using fossil carbon content (14C) alone would likely underestimate environmental loadings of synthetic hormones. Fortunately, natural and synthetic hormones have distinct 13C signatures. Typical C4 plant contributions to our diets are reflected in endogenous (“natural”) steroids (δ13C ~ -16 ‰ to -26 ‰), which are enriched compared to synthetic estrogens (δ13C = -30.0 ± 0.9 ‰) and progestins (δ13C = -30.3 ± 2.6 ‰). This distinction is frequently used in anti-doping investigations and to detect illegal hormone treatment in livestock. Our results suggest that 13C may also hold promise for apportioning sources of natural and synthetic steroidal hormones in a variety of environmental matrices.

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SESSION 20

14C AND MODELLING

ConvenersF. marzaioli (ITA), R. muscheler (SWE), K. Rodgers (USA)

DescriptionRadiocarbon, the cosmogenic and anthropogenic (bomb carbon) radionuclide, is widespread in all the environmental compartments being naturally involved in the global carbon cycle. Due to its nature, 14C preserves the potential to serve as process tracer and/or chronometer. Since its discovery and the birth of the radiocarbon dating methodology, modelling approaches have been widely applied to disentangle the physical mechanisms governing its production and observed distributions. Over the last decades, with the advent of the earth and climate change sciences, radiocarbon became a preferential tool for the study of dynamical processes in climate and carbon cycle. For the carbon cycle, this includes interactions with the physical climate system, and this has been investigated using a variety of modelling tools and methods.This session aims to attract contributions applying modelling approaches to the study of processes characterizing the atmosphere, hydrosphere, biosphere and atmosphere and fluxes within and between these compartments. Contributions quantifying natural changes and the impact of anthropogenic actions on the contemporary and past climate system are also particularly welcome.

Keywords14C production modelling, direct/inverse modelling for global cycle, past and contemporary climate change

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S20-P-133

SYNTHETIC CONSTRAINT OF ECOSYSTEM C MODELS USING RADIOCARBON AND NET PRIMARY PRODUCTION (NPP) IN NEW ZEALAND GRAZING LAND

BAISDEN W.T., KelleR e.D.


AbstractTime-series radiocarbon measurements have substantial ability to constrain the size and residence time of the soil C pools commonly represented in ecosystem models. Radiocarbon remains unique in the ability to constrain the large stabilized C pool with decadal residence times. Radiocarbon also contributes usefully to constraining the size and turnover rate of the passive pool, but typically struggles to constrain pools with residence times less than a few years. Overall, the number of pools and associated turnover rates that can be constrained depends upon the number of time-series samples available, the appropriateness of chemical or physical fractions to isolate unequivocal pools, and the utility of additional C flux data to provide additional constraints. In New Zealand pasture soils, we demonstrate the ability to constrain decadal turnover times within a few years for the stabilized pool and reasonably constrain the passive fraction. Good constraint is obtained with two time-series samples spaced 10 or more years apart after 1970. Three or more time-series samples further improve the level of constraint. Work within this context shows that a two-pool model does explain soil radiocarbon data for the most detailed profiles available (11 time-series samples), and identifies clear and consistent differences in rates of C turnover and passive fraction in Andisols vs Non-Andisols. Furthermore, samples from multiple horizons can commonly be combined, yielding consistent residence times and passive fraction estimates that are stable with, or increase with, depth in different sites.

Radiocarbon generally fails to quantify rapid C turnover, however. Given that the strength of radiocarbon is estimating the size and turnover of the stabilized (decadal) and passive (millennial) pools, the magnitude of fast cycling pool(s) can be estimated by subtracting the radiocarbon-based estimates of turnover within stabilized and passive pools from total estimates of NPP. In grazing land, these estimates can be derived primarily from measured aboveground NPP and calculated belowground NPP. Results suggest that only 19-36% of heterotrophic soil respiration is derived from the soil C with rapid turnover times. A final logical step in synthesis is the analysis of temporal variation in NPP, primarily due to climate, as driver of changes in plant inputs and resulting in dynamic changes in rapid and decadal soil C pools. In sites with good time series samples from 1959-1975, we examine the apparent impacts of measured or modelled (Biome-BGC) NPP on soil radiocarbon (Fraction Modern). Ultimately, these approaches have the ability to empirically constrain, and provide limited verification, of the soil C cycle as commonly depicted ecosystem in biogeochemistry models.

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S20-P-134

CHANGING CONTROLS ON OCEANIC RADIOCARBON: NEW INSIGHTS ON SHALLOW-TO-DEEP OCEAN EXCHANGE AND ANTHROPOGENIC CO2 UPTAKE

GRAVEN H.(1), GRUbeR n.(2), KeY R.(3), KHaTIWala S.(4), GIRaUD X.(5)

(1) University of california - San Diego, la Jolla, UnITeD STaTeS; (2) eTH Zurich, ZURIcH, SWITZeRlanD; (3) Princeton University, PRInceTon, UnITeD STaTeS; (4) lamont-Doherty earth observatory, PalISaDeS, UnITeD STaTeS; (5) aix-Marseille University, aIX-en-PRoVence, fRance

AbstractOceanic measurements of bomb-produced 14C have provided a powerful tracer of oceanic exchange and transport processes, particularly through their constraint on the rate of air-sea gas exchange. The penetration of bomb-14C was initially limited by air-sea exchange rates due to the abrupt increase in atmospheric concentration and strong resulting air-sea gradients. We will show that air-sea exchange rates are now less important than internal ocean transport and mixing rates in determining air-sea fluxes of 14C and the redistribution of oceanic 14C. This is because a large amount of 14C has accumulated in the shallow ocean, which has strongly reduced and even reversed air-sea gradients in some regions. Therefore, 14C is now most sensitive to the same processes that determine anthropogenic CO2 uptake. We use observed 14C changes between hydrographic surveys in recent decades to evaluate ocean model transport and place independent upper and lower bounds on global oceanic CO2 uptake over 1990-2007.

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337

S20-P-135

MODELLING ATMOSPHERIC 10Be ON A 75 KYR TIMESCALE: DEPENDENCE ON A VARYING GEOMAGNETIC FIELD STRENGTH AND CLIMATE CHANGE

ELSÄSSER C.(1), WaGenbacH D.(1), leVIn I.(1), aSGeIRSSon b.(1), laJ c.(2), MUScHeleR R.(3)

(1) Institute of environmental Physics, University of Heidelberg, HeIDelbeRG, GeRManY; (2) laboratoire des Sciences du climat et de l’environnement, GIf-SUR-YVeTTe, fRance; (3) Department of earth and ecosystem Sciences, Division of Geology, lund University, lUnD, SWeDen

AbstractPast variations of atmospheric 14C originate in both, changes in the carbon cycle and a varying production rate (driven by geomagnetic and solar activity changes). Although extensively investigated, the share of each determining factor is a matter of ongoing debate. Being independent of global carbon fluxes, the cosmogenic aerosol-borne radionuclide 10Be, that can be measured in polar ice-cores, allows for reconstructing the production rate variability. While its short atmospheric lifetime in principle offers a direct record of the past production rate changes, atmospheric transport and deposition effects may distort the production signal under investigation. Several attempts have been made to investigate these effects using global circulation models, but these model runs are normally restricted to decennial time scales. Indeed, it is of special interest to largely extend the time scale under investigation to several 1000 years, since the shape of the production distribution follows changes in the geomagnetic field.

In our attempt to model atmospheric 10Be we used extensive data sets of global bomb fission radionuclide measurements to adapt a well-calibrated and intensively used box model (of the atmospheric 14C cycle) for simulations of aerosol-borne species. Using global 7Be measurements for model validation, our results reveal that this comparatively simple model approach is well suited to also simulate the spatial and temporal distribution of 10Be in the atmosphere. Extension of model simulations to the 75 kyr time scale is now possible, and, for the first time, respective 10Be simulations can be directly compared to ice core records. We used several independent reconstructions of the geomagnetic field intensity to drive the 10Be variability and investigate climate change effects (glacial-interglacial) in a dedicated sensitivity study. Finally, we review the capability of 10Be to be used as a proxy for the 14C production rates.

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S20-P-136

DEVELOPMENTS IN MODELLING OF C-14 IN THE BIOSPHERE FOR SOLID RADIOACTIVE WASTE DISPOSAL

MOBBS S.(1), SHaW G.(2), noRRIS S.(3), MaRanG l.(4), SUMeRlInG T.(5), albRecHT a.(6), XU S.(7), THoRne M.(8), lIMeR l.(9), PaUlleY a.(10), SMITH K.(1), SMITH G.(11)

(1) eden nuclear and environment, faRInGDon, UnITeD KInGDoM; (2) nottingham University, noTTInGHaM, UnITeD KInGDoM; (3) nDa, lonDon, UnITeD KInGDoM; (4) eDf, PaRIS, fRance; (5) llWR, DRIGG, UnITeD KInGDoM; (6) anDRa, PaRIS, fRance; (7) SSM, STocKHolM, SWeDen; (8) Mike Thorne and associates, HalIfaX, UnITeD KInGDoM; (9) limer Scientific consulting ltd, SHanGHaI, cHIna; (10) Quintessa, HenleY, UnITeD KInGDoM; (11) GMS abingdon ltd, abInGDon, UnITeD KInGDoM

AbstractIt has long been recognised that C-14 is present in solid radioactive wastes arising from the nuclear power industry, in reactor operating wastes and, more significantly, in graphite and activated metals that will arise from reactor commissioning. Its relatively long half-life of 5730 years means that there is the potential for releases of C-14 to the biosphere from deep and near-surface radioactive waste repositories. These releases may occur as C-14 bearing gases, especially methane, or as aqueous species and enter the biosphere from below via natural processes or via groundwater pumped from wells.Whether released from repositories with gaseous or aqueous species, rapid equilibration tends to occur in the unsaturated soil zone, and a particular focus of attention is then the behaviour of C-14 incorporated into carbon dioxide evolved from the soil by microbial processes. C-14 bearing carbon dioxide mixes with natural C-14 and stable isotopes of C in the soil and the plant canopy atmosphere with degassing and re-deposition allowing inter-compartment transfers with eventual transfer into plant biomass (primarily through photosynthesis) and thence into the food chain. Several assessment models will be outlined that have been developed, incorporating different dynamic and static modules.A recent model inter-comparison exercise was undertaken to simulate the release of C-14 from the geosphere to the biosphere. This was organised by BIOPROTA, an international collaboration forum to address key uncertainties in the assessment of doses from radioactive waste management. This identified significantly different results for the activity concentrations in the soil, atmosphere and plant compartments, based upon the modelling approaches presented above. The major source of uncertainty was related to the identification of conditions under which mixing occurs and isotopic equilibria are established. Furthermore, whilst the assumed field geometry (i.e. size) plays a role in determining the calculated atmospheric C-14 concentrations, the openness of the plant canopy and the wind profile in and above that canopy are the key drivers. These and other spatial and temporal variations, e.g. carbon pools in soils, will be described.The inter-comparison helped to identify key processes that will allow us to improve our system understanding and associated simulations when considering the temporal and spatial conditions of actual assessment scenarios, i.e. the nature of the release from the geosphere. Research activities underway within the BIOPROTA forum to address some of these uncertainties will be described, in particular the work by our British colleagues investigating the soil-atmosphere-plant subsystem. Such experimental results will help us to make connections to existing models used to describe heat, moisture and momentum transport in plant canopies.

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S20-P-137

TEMPORAL AND SPATIAL DISTRIBUTION OF THE JOMON ARCHAEOLOGICAL SITES IN JAPAN USING RADIOCARBON CUMULATIVE PROBABILITY AND ECO-CULTURAL NICHE MODELS

OMORI T.(1), KonDo Y.(2), YoneDa M.(1)

(1) The University of Tokyo, KaSHIWa, JaPan; (2) Tokyo Institute of Technology, MeGURo, JaPan

AbstractWe report here a simulation models for temporal and spatial distribution. To reveal human adaptation to climate and environmental changes, it is necessary to understand not only the pattern of past environmental changes but also the distribution on archaeological evidence with high time-space resolution. Using radiocarbon cumulative probability and eco-cultural niche model, we illustrate the temporal and spatial distribution of archaeological evidence. This study focused on the southwest Kanto region during the Jomon period. In this region, an enormous number of archaeological site, over 6,000 sites, was excavated, and various radiocarbon chronologies were constructed so far. On the basis of archaeological approach with ceramic typology and radiocarbon dating, Kobayashi (2004) described the distribution and expansion of cultural exchanges during Jomon period. Although its archaeological research provided elaborate speculation for Jomon culture, the time resolution was not enough to discuss subtle adaptation to environmental changes. We collected the radiocarbon data from journal articles, books and research reports, and calculate radiocarbon cumulative probability to evaluate the time span and its likelihood for each cultural period. For these calculations, 14C Bayesian analysis with archaeological information was carried out. The obtained radiocarbon dates were used for spatial analysis. Eco-cultural niche model, such as Genetic Algorithm for Rule-set Production (GARP) and Maximum Entropy Model (Maxant), can expect suitable sets of ecological parameters for a species and illustrated predictive distribution. Combining the probability density of radiocarbon date to these niche models, the distribution model included the likelihood can be derived. In this paper, we will discuss the simulation model, and compare with the ecological and archaeological distributions.

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S20-P-138

OCEAN BOMB RADIOCARBON SINK: AN ELUSIVE PROBLEM?

MOUCHET A.

University of liege, lIÈGe, belGIUM

AbstractThe radiocarbon released in the atmosphere by nuclear weapons testing may provide the means to constrain global air-sea CO2 exchange as well as to assess near-surface circulation, vertical transport or mixing schemes in OGCMs. For that purpose a precise estimate of the ocean bomb 14C sink is necessary. However, due to the scarcity of pre-bomb ocean data, the exact amount that entered the sea may only be indirectly obtained from field measurements. Further, large discrepancies exist between data-based estimates and model reconstructions of the ocean bomb radiocarbon inventory. In order to resolve this gap, it has been proposed either that the data-based bomb 14C ocean inventory as initially proposed by Broecker et al. (1995) is overestimated (Rubin and Key, 2002; Peacock, 2004) or that the CO2 piston velocity should be revised downward (Sweeney et al., 2007; Muller et al., 2008).

Here we compare the transient 14C distributions in the ocean over the industrial era as predicted by two OGCMs when using different assumptions for modelling radiocarbon. First, the full carbon cycle is considered, that is including a complete representation of carbon isotopes and biological cycle. In the second set of experiments biological activity is neglected. Then, the simplified method of Toggweiler et al. (1989) is adopted.

While the bomb radiocarbon ocean uptake appears to be strongly affected in areas with significant control from biological activity on air-sea CO2 exchange the global ocean inventory does not differ significantly between biotic and abiotic experiments. On the other hand ocean inventories are about 10% lower with the simplified method which consists in transporting the 14C/C ratio. Differences among inventories predicted by the different OGCMs are much lower.

From these experiments it may be concluded, in agreement with Naegler (2009), who adopted another method of investigation, that field inventories are probably underestimated. This stems from the method that data-based reconstructions are based upon, mainly the assumption that the air-sea CO2 disequilibrium remained constant with time.

Shortcomings in OGCMs (e.g., inadequate vertical mixing) as well as the gas exchange velocity may explain the remainder of the discrepancy between model results and field estimates. These aspects are also examined.

References1. Broecker, W. S., et al., 1995, Global Biogeochem. Cycles, 9, 263–288, doi:10.1029/95GB00208.2. Müller, S. A., et al., 2008, Global Biogeochem. Cycles, 22, GB3011, doi:10.1029/2007GB003065.3. Naegler, T., 2009, Tellus, 61, 372–384, doi:10.1111/j.1600-0889.2008.00408.x.4. Peacock, S., 2004, Global Biogeochem. Cycles, 18, GB202210, doi:10.1029/2003GB002211.5. Rubin, S., and R. Key, 2002, Global Biogeochem. Cycles, 16, 1105, doi:10.1029/2001GB001432.6. Sweeney, C., et al., 2007, Global Biogeochem. Cycles, 21, GB2015, doi:10.1029/2006GB002784.7. Toggweiler, J. R., et al., 1989, J. Geophys. Res., 94, doi:10.1029/JC094iC06p08217.

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PostersCommunications

Session B

InDeX bY SeSSIon

Wednesday July 11Thursday July 12Friday July 13Session 1 - Calibration

Session 5 - Statistical tools

Session 6 - Variations in radiocarbon reservoir effects

Session 7 - Radiocarbon dating and the Palaeolithic

Session 8 - Archeology - Eurasia and Africa

Session 9 - Radiocarbon and Archaeology of the Americas and Oceania: Improving Chronologies and Theoretical Insights

Session 10 - Oceanic paleoclimatology and paleoceanography

Session 11 - Continental paleoclimatology and paleohydrology

Session 12 - Insights into the ocean carbon cycle from radiocarbon measurements

Session 14 - Continental carbon cycle

Session 15 - Atmospheric carbon cycle

Session 18 - Cosmogenic nuclides

Session 19 - Unusual Applications of 14C Measurement

342

SESSION 1

CALIBRATION

ConvenersE. Bard (FRA), J. van der Plicht (NLD), P. Reimer (UKGBR)

DescriptionRadiocarbon calibration is essential for correcting for the variability of the initial 14C content of the carbon reservoir where a sample grew or was formed. This session will cover all aspects of calibration including new and/or refined potential calibration data from a variety of archives, regional and/or time-dependent reservoir offsets, statistical methods for calibration and curve construction and techniques which help to constrain past 14C production changes such as 10Be or palaeomagnetics

Keywordscalibration, reservoir ages, 14C production

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S01-P-139

INTEGRATION OF THE OLD AND NEW LAKE SUIGETSU (JAPAN) TERRESTRIAL RADIOCARBON CALIBRATION DATASETS

STAFF R.A.(1), bRonK RaMSeY c.(1), bRYanT c.(2), bRocK f.(1), KITaGaWa H.(3), Van DeR PlIcHT J.(4), ScHlolaUT G.(5), MaRSHall M.(6), bRaUeR a.(5), laMb H.(6), PaYne R.(7), TaRaSoV P.(8), HaRaGUcHI T.(9), GoTanDa K.(10), YonenobU H.(11), YoKoYaMa Y.(12), naKaGaWa T.(7)

(1) University of oxford, oXfoRD, UnITeD KInGDoM;(2) neRc Radiocarbon facility (environment), eaST KIlbRIDe, UnITeD KInGDoM;(3) nagoya University, naGoYa, JaPan;(4) University of Groningen, GRonInGen, neTHeRlanDS;(5) German Research center for Geoscience (GfZ), PoTSDaM, GeRManY;(6) aberystwyth University, abeRYSTWYTH, UnITeD KInGDoM;(7) University of newcastle, neWcaSTle-UPon-TYne, UnITeD KInGDoM;(8) freie Universität berlin, beRlIn, GeRManY;(9) osaka city University, oSaKa, JaPan;(10) chiba University of commerce, cHIba, JaPan;(11) naruto University of education, naRUTo, JaPan;(12) University of Tokyo, ToKYo, JaPan

AbstractThe varved sediment profile of Lake Suigetsu, central Japan, offers an ideal opportunity from which to derive an extended terrestrial record of atmospheric 14C across the entire range of the radiocarbon dating method. Previous work by Kitagawa and van der Plicht (1998a, 1998b, 2000) provided such a dataset; however, problems with the varve-based age scale of their ‘SG93’ sediment core precluded the use of this dataset for 14C calibration purposes. Lake Suigetsu was re-cored in summer 2006, with the retrieval of overlapping sediment cores from four parallel boreholes enabling complete recovery of the sediment profile for the present ‘Suigetsu Varves 2006’ project (Nakagawa et al., in press). Over 600 14C determinations have been obtained from terrestrial plant macrofossils picked from the latter ‘SG06’ composite sediment core, which, coupled with the core’s independent varve chronology, provides the only non-reservoir-corrected 14C calibration dataset across the radiocarbon dating range. Additionally, recent physical matching of archive U-channel sediment from SG93 to the fully continuous SG06 sediment profile now allows the integration of the ≈ 300 14C determinations from the SG93 project with the SG06 dataset. This paper presents the excellent agreement between the respective projects’ 14C data, and illustrates the ≈ 900 individual radiocarbon determinations spanning the last circa 55,000 cal. years comprising the composite Lake Suigetsu 14C calibration dataset.

References1. Kitagawa H. and van der Plicht J. (1998a) Science 279, 1187-1190.2. Kitagawa H. and van der Plicht J. (1998b) Radiocarbon 40 (1), 505-515.3. Kitagawa H. and van der Plicht J. (2000) Radiocarbon 42 (3), 369-380.4. Nakagawa T. et al. (in press) Quaternary Science Reviews.

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S01-P-140

ARE THE FRACTIONATION CORRECTIONS CORRECT: ARE THE ISOTOPIC SHIFTS FOR 14C /12C RATIOS IN PHYSICAL PROCESSES AND CHEMICAL REACTIONS REALLY TWICE THOSE FOR 13C /12C?

SOUTHON J.

University of california, IRVIne, ca 92697-3100, UnITeD STaTeS

AbstractA critical part of the overall radiocarbon calibration process involves corrections for isotopic fractionation, that are necessary for placing radiocarbon dates on different materials on a common time scale. In conventional radiocarbon calculations these corrections are based on 13C/12C ratios (d13C values) with an assumed value of 2.0 for the fractionation for 14C relative to 13C (Craig, 1954): that is, isotopic discrimination in physical and chemical processes is assumed to cause relative shifts in the 14C /12C ratio that are exactly double those of 13C /12C. However, a 1984 experiment (Saliège and Fontes, 1984) produced a value for the fractionation ratio in photosynthesis of 2.3, that is still used in some modeling studies of radiocarbon in groundwater and speleothems. While the value of 2.3 is almost certainly incorrect, quantum mechanics calculations (Bigeleisen and Mayer, 1947) suggest that the true value may indeed deviate from 2.0. Given the high precisions that are now achievable in 14C measurements, these deviations could significantly impact the accuracy of some 14C dates. This presentation will re-analyze the 1984 data and give a brief overview of the quantum mechanics results. It is also intended to raise the visibility of this issue within the radiocarbon community, and hopefully to stimulate further work.

References1. Bigeleisen, J., Mayer M. G., 1947. Calculation of equilibrium constants for isotopic exchange reactions.

Journal of chemical Physics 15, 261-2672. Craig, H., 1954. Carbon-13 in plants and the relationships between carbon-13 and carbon-14 in nature.

Journal of Geology 62, 115-149.3. Saliège, J.F, Fontes, J. Ch., 1984. Essai de determination experimentale du fractionationnement des isotopes

13C et 14C du carbone au cours de processes naturels, International Journal of applied Radiation and Isotopes, 35 (1) 55-62

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S01-P-141

ESTIMATION OF 14CO2 AMOUNT IN THE ATMOSPHERE DURING HOLOCENE AND LATE GLACIAL

SVETLIK I.(1), PoVInec P.(2), feJGl M.(3), TUReK K.(1), PacHneRoVa bRabcoVa K.(1), ToMaSKoVa l.(1)

(1) nuclear Physics Institute aS cR, PRaGUe, cZecH RePUblIc;(2) Department of nuclear Physics and biophysics, faculty of Mathematics, Physics and Informatics, comenius University, bRaTISlaVa, SloVaKIa;(3) national Radiation Protection Institute, PRaGUe, cZecH RePUblIc

AbstractResults of calculation of activity concentration of atmospheric 14CO2 in the air during Holocene and Late Glacial periods are presented. Data on the reconstruction of the past CO2 mixing ratio from the Antarctic ice cores, and the D14C activity levels from IntCal09 and SHCal04 calibration curves were used in calculations. The resulting parameter of the 14CO2 concentrations in the air is reported in mBq of 14C per mole of the air. The parameter is connected with the quantity of 14C atoms/14CO2 molecules in the troposphere, without influencing a CO2 dilution. The resulting curve of activity concentration of atmospheric 14CO2 will be discussed and compared with paleodata of cosmogenic production of other radionuclides (10Be), the atmospheric CO2 mixing ratios, and the D14C values.

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346

S01-P-142

A HISTORICAL REVIEW OF SOME OF THE CONSENSUS VALUES FOR SAMPLES FROM PAST INTERNATIONAL RADIOCARBON INTER-COMPARISONS

SCOTT M.(1), cooK G.(2), naYSMITH P.(2)

(1) University of Glasgow, GlaSGoW, UnITeD KInGDoM;(2) SUeRc, eaST KIlbRIDe, UnITeD KInGDoM

AbstractMore than 20 years have passed since we started our series of inter-comparisons, during which time an archive of reference materials has been created for subsequent distribution as requested. In each inter-comparison, we have followed the same procedure to estimate consensus values for those reference materials for which we did not have a pre-defined age. The procedure is based on a three stage approach using robust statistics. We are aware of the continuing widespread use of some of the reference materials from TIRI, FIRI and VIRI as part of internal laboratory quality assurance procedures, especially in the case of AMS laboratories. It therefore seemed timely to:

1. review the published consensus values, especially since some were based on a relatively small set of measurements and so may be less robust and

2. to investigate whether these values need to be corrected.

We therefore instigated a review of the consensus values for as many of the reference materials as possible. To achieve this, we wrote to laboratories (AMS) that had been provided with these materials in large quantities and requested any available data for them.Materials that we report on include amongst others barley mash (from TIRI), whale bone and horse bone (from VIRI), cellulose (from FIRI), wood and carbonate from several exercises and humic acid.

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S01-P-143

THE NEXT INTERNATIONAL RADIOCARBON INTER-COMPARISON

SCOTT M.(1), cooK G.(2), naYSMITH P.(2)

(1) University of Glasgow, GlaSGoW, UnITeD KInGDoM;(2) SUeRc, eaST KIlbRIDe, UnITeD KInGDoM

AbstractWhile many laboratories have a well-defined set of internal quality control procedures, there remains a strong need to explore the comparability of results from different laboratories and hence generate consensus values for a range of reference materials to assist laboratories in independently assessing quality, and to quantify precision and accuracy. Inter-laboratory comparisons (sometimes also called proficiency trials) are designed to:• assess comparability of measurements made by the different laboratories• assist in the definition of overall uncertainty when results from different laboratories are used.An additional benefit that has arisen from past inter-comparisons has been the creation of a bank of well characterized reference materials which are made available to the community on request. The design of this new inter-comparison is that there will be one single round of sample distribution and that it will be restricted to AMS facilities in the main, due to the difficulty in acquiring sufficient quantities of material for radiometric laboratories. The majority of samples will be wood, but we will also include a small number of bone and other samples.The design of this new study is as follows:• a sequence of known age tree-rings (or if not possible, a floating tree ring sequence) will be provided. Ideally, this will be material from a time period within the calibration curve where there remains considerable uncertainty. This may be a sequence of single rings (appropriate for AMS) but may more likely be a sequence of multi-ring increments from a time period where there is a strong 14C activity gradient over the rings. Depending on availability, we envisage that we might provide two such sequences from different time periods (a maximum of 8 samples). The tree ring samples will be identified in their sequence, thus ensuring that the relationship of one sample to another is known. • several samples that are 14C-free (background)- we have already received one bone sample and are in discussion concerning a further wood background sample.• the final sample,again depending on the time period of the tree-rings, will be a modern sample.This exercise will last just over two years and will be concluded by the end of 2014.

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S01-P-144

INTERCOMPARISON OF RADIOCARBON DATING OF WOOD SAMPLES AT LUND UNIVERSITY AND ETH ZURICH: EXTRACTION, GRAPHITIZATION, AND MEASUREMENT.

ADOLPHI F.(1), GUeTTleR D.(2), WacKeR l.(2), SKoG G.(1), MUScHeleR R.(1)

(1) lund University, lUnD, SWeDen;(2) eTH Zurich, Switzerland, ZURIcH, SWITZeRlanD

AbstractThe International Radiocarbon Intercomparison Projects addressed quality assurance among different 14C measurement techniques and facilities. In addition, they partly addressed the influence of preparation protocols. However, scatter within each measurement technique could not be resolved in detail. With increasing precision of AMS measurements the investigation of this scatter becomes more important since it might be limiting the accuracy of high precision radiocarbon dating.Here we report a systematic comparison between the ETH Zurich and Lund University AMS facilities regarding the preparation and 14C-AMS dating of wood samples.The tests include two wood samples of known calendar age, and a blank sample from Eeemian oak. Both labs pretreated several batches of each sample to holocellulose following the BABAB protocol (Nemec et al. 2010). In Zurich samples are combusted in an elemental analyzer coupled to an automatic graphitization system. Lund uses sealed quartz tube combustion and a manual, less standardized graphitization line. Both setups reduce CO2 by reaction with H2 in the presence of Fe-catalyst. AMS-14C measurements were done using the MICADAS in Zurich, and the NEC-SSAMS in Lund. Both labs exchanged aliquots of holocellulose and graphite targets to allow for an independent assessment of chemical pretreatment, graphitization, and measurement.For the known samples we find good agreement between 14C-date determinations in both labs and expected ages from the INTCAL09 calibration record (Reimer et al. 2009). Reproducibility of the measurements agrees well within the quoted errors. AMS measurements in Lund yield larger errors than in Zurich due to lower counting statistics and superior machine conditions in Zurich. Results for machine blanks are about 2,000 14C years older in Zurich which is likely due to isobar corrections which are not possible at the NEC-SSAMS. Two extractions of blank samples done in Zurich yield significantly higher background levels. This could be related to a cellulose storage effect and will be discussed. Differences due to graphitization systems are more ambiguous.Interestingly, one of our known samples shows perfect agreement to measurements of the German oak chronology (Stuiver et al. 1998), being about 35 14C years older than INTCAL09 calibration record (Reimer et al. 2009) at that time.

References1. Nemec M, Wacker L, Hajdas I, Gäggeler H. 2010. Alternative Methods for Cellulose Preparation for AMS

Measurement. Radiocarbon 52(2-3):1358-13702. Reimer PJ, et al. 2009. INTCAL09 and MARINE09 radiocarbon age calibration curves, 0-50,000 years calBP.

Radiocarbon 51(4):1111-11503. Stuiver M, Reimer PJ, Brazunias TF. 1998. High-Precision Radiocarbon Age Calibration for Terrestrial and

Marine Samples. Radiocarbon 40(3):1127-1151

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S01-P-145

ACCURATE AGE DETERMINATION OF A HOLOCENE WIDE-SPREAD KG (KAWAGODAIRA) TEFRA IN JAPAN BY A WIGGLE MATCHING METHOD WITH A CONSIDERATION ABOUT THE POTENTIAL INFLUENCE BY LOCAL ANOMALIES OF ATMOSPHERIC 14CO2

TANI S.(1), KITaGaWa H.(1), HonG W.(2), PaRK J.(2), SUnG K.(2)

(1) nagoya University, naGoYa, JaPan;(2) Korea Institute of Geoscience and Mineral Resources (KIGaM), DaeJeon, SoUTH KoRea

AbstractLayers of volcanic ash or tephra form widespread chronostratigraphic marker horizons because of their distinctive characteristics and rapid deposition over large areas. Kg (Kawagodaira) tefra from Mt. Amagi (Izu Peninsula, central Japan) has been identified at archaeological sites as well as lake and terrestrial sediment cores in the central Japan, and have been used as a chronological control in Holocene. We used a fossil wood log with ca 150-year rings which was collected from the ignimbrite deposits on Mt Amagi (Kawagodaira). Thirty 14C data of tree-ring samples in every five years were used to derive a new precise and accurate date for the eruptions via «wiggle-matching» - matching the radiocarbon dates of a sequence of samples from the tree ring with the Northern Hemisphere calibration curve. In addition, we assessed the potential influence of local anomalies of atmospheric D14C by giving assumed offsets to a set of tree-ring 14C data and calculating the fitness between tree-ring 14C data (with offset) and the Northern Hemisphere calibration curve. The offset value at the best marching may correspond to local anomalies of atmospheric D14C. This approach might give a key to investigate the local offset of Northern Hemisphere calibration curve for the period and area that dendrochronologically dated tree does not exist.

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S01-P-146

EFFECTS OF LASCHAMP GEOMAGNETIC EXCURSION ON 14C PRODUCTION

CAUQUOIN A.(1), RaISbecK G.(2)(1), JoUZel J.(1), PaIllaRD D.(1)

(1) laboratoire des Sciences du climat et de l’environnement, GIf-SUR-YVeTTe, fRance;(2) centre de Spectrométrie nucléaire et de Spectrométrie de Masse, In2P3-cnRS-Université de Paris-Sud, oRSaY, fRance

AbstractThe atmospheric ratio 14C/C depends on two factors:

(i) cosmogenic production, influenced by solar activity and geomagnetic field,(ii) carbon distribution in the atmosphere, biosphere and oceans.

Around 40 000 years ago the calibration curve remains uncertain due to the low 14C/C ratio, uncertain reservoir effects, and the limited number of measurements. It is therefore interesting to study the production part during this time in order to provide some guidelines about 14C calibration, and/or to constrain the changes in carbon cycle necessary to bring model results into agreement with observations.The Laschamp excursion, which is a period of reduced geomagnetic field intensity, occurred ~41 ka BP. As a consequence, during this period cosmogenic isotope (10Be, 14C) production increased dramatically and its sensitivity to solar activity was enhanced.We focus here on the contribution of the Laschamp event to the 14C/C ratio (expressed as D14C) in the atmosphere between 37.5 and 45.5 ky BP. To this end, we use high-resolution (decadal) profiles of 10Be in ice cores from both Antarctica (EDC) and Greenland (GRIP – NGRIP) converted to 14C using the 10Be deposition pattern of Field et al. [1] and updated 14C/10Be production calculations from Masarik and Beer [2]. The results are input into a 12-box carbon cycle model. The use of the high-resolution 10Be input data allows us to study the influence of solar as well as geomagnetic modulation on the 14C production rate. We find that the amplitude of atmospheric D14C due to increased production during this period varies from 470‰ (EDC) and 565‰ (Greenland) for pre-industrial conditions (modern carbon cycle), to 510‰ (EDC) and 615‰ (Greenland) for estimated glacial conditions. These results can be compared to the IntCal09 calibration curve which shows an increase of ~400‰ in atmospheric D14C over the same period. We emphasize that our results are very sensitive to the choice of production calculations employed to make the conversion from 10Be to 14C. For example, using the same model, input data and glacial carbon cycle parameters, but the 1999 production calculations of Masarik and Beer [3], we find a D14C of 370‰ for EDC and 430‰ for Greenland. We have very recently learned of some new 14C production calculations by Kovaltsov, Mishev & Usoskin (provided by I. Usoskin, personal communication). We will discuss the implications of those calculations at the meeting.The box model used here assumes a constant carbon cycle. Because the Laschamp excursion straddles Dansgaard-Oeschger event 10, it would be interesting to do a similar study using a dynamic model to investigate the influence of possible changes in the carbon cycle during this period.

References[1] Field et al. (2006) J. Geophys. Res. 111, D15107.[2] Masarik and Beer (2009) J. Geophys. Res.114, D11103.[3] Masarik and Beer (1999) J. Geophys. Res.104(D10), 12,099–12,111.

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S01-P-147

TREE-RING 14C RECORDS ON ICE CORE TIME SCALES

MUSCHELER R.(1), aDolPHI f.(1), SVenSSon a.(2)

(1) lund University, lUnD, SWeDen;(2) University of copenhagen, coPenHaGen, DenMaRK

AbstractThe radiocarbon calibration curve is most accurate for the period where it is based on 14C measurements on dendrochronologically-dated trees. Tree-ring 14C records with relatively robust time scales extend nowadays back to about 14.000 years BP. Prior to this period radiocarbon calibration is based on less direct recorders of the atmospheric 14C variations (e.g. corals, foraminifera) that are usually also connected to more unsecure time scales.Recent progress in the development of floating tree ring chronologies has the potential to push the tree-ring based atmospheric 14C reconstructions further back into the past but the lack of independent and absolute dating is a problem if the records should be used for calibration purposes.However, independent age estimates can be obtained from the comparison to 10Be records from ice cores since 10Be and 14C records contain the common production rate signal driven by the varying cosmic ray flux impinging on the atmosphere.By comparing the GRIP 10Be record [Muscheler et al., 2004] with the floating Kauri 14C sequences [Turney et al., 2010] we will show the potential of combining both records for testing the presently available calibration record [Reimer et al., 2009]. The comparison illustrates systematic differences between ice core and 14C time scales. Furthermore, this comparison can provide valuable information about the carbon cycle during the last ice age.

References1. Muscheler, R., J. Beer, G. Wagner, C. Laj, C. Kissel, G. M. Raisbeck, F. Yiou, and P. W. Kubik (2004), Changes

in the carbon cycle during the last deglaciation as indicated by the comparison of 10Be and 14C records, earth Planet. Sc. lett., 219, 325-340.

2. Reimer, P. J., et al. (2009), IntCal09 and Marine09 radiocarbon age calibration curves, 0–50000 years cal BP, Radiocarbon, 51(4), 1111-1150.

3. Turney, C. S. M., et al. (2010), The potential of New Zealand kauri (Agathis australis) for testing the synchronicity of abrupt climate change during the Last Glacial Interval (60,000-11,700 years ago), Quaternary Science Reviews, 29(27-28), 3677-3682.

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S01-P-148

RADIOCARBON AGES OF ANNUAL RINGS FROM JAPANESE WOOD: EVIDENT AGE OFFSET FROM INTCAL09

NAKAMURA T., MaSUDa K., MIYaKe f., naGaYa K., YoSHIMITSU T.

nagoya University, naGoYa, JaPan

AbstractFor a comparison of tree-ring 14C data for Japanese trees with those of IntCal09, we have measured 14C ages of annual rings from three Japanese cedar trees grown on the Japanese archipelago. The first tree possessing a total of 382 annual rings was collected from the Murouji temple in Nara prefecture, central Japan (34°N, 136°E). The second one with totally 712 annual rings was collected from Yaku-shima Island in Kagoshima Prefecture, southern Kyushu, Japan (30°18’N, 130°30’E). The third huge one possessing 1455 annual rings was collected from the central part of Yaku-shima Island at the altiutude of around 1000 m, although the precise location of its growth is unknown. Calendar ages of annual rings were determined by dendrochronology for all three woods. For the Murouji tree (the first one) and the smaller Yaku-sugi tree (the second one), as an another test, the bomb peak in the 14C concentration was determined in the annual rings to assign the calendar age of AD1964. We separated tree rings grown in AD 1617-1739, AD 1413-1615, and AD 146-1072, and up to now measured 14C ages for 61, 173 and 446 annual rings from respective trees, on the single annual-ring basis.The individual annual ring was separated, the alpha-cellulose fraction was extracted after an acid-alkali-acid treatment, and a graphite target was prepared at the Solar Terrestrial Laboratory, Nagoya University. The carbon isotope ratios were measured on the targets at the Center for Chronological Research, Nagoya University.When the measured 14C dates are compared with the data points of the IntCal09 and SHCal04 datasets, it is recognized as a general trend that 14C wiggles of IntCal09 are well reproduced in the Japanese wood data. In particular, the 14C dates for Japanese wood in the calendar age range from AD1413 to 1739 are quite consistent with the IntCal09 dataset. To investigate the agreements between the two, the difference of 14C ages from Nagoya to those from IntCal09 was evaluated. The average shifts of Nagoya 14C ages from IntCal09 14C ages and one-sigma values were obtained to be +24.7, +15.9 and +5.3 14C years, and ±30.4, ±22.1, and ±20.8 14C years, for the calendar-year intervals of AD146-1072, AD1413-1615 and AD1617-1739, respectively. The difference of 14C age of SHCal04 to that of IntCal09 for respective calendar dates from AD1 to AD1950 is 49.3±15.0 14C years on an average. These results suggest that 14C ages of the bigger Yaku-sugi wood tend to be older than those of IntCal09, and are in-between values of 14C ages of IntCal09 and SHCal04. A similar trend has been reported for other Japanese trees collected from Ashinoko Lake, central Japan, comparing with IntCal98, for the restricted calendar age range (AD50-AD250). By this research, the disagreements became clear for 14C ages of Japanese woods from those of IntCal09, and our data suggest that air mass derived occasionally to southern Japan from the southern hemisphere is responsible for this phenomena.

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S01-P-149

ANNUAL BRISTLECONE PINE AND GERMAN OAK 14C DATA SETS CONFIRM 2625 BP 14C WIGGLE: MAJOR TWO DECADE REDUCTION IN 14C PRODUCTION?

FAHRNI S.M.(1), fUlleR b.T.(1), fRIeDRIcH M.(2), MUScHeleR R.(3), SoUTHon J.(1), WacKeR l.(4), TaYloR R.e.(5)

(1) Department of earth System Science, University of california, Irvine, IRVIne, UnITeD STaTeS;(2) Institute of botany, University of Hohenheim, STUTTGaRT, GeRManY;(3) Department of Geology, lund University, lUnD, SWeDen;(4) Institute of Particle Physics, eTH Zurich, ZURIcH, SWITZeRlanD;(5) Department of anthropology, University of california, Riverside and cotsen Institute of archaeology, University of california, los angeles, RIVeRSIDe/loS anGeleS, UnITeD STaTeS

AbstractPreviously published 14C measurements on decadal tree ring-dated Bristlecone pine wood (White Mountains, California, USA) have generally confirmed the overall contours of the almost 350 year “warp” in the mid First-Millennium BC INTCAL09 14C time scale as defined by tree ring-dated Irish and German oaks. In addition, a synthesized D14C record based on 10Be data from the GRIP Greenland ice core generally tracks the INTCAL09 consensus plot for this period.Within the ~350 year 14C plateau, two short-term 14C wiggles were noted: the first centered on 2405 cal BP and a second centered on 2625 cal BP. The 2405 cal BP episode was defined by only a single data point obtained on German oak. The consensus tree-ring/14C based INTCAL09 data does not recognize a feature at 2405 cal BP in light of data measured on Irish oak. In addition, the synthesized 10Be-based D14C follows the Irish oak data at 2405 cal BP. In contrast, the 2625 cal BP excursion is recognized by both.To further clarify the magnitude of the 2625 cal BP event, 14C determinations have been obtained on the same tree-ring dated Bristlecone pine series on which decadal wood samples had been measured, but in annual increments spanning 2611 to 2630 cal BP. Also, 14C determinations have been obtained on annual rings from tree-ring dated German oak spanning 2578 to 2647 BP. Both the annual 14C bristlecone pine and 14C German oak results confirm that a very rapid transient decrease in the 14C content of our tree ring/14C dated wood samples occurred over a period of about two decades.One possible interpretation of these data is that 14C production was significantly reduced for 10-20 years beginning about 2645 cal BP. An alternative explanation involving increased outgassing from the southern Oceans may be, in part or in whole, responsible for this effect. An evaluation of these and other possible interpretations will be considered citing evidence for and against the validity of the various explanations. Improvements in the 10Be-based curve using the most recent ice core time scale and resulting recalculations of the 10Be fluxes will also be presented. Moreover, we will compare the data documenting the 2625 cal BP event with that involving short-term increased solar activity and an associated 14C production rate drop around AD 1780.Our results document the value of targeted re-measurements of data underlying the 14C calibration curve for

(I) high-precision 14C dating and

(II) the discussion of the origins of atmospheric 14C variations such as, for example, solar activity variations in the past.

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S01-P-150

RE-INVESTIGATING THE ISOTOPIC FRACTIONATION CORRECTIONS IN RADIOCARBON MEASUREMENTS

FAHRNI S.M., SanToS G.M., SoUTHon J., XU X.

Department of earth System Science, University of california, Irvine, IRVIne, UnITeD STaTeS

AbstractBy convention (Stuiver and Polach, 1977), 14C data has to be corrected for any isotopic fractionation occurring in nature, during the sample preparation or the measurement. The fractionation factor b = 2.0 used to correct the 14C/12C ratio for shifts in the 13C/12C ratio has been proposed in 1954 (Craig, 1954) and has been applied ever since. While theoretical considerations have suggested moderate deviations of b from 2.0, some measurements have suggested larger differences (e.g. Saliège and Fontes, 1984). With the increasing precision of radiocarbon measurements, potential deviations of b from 2.0 become more significant, since these could cause shifts of several decades in some radiocarbon dates (Southon, 2011). It is therefore of great interest for the radiocarbon community to re-evaluate the fractionation corrections.We present approaches for the experimental determination of b and discuss results and their effects on radiocarbon dating.

References1. Stuiver M., Polach H.A., 1977. Discussion: reporting of 14C data. Radiocarbon 19(3):355–63.2. Saliège J.F., Fontes J.C., 1984. Essai de détermination expérimentale du fractionnement des isotopes 13C et

14C du carbone au cours de processus naturels. International Journal of applied Radiation and Isotopes 35(1):55–62.

3. Craig H., 1954. Carbon 13 in plants and the relationships between carbon 13 and carbon 14 in nature. Journal of Geology 62(2):115–49.

4. Southon J., 2011. Are the Fractionation Corrections Correct: Are the Isotopic Shifts for 14C/12C Ratios in Physical Processes and Chemical Reactions Really Twice Those for 13C/12C? Radiocarbon 53(4):691–704.

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S01-P-151

RADIOCARBON DATING OF JAPANESE TREE-RINGS WITH DELTA-18O CHRONOLOGY

SAKAMOTO M.(1)(2), naKaTSUKa T.(3), oZaKI H.(1)(4), MITSUTanI T.(5)(6)

(1) national Museum of Japanese History, SaKURa, JaPan;(2) The Graduate University for advanced Studies, SaKURa, JaPan;(3) nagoya University, naGoYa, JaPan;(4) The University of Tokyo (at present), ToKYo, JaPan;(5) nara national Research Institute for cultural Properties, naRa, JaPan;(6) Reserach Institute for Humanity and nature, KYoTo, JaPan

AbstractRadiocarbon dating of tree-rings in several regions with absolute chronology, that is ring-width dendrochronology, is required to discuss regional offsets from IntCal calibration curve. However, such tree-rings are limited in Japanese archipelago so far. For example, radiocarbon ages of dendro-dated bogwoods of Japanese cedar excavated in Hakone, Kanagawa1 and Japanese cypress in Toyamagawa, Nagano2 showed clear offsets from IntCal calibration curve during 1st to 2nd century AD. Radiocarbon dating of tree-rings from two wooden coffins made of Japanese umbrella pine in Nara3 was also carried out, but the comparison to calibration curve was not enough due to the lack of absolute tree-ring age.Recently, Nakatsuka proposed the possibility of delta-18O chronology of tree-rings in Japanese archipelago4. The oxygen isotope ratios of cellulose extracted from annual tree-ring is mainly controlled by precipitations and summer relative humidity in humid regions such as Japan. Oxygen isotope time-series of tree-ring cellulose shows high correlation among different tree species, not only conifer but also hardwood, in a certain clime. Therefore, delta-18O chronology of tree-rings can be rapidly constructed and extended after the measurement of oxygen isotope ratios with known age by ring-with dendrochronology.We examined the oxygen isotope time-series of previous tree-ring samples and the comparison of ring-width pattern and 14C-wiggle matching was carried out. Regional effects on calibration curve for Japanese tree-rings were confirmed by adding the absolute age by delta-18O, suggesting that this chronology should be a powerful tool in construction of calibration curve for radiocarbon dating.This work was supported by a Grants-in-Aid for Scientific Research (No. 21240072) of the Japan Society for the Promotion of Science.

References1. Sakamoto M., Imamura M., van der Plicht J., Mitsutani T., Sahara M. (2003) Radiocarbon 45: 81-89.2. Ozaki H., Sakamoto M., Imamura M., Matsuzaki H., Nakamura T., Kobayashi K., Itoh S., Niu E., Mitsutani T.

(2009) 20th International Radiocarbon Conference. Hawaii, United States.3. Sakamoto M., Ozaki H., Mitsutani T. (2011) 12th International Conference on AMS. Wellington, New Zealand.4. Nakatsuka T. (2011) 4th East Asia AMS Symposium. Tokyo, JAPAN.

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S01-P-152

REGIONAL OFFSET OF RADIOCARBON AND ITS VARIATION IN KOREA DURING THE LAST 600 YEARS

HONG W.(1), PaRK J.(1), PaRK G.(1), SUnG K.(1), PaRK W.(2), lee J.(1)

(1) Korea Institute of Geoscience and Mineral Resources, DaeJeon, SoUTH KoRea;(2) chungbuk national University, cHeonGJU, SoUTH KoRea

AbstractA series of annual tree-ring measurement has been performed for reconstruction of radiocarbon concentration variation in Korea. The absolute ages of the samples were determined by dendrochronological method. The main purpose of this project is production of a calibration curve to reduce error included in radiocarbon age due to regional offset of this country. However, high resolution data of 14C concentration variation over the several hundred years implies many things such as cosmic-ray variation, regional geological events, and impactful climate change. Among them, we notice their relation with the climate change.In this presentation, results of tree-ring measurement with range of AD 1,650 to 1850 will be shown with the results of AD 1,250 to 1,650, which were published previously. The discrepancy from IntCal data are regarded as regional offset of Korea. The average offset during the first 400 years of the range, which is included in Little Ice Age, was apparently larger than the average over the last 200 years. One of the reasons of regional offset around Korea is thought to be contribution of 14C depleted CO2 released from northern Pacific Ocean where old deep water is upwelling to the surface. It is thought that the temperature change may affect on the releasing rate of 14C depleted CO2.

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S01-P-153

NOTE ON REPORTING OLD RADIOCARBON AGES AND THEIR CALIBRATION

NADEAU M.J., GRooTeS P.M.

christian-albrechts University in Kiel, KIel, GeRManY

AbstractThe basis of a radiocarbon date is the 14C content of a sample expressed in percent modern carbon and its Gaussian uncertainty. This is then converted into a conventional radiocarbon age, using what is known as Libby 14C half life, via a simple equation – Age = -ln (14C activity in pMC / 100) x 8033 (Stuiver and Pollack 1977). This conventional 14C age can then be calibrated using several programs written for this purpose, all using the current 14C calibration curve, Intcal 09, that translate a conventional 14C age into a “real” calendar age. The 14C conventional ages are often expressed with symmetrical positive and negative uncertainties, assuming that a linear approximation can be used to represent the logarithmic equation over the uncertainty range of the 14C. This, however, is not valid for older samples (or small samples with larger uncertainties) where this assumption is no longer correct. Nevertheless, old samples (> 30 ka BP) are often reported with symmetrical uncertainties, which is mathematically wrong. This mistake had fewer implications in the past, when the calibration curve was limited to 12.4 ka BP. With the extension of the calibration to 24 ka BP and 26 ka BP in Intcal 98 and Intcal 04, and then to 50 ka BP in Intcal 09, this misrepresentation of the conventional 14C ages uncertainty is propagated in the calibrated age range and can lead to significant errors in the assumed calibrated age range. We will discuss limits beyond which the linear assumptions cannot be used and show the effect of this misuse on both the conventional 14C age and the calibrated age probability distributions.

ReferencesStuiver ad Pollack (1977), Discussion: Reporting of 14C Data, Radiocarbon 19 (3) p. 355-363

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SESSION 5

STATISTICAL TOOLS

Convenersm. Blaauw (GBR), A. millard (GBR), m. Scott (GBR)

DescriptionStatistical tools are increasingly used to synthesize elements of radiocarbon science with other scientific information, for example:- chronological models incorporating stratigraphic and depositional processes- spatial modelling of radiocarbon measurements- statistical analysis for quality control- representations of laboratory processes- uses of calibration curve data for purposes other than calibration, e.g. palaeoclimate or forensic studies

This session will bring together this broad field of applications, to encourage discussion and cross-fertilisation.

Keywordsmodels, statistics, calibration, synthesis

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S05-P-154

DOES MULTIVERSE IDEA INFLUENCE THE INTERPRETATION OF RADIOCARBON DATES?

WALANUS A.

aGH University of Science and Technology, KRaKÓW, PolanD

AbstractThe radiocarbon method is straightforwardly connected to the quantum mechanic of the 14C nucleus. The absolutely indeterminate behaviour of this unstable nucleus, stored in the benzene vial, determines radiocarbon determination. (With AMS things go another way, although, the quantum engine, and the final result is the same.)May be that is a good reason to be interested in a high level philosophy such as the Hugh Everett’s many-worlds interpretation of quantum mechanics. Maybe the notion of the multiverse in the title is only a joke, but maybe only 95% so. Believing that 5% sometimes happens, let’s consider an easy, one year sample (cereal seed) of age T. The value of T is for ever unknown to us (as well as its 14C abundance in time of its charring in the neolithic fire and in the later time of its complete burning in the lab’s oven).Assuming T, the conventional radiocarbon age Tc is defined by the calibration curve with the precision, say ±15yr. Tc is an example of quantum mechanics observable. In our universe, we have got the measurement result Tc’ (±σ), however, in other universes the results are Tc’’, Tc’’’, and so on. We have Tc’±σ, however, we would have got Tc’’±σ. Let’s consider the two probability density functions of T, both obtained by the standard calibration procedure, albeit with the first radiocarbon date Tc’±σ and the second, for example Tc’+σ ±σ. Resulting density functions can differ considerably. This means that by random chance we would obtain deeply different results, in the sense of probability density functions as well as confidence interval. The question is, if the same uncertainty (described by σ) is not taken into account twice here. The multiverse idea was invoked here just for an easier grasp of some idea.The same sample dated for the second time will produce another result. Other calibrated probability density functions would be obtained with the probability governed by the normal distribution with the parameters: Tc (unknown) and σ (known). For the given T, all possible values of Tc’ may be considered, from the range, say Tc±3σ, with the step of 1yr, and with the statistical weight determined by the normal distribution Tc±σ. Some measure of the degree of difference between two calibrated densities may be defined and applied to the density functions obtained for radiocarbon determinations Tc’±σ and Tc±σ. Summing up the measures for all the accepted values of Tc’, gives the general measure, which tell us something about the additional uncertainty involved. The proposed measure, calculated for the all INTCAL09 ages T (50,050 - 50 yr b2k) gives another insight into the calibration curve.

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S05-P-155

VISUALIZATION OF THE RESOLUTION POWER OF THE RADIOCARBON METHOD

WALANUS A.(1), nalePKa D.(2)

(1) aGH University of Science and Technology, KRaKÓW, PolanD;(2) W. Szafer Institute of botany PaS, KRaKÓW, PolanD

AbstractIn the forensic applications of radiocarbon, as well as in the semi-forensic, historical ones, like for example that of the authentication of the Copernicus grove, the simple question may arise: would it be possible to distinguish two samples of a given expected ages? A similar question would be if it would be possible to check if the sample is of the age T1 or T2. The most striking example is the case of the bomb 14C, because of the one year resolution possibility from the one side, and the ten or twenty year ambiguity, from the other.However, the case of the time span 1400AD-1950AD, as defined by the Copernicus life time and possible contemporary forgery, is non trivial as well.The wiggle-type shape of the calibration curve is nothing new, however, to convince archaeologists/historians of its implications may be another subject of some relevance to the science.We propose a diagonally symmetrical map, with two (cal) time axis. Pixels of the map, which are of the size of the calibration curve resolution (5 yr for example), are coloured according to the power (1-b) of the statistical test of un-equality of ages. The power is calculated under the assumption of a test significance level (a) and date errors (σ). However, since σ and F-1(a) are inversely proportional in the b calculation formula (where F-1 denotes the inverse normal distribution function), the map colours definition can be recalculated to any of the three: a, b, σ, with two others taken as parameters. The σ=(σ1

2+ σ22)1/2, where σ1 and

σ2 are the errors of two samples compared (σ2 can be zero if the precise historical data is involved). The map is created for the full INTCAL 09 age range and beyond: 50,050 - 0 yr b2k.In parallel, we propose another visualization of the resolving power of the radiocarbon method. It has a form of a simple plot of a function of a probability versus the real sample age (cal). The plot is parametrized by the σ value. The probability plotted, which illustrates the resolution power, is defined by the relation of two hypothetical samples dated. For a given age T, the samples are assumed to have the true ages T1=T-σ and T2=T+σ, respectively. The question is if the radiocarbon dates (conv) will appear in the correct time order. The probability that T1 is less than T2, which is by no means 1 and is frequently below 0.5, give some measure of the resolving power of the method. Out of the calibration curve wiggles, assuming the absolute smoothness of the curve, the probability in question is equal to 0.92 (=F(21/2)). Wiggles make the probability of the correct samples age order instable, generally lower, although, sometimes much closer to 1 than 0.92 is. The age 570 b2k is a good positive example while at T=420 b2k, the probability of the correct order, for σ = 25, 50, and 100 yr, is equal to 0.4, 0.5, and 0.8 respectively.

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S05-P-156

WIGGLE MATCHING IN CALCULATION SPREADSHEET

KRAPIEC M., WalanUS a.

aGH University of Science and Technology, KRaKÓW, PolanD

AbstractWiggle matching is a simple idea with an almost equally simple calculation. In opposition to the advanced calibration programs it is possible to obtain comprehensible results with just one formula in a calculation spreadsheet, for example MS Excel. Visual Basic programming is not necessary here, however, a small VB code makes calculations comfortable. The VB code is short and clear and can be easily modified by a skilled student, if necessary. The most important thing seems to be that the form of the result, namely the plot of the sum of squares (or optionally chi-squared p-value), is as simple for management to do as Excel graphs are.The calibration curve stored in the spreadsheet is recalculated down to the yearly resolution (and is inversed upside down i.e. 50kyr is at the bottom). It makes the xls file 2.5MB large, which is of course not an issue for contemporary computers. Such an approach simplifies the wiggle-matching calculations. Assuming that the calibration curve is stored in the first columns (A - CAL BP, B - 14C age, C - Error), the formula for calculating the sum of squares is as follows: =(2690-b1)^2/(40^2+c1^2)+(2820-b38)^2/(60^2+c38^2)...It must be stressed that it is not the most comfortable method but the simplest one. There are two radiocarbon dates visible in the presented formula: 2690±40 and 2820±60, as well as the distance between them. The distance (assumed to be precise) is 37 yrs, and in the formula is used to address the proper position of the calibration data, the 14C age and Error (b38 and c38, in relation to b1 and c1). The formula can be extended to any number of samples. Staying within the spreadsheet (with no VB programming) it is possible to write a formula which creates the formula given above on the basis of the set of dates pasted into the spreadsheet.As an example of flexibility offered by the presented approach, the method of identification of incompatible dates may be given. Instead of summing up squares of differences, such as in the formula presented above, the components would be calculated separately and then totalled. Having the square of the difference plotted for each date enables it to identify the one that is inconsistent with the other dates.The plot of chi-squared p-value, obtained with the application of one additional function, make it relatively easy to simply read out the confidence interval of the final wiggle-matched date.The aforementioned functionality is available with the VB macro by button clicks. The macro comprises also the Monte Carlo simulation for the date reliability estimation, which is the kind of functionality which is behind the capability of the simple spreadsheet formulas. The main idea driving our proposition, however, is that of having calculations visible and explicit, what can be attained with the calculation spreadsheet.

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S05-P-157

BAYESIAN APPROACH OR ROBUST BAYESIAN ANALYSIS?

ZINK A.

c2RMf, PaRIS, fRance

AbstractThe Bayesian approach is widely used in radiocarbon dating and integrated within the most common softwares such as Bcal or OxCal (Bronk Ramsey, 2009). It is used primarily to reduce uncertainty of radiocarbon ages (likelihood) using additional information (prior). A major criticism of the Bayesian approach is the definition of the prior information and the conversion into mathematical forms, which strongly depend on the practitioners. The error made IIon the prior influences the final result (posterior).To minimize the uncertainty about the prior, a solution is the use of robust Bayesian analysis (Weninger et al., 2010). This method generalizes the Bayesian analysis by testing a variety of priors. It is close to probability bounds analysis, in particular the Dempster-Shafer theory, that use interval bounds as uncertainty about the parameters probability. These methods are particularly used in Risk analysis (Ferson and Hajagos, 2004) in which the aim is to estimates the maximum risk.In scientific reasoning, the aim is to test hypotheses. If we consider the prior as the hypothesis to be tested, the subjectivity of the prior is irrelevant (limited by our beliefs, our know-how or our knowledge, the assumptions are inherently subjective). The posterior deduced from the application of Bayes’ theorem to the prior is the logical result of the test We can therefore work with a single prior (classical Bayesian analysis) as long as it is explicit and therefore open to criticism.

References1. Bronk Ramsey C. (2009) Bayesian analysis of radiocarbon dates. Radiocarbon, 51, 337 - 3602. Ferson S., Hajagos J.G. (2004) Arithmetic with uncertain numbers: rigorous and (often) best possible answers.

Reliability engineering and system safety, 85, 135-1523. Weninger F., Steier P., Kutschera W., Wild E.M. (2010) Robust bayesian analysis, an attempt to improve

Bayesian sequencing. Radiocarbon, 52, 963-983

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S05-P-158

AGE-DEPTH MODEL CONSTRUCTION USING NONPARAMETRIC METHOD - A CASE STUDY FOR PELEOENVIRONMENTAL RECORDS DATED BY RADIOCARBON, U-SERIES AND LEAD 210PB

HERCMAN H., GaSIoRoWSKI M., PaWlaK J.

Institute of Geological Sciences, PaS, WaRSZaWa, PolanD

AbstractPaleoenvironmental reconstructions are visualization of particular indicator changes (‘major analysis’) as a depth function. Time information we obtain using isotopic dating methods, e.g. radiocarbon, U-series methods. Additionally, usually dating resolution (number of dated samples) is much lower than ‘major analysis’ samples. However, we need ages of ever sample. Than, age-depth estimation is a crucial step of paleoenvironmental reconstruction.We present a new system for chronology construction. It can be used for profiles that have been dated by different methods. As input data, the system uses the following basic measurements: activities, atomic ratios or age, as well as depth measurement. Based on probability distributions describing the measurement results, the system estimates the age~depth relation and its confidence bands. To avoid the use of difficult-to-meet assumptions, it uses nonparametric methods. We applied a Monte Carlo simulation to model age and depth values based on the real distribution of counted data (activities, atomic ratios, calibrated ages, depths etc.). Several fitting methods could be applied for estimating the relationships; based on several tests, we decide to use LOESS method (locally weighted scatterplot smoothing). The stratigraphic correction procedure applied in the system uses a probability calculus, which assumes that the ages of all the samples are correctly estimated. Information about the probability distribution of the samples’ ages is used to estimate the most probable sequence that is concordant according to the superposition rule.The method of model construction and its verification we will present using lake sediment and speleothems sequences dated by lead 210Pb, U-series and radiocarbon methods. The obtained model can be verified in two ways. The first one is to compare model with independend isotopic dating results. It will be present for the lake sediment core dated by 210Pb method with some radiocarbon datings and the speleothems profile dated by U-series and radiocarbon methods. The second method of model verification will deal with dam lake sediments of known age.

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S05-P-159

CLIMATE WAVELET SPECTRUM ESTIMATION UNDER CHRONOLOGY UNCERTAINTIES

LENOIR G., cRUcIfIX M.

Université catholique de louvain, loUVaIn-la-neUVe, belGIUM

AbstractSeveral approaches to estimate the chronology of palaeoclimate records exist in the literature: simple interpolation between the tie points, orbital tuning, alignment on other data... These techniques generate a single estimate of the chronology. More recently, statistical generators of chronologies have appeared (e.g. OXCAL, BCHRON) allowing the construction of thousands of chronologies given the tie points and their uncertainties. These latter are, for example, radiocarbon-dated layers in a core. These techniques are based on advanced statistical methods. They allow one to take into account the uncertainty of the timing of each climatic event recorded into the core.On the other hand, when interpreting the data, scientists often rely on time series analysis, and especially on spectral analysis. Given that paleo-data are composed of a large spectrum of frequencies, are non-stationary and are highly noisy, the continuous wavelet transform turns out to be a suitable tool to analyse them. The wavelet periodogram, in particular, is helpful to interpret visually the time-frequency behaviour of the data.Here, we combine statistical methods to generate chronologies with the power of continuous wavelet transform. Some interesting applications then come up: comparison of time-frequency patterns between two proxies (extracted from different cores), between a proxy and a statistical dynamical model, and statistical estimation of phase-lag between two filtered signals. All these applications consider explicitly the uncertainty in the chronology. The poster presents mathematical developments on the wavelet spectrum estimation under chronology uncertainties as well as some applications to radiocarbon-dated Quaternary data.

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S05-P-160

MODELLING THE AGE OF THE CAPE RIVA TEPHRA

LEE S.(1), bRonK RaMSeY c.(1), HaRDIMan M.(2)

(1) University of oxford, oXfoRD, UnITeD KInGDoM;(2) Royal Holloway, University of london, eGHaM, UnITeD KInGDoM

AbstractTephrochronology is an important tool for palaeochronology and climate reconstruction. Tephra provides independent, physical links between different records. It can also be used as a dating tool. Radiocarbon acts as an indirect dating method for estimating the ages of tephra when direct dating is not possible. Recent advances in Bayesian age-depth modelling have greatly enhanced our ability to produce high-precision stratigraphic models.This poster presents a modelled age of the tephra from the Cape Riva eruption of Santorini. This tephra has been found across the Eastern Mediterranean and presents an important link between different marine and terrestrial records. A robust age of the tephra is obtained using a Poisson process model together with a model averaging technique (Bronk Ramsey, this session) and by cross-linking two terrestrial records from the literature, from Lesvos Island (Margari, 2009) and Tenaghi Philippon (Müller et al, 2011), Greece.

References1. Margari, V., Gibbard, P. L., Bryant, C. L., and Tzedakis, P. C. (2009) Character of vegetational and environmental

changes in southern Europe during the last glacial period; evidence from Lesvos Island, Greece. QSR 28, 1317-1339

2. Müller, U. C., Pross, J., Tzedakis, P. C., Gamble, C., Kotthoff, U., Schmiedl, G., Wulf, S. and Christanis, K. (2011) The role of climate in the spread of modern human into Europe. QSR 30, 273-279

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S05-P-161

RADIOCARBON DATING AND AGE-DEPTH MODEL FOR LAMINATED LAKE SEDIMENTS FROM LAKE SZURPILY, NE POLAND

PIOTROWSKA N.(1), TYlMann W.(2), KInDeR M.(2), enTeRS D.(3)

(1) Silesian University of Technology, Institute of Physics, GaDaM centre of excellence, GlIWIce, PolanD;(2) University of Gdansk, Institute of Geography, GDanSK, PolanD;(3) University of bremen, GeoPolaR Institute of Geography, bReMen, GeRManY

AbstractIn the framework of NORPOLAR (Northern Polish Lake Research), interdisciplinary research on laminated sediments from four northern Polish lakes is carried out. These paleolimnological studies will provide new high-resolution data of climatic and environmental changes in this part of Europe. The dating of sediment cores performed so far indicates, that three records retrieved cover the time span of entire Holocene up to the present time, and one of them from ca. 9500calBP.One of the investigated lakes is Lake Szurpily, located in the NE edge of the Polish territory in the Suwalki Lakeland (54°13’40’’N, 22°53’35’’E). The landscape of this area was shaped by the retreating ice sheet, which formed, among others, numerous lakes, moraine and kame hills. Lake Szurpily covers 0.89km2, has a well-developed coastline, and the point of maximum depth (46.8m) was chosen as a coring location.The recovered sediment core was subjected to palynological analysis, which allowed reconstruction of the land cover changes in the lake surroundings, as well as the human influence and development of aquatic plants. The diatom analysis resulted in the reconstruction of lake level, trophy and pH changes. The geochemical measurements have also been performed with use of X-ray Fluorescence, andthe stable isotope analyses are being carried out.Radiocarbon dating has been performed for macrofossils of the terrestrial origin collected from sediment material and identified botanically, e.g. fragments of leaves, pine epidermis and needles. In total 20 AMS measurements have been completed, mainly in frame of the running project «Modelling of calendar timescales for laminated lake sediments in Northern Poland as a basis for high-resolution palaeoenvironmental reconstructions» funded by Polish Ministry of Science and Higher Education (no. NN306291639). The complete and comprehensive interpretation of the results requires a robust calendar timescale to be reconstructed for investigated sediment core. The final age-depth models will be based on various dating methods, taking into account the assumptions, limitations and uncertainties of each method. Varve counting is being performed for laminated sections of the core. The isotopic methods 210Pb and 137Cs will provide additional age control for uppermost parts.The presentation will focus on the radiocarbon dataset, which will be used in age-depth modelling. The one evident and some more possible outliers will be discussed taking into account the probable reasons for their occurrence. Finally, the age-depth model obtained with use of the varve chronology data to estimate the interval between the 14C dated levels, where possible, will be presented. This model will be discussed and compared with the model constructed solely on radiocarbon dates with assumed stratigraphical order.

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S05-P-162

A CELTIC GUITAR ON SKYE? THE USE OF RADIOCARBON DATING AND BAYESIAN ANALYSIS TO PRODUCE A ROBUST AND REFINED DATE ESTIMATE FOR THE EARLIEST-KNOWN MUSICAL INSTRUMENT FRAGMENT IN BRITAIN

HAMILTON D.(1), bIRcH S.(2), cooK G.(1), laWSon G.(3)

(1) University of Glasgow, eaST KIlbRIDe, UnITeD KInGDoM;(2) West coast archaeological Services, cRoMaRTHY, UnITeD KInGDoM;(3) University of cambridge, caMbRIDGe, UnITeD KInGDoM

AbstractIn archaeology, the combination of radiocarbon dating and Bayesian analysis into complex chronological models is often associated with the investigation of the chronology of a specific site, or the currency of a type of material culture. The objective is usually to produce date estimates for ‘events’ that cannot be directly dated - e.g. the construction of a structure, the digging of a ditch, the introduction of a pottery type. Only in rare cases does the modelling also strive to produce a highly precise date estimate for a specific context.Here we use the information derived from modelling a suite of radiocarbon dates from the area within and lying immediately outside of the Iron Age site at High Pasture Cave, Isle of Skye, Scotland, to provide a robust date estimate for the deposition of a charred wooden bridge piece from a prehistoric stringed instrument. Destructive direct dating of the object was discouraged given its cultural significance. But, more importantly, any date on the bridge piece would almost certainly suffer from an ‘old wood’ offset of unknown age.To overcome the difficulty of directly dating the object, the context from which the instrument fragment had been recovered was incorporated into the full dating programme. Not only did this provide a method to date the object, but also provided a date estimate that was significantly more precise than had a high-precision date on the object been possible. The results of the Bayesian modelling estimate that the specific context was formed in the second half of the 4th century cal BC.

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S05-P-163

IS A TRAPEZIUM JUST A DISTORTED RECTANGLE? THE CHRONOLOGICAL MODELLING OF BEAKERS IN BRITAIN USING DIFFERENTLY SHAPED PRIOR DISTRIBUTIONS

MARSHALL P.(1), HaMIlTon D.(2), PaRKeR PeaRSon M.(3), JaY M.(3)

(1) english Heritage, lonDon, UnITeD KInGDoM;(2) University of Glasgow, eaST KIlbRIDe, UnITeD KInGDoM;(3) University of Sheffield, SHeffIelD, UnITeD KInGDoM

AbstractFor two centuries archaeologists have been debating the identity of the ‘Beaker folk’: Were they prehistoric immigrants to Britain or indigenous consumers of a developed ‘Beaker package’? The Beaker People Project has analysed nearly 350 individuals ranging geographically from the north of mainland Scotland to the Wessex heartland of southern England. Radiocarbon dating has been undertaken on nearly 200 individuals, and allows us to better understand the chronology of Beakers.The application of the ‘uniform distribution’ prior, when constructing Bayesian models of archaeological data, has been shown over the past two decades to be relatively robust. However, the use of a uniform distribution to model the currency of material culture, such as Beakers, is far from ideal. This is especially so if we envisage a scenario in which Beakers originate at a given time in a given place, are gradually produced in greater numbers over time, and then decrease as popularity wanes (akin to notions of ‘introduction, blooming and decline’). Trapezium-shaped prior distributions have recently been used to model the gradual introduction and demise of archaeological phases but, until now, have not been routinely available. We explore what differences the use of these two different priors makes to our understanding of the chronology of Beakers in Britain. We also question whether, without understanding the actual distribution for the use of Beakers, it is possible that assumptions such as a trapezium-shaped prior could simply distort the picture.

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S05-P-164

BAYESIAN APPROACH TO 14C DATES IN ESTIMATION OF LONG-TERM ARCHAEOLOGICALSEqUENCES IN ARID ENVIRONMENT.THE HOLOCENE SITE OF TAKARKORI ROCK SHELTER, SW LIBYA.

CHERKINSKY A.(1), bIaGeTTI S.(2), DI leRnIa S.(2)

(1) University of Georgia, aTHenS, UnITeD STaTeS;(2) Dipartimento di Scienze dell’antichita. Sapienza, Universita di Roma, RoMa, ITalY

AbstractCaves and rock shelter are critical loci for the analysis and understanding of human trajectories in the past. Use and re-uses of the same context, however, might have had serious impacts on depositional aspects. This is particularly true for the archaeological filling of desert environment, such as the central Sahara, where most of the deposits are the loose rich with organic sand. Besides traditional stratigraphic reconstructions and detailed study of the material culture, radiocarbon measures from different contexts run on several types of material (bone, dried and charred coprolite, uncharred and charred plant remains, etc) can highlight intrinsic critical aspects of 14C determinations. These must be carefully evaluated to veritably enhance the chronological assessment of the life history of the site. We present here the statistical of the set of about 50 radiocarbon measures from the site of Takarkori, SW Libya, where early Holocene foragers and then groups of cattle herders inhabited the area from ca 10200 to 4600 years BP.We have used BCal Bayesianradiocarbon calibration program designed for statistical presentation of the calibrated data and estimation of their probability for the different phases. The Takarkori rock shelter was occupied during four phases of the following cultures: Late Acacus from 10170 to 8180 years BP; Early Pastoral, 8180-6890 years BP; Middle Pastoral, 7160-5610 years BP; and Late Pastoral, 5700-4650 years BP.

References1. http://bcal.sheffield.ac.uk and also cite the paper that launched the service:2. Buck C.E., Christen J.A. and James G.N. (1999). BCal: an online Bayesian radiocarbon calibration tool.

Internet archaeology, (http://intarch.ac.uk/journal/issue7/buck/).

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S05-P-165

IMPROVING AND TESTING THE REPEATABILITY OF C-14 AMS MEASUREMENTS

ZONDERVAN A.(1), KaISeR J.(1), WeST J.(1), TURnbUll J.(1), bRaIlSfoRD G.(2), MoSS R.(2)

(1) GnS Science, loWeR HUTT, neW ZealanD;(2) national Institute of Water and atmospheric Research (nIWa), WellInGTon, neW ZealanD

AbstractAs AMS techniques and systems continue to advance, C-14 applications target ever more subtle radiocarbon signals. One such application is the use of atmospheric 14CO2 as a tracer for CO2 fluxes between ocean, atmosphere, and biosphere reservoirs. We have started a project to replicate parts of and extend the atmospheric 14CO2 record from Baring Head, New Zealand, through best possible AMS measurements, using state-of-the-art equipment and quality control procedures. The World Meteorological Organisation (WMO - Global Atmospheric Watch) has set a long-term goal for inter-laboratory comparability in D14C in atmospheric CO2 equal to 1‰. We support the pursuit of this goal through study of how errors in AMS observations arise and how they should be handled in quantifying final uncertainties and confidence intervals.In this presentation, we discuss (I) the limited validity of some assumptions and practices in reducing C-14 AMS measurement data, (II) our present method of dealing with the largest source of non-Poisson error, imperfect cathode-to-cathode repeatability, (III) its connection to the finite scope of correcting for isotopic fractionation in sample graphitization, AMS ion source, and beam transport, and (IV) early results suggesting an overall repeatability of ≈ 1.5‰ in D14C.

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371

S05-P-166

COMPLEX STATISTICAL MODEL OF THE LAKE SOPPENSEE CHRONOLOGY

MICHCZYNSKI A.(1), HaJDaS I.(2)

(1) Institute of Physics, Silesian University of Technology, GlIWIce, PolanD;(2) Ion beam Physics, eTH, ZÜRIcH, SWITZeRlanD

AbstractThis study presents new complex statistical model of the Lake Soppensee chronology, which joins two types of accessible chronological information together.The first type of information is represented by the varve chronology constructed for laminated part of Soppensee sediment (depth 540 - 360 cm) and fitted to the IntCal09 radiocarbon calibration curve. The second type of information is represented by radiocarbon dates obtained for non-laminated or partially laminated parts of the sediment. These dates have been used for construction of age-depth model. This complex statistical model makes a supplement of our previous work published in Radiocarbon, where chronologies constructed on a base of these two types of information separately were compared (Hajdas, Michczynski 2010).The complex statistical model of the Lake Soppensee chronology has been constructed using OxCal 4.1 program. The model consists of three parts included in Sequence function. The main part is the varve chronology, which is fitted to the IntCal09 using OxCal wiggle-matching function D_Sequence on a base of 54 radiocarbon dates. Two remaining parts concern time periods before and after accumulation of laminated sediment. They are constructed using OxCal age-depth model function P_Sequence with k parameter equal to 3 (1/cm). These three parts are separated by OxCal boundary commands. Additional Boundary command is included inside P_Sequence function, which describes age-depth relationships for lower part of the sediment, and points a borderline between non-laminated and partially laminated part of the sediment.Important element of the present work is discussion of appropriate threshold value of the overall agreement index. Because in a model constructed using wiggle-matching function D_Sequence is only one independent parameter, the threshold value of the overall agreement index depends on a number of dates included in the model (Bronk Ramsey et al. 2001). The complex model, which includes both D_Sequence and P_Sequence functions, needs special estimation of the threshold value. In this case the threshold value of the overall agreement index should be lower than 60% or overall agreement index of the model should be appropriately recalculated.Presented model confirms our previous conclusions that depositional conditions of the lake Soppensee were rather stable during the early Holocene and allows to make precise dating of chronological events.

References1. Bronk Ramsey C., Van Der Plicht J., Weninger B. 2001. «Wiggle Matching» Radiocarbon Dates. Radiocarbon

43 (2; PART A): 381-390.2. Hajdas I., A. Michczyński. 2010. Age-Depth Model of Lake Soppensee (Switzerland) Based on the High-

Resolution 14C Chronology Compared with Varve Chronology. Radiocarbon 52 (3): 1027-1040

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S05-P-167

TO SUM, OR NOT TO SUM: THAT IS THE qUESTION

MICHCZYNSKI A.

Institute of Physics, Silesian University of Technology, GlIWIce, PolanD

AbstractThe problem how to estimate a time interval of an archeological or geological phase using a group of radiocarbon dates assigned to this phase is typical problem, which must be often solved when a chronology of an investigated site is constructed. In nineties there was widely used the method, which creates a summed probability density distribution of a phase by summing individual distributions of the calibrated dates of samples, which represent this phase. The interquartile range (Aitchison et al. 1991) or the highest probability confidence intervals of this summed distribution are usually interpreted as the time limits of the phase. This method is also implemented to OxCal program by the Sum command of the Chronological Query Language. However this method was then criticized as based on unclear statistical basis. Instead of this a calculation of the start and end of the phase using the OxCal boundary command was proposed. This poster presents comparison of the results obtained by the both methods for a case study of the Wolin settlement, located at the Polish Western Pomerania. It shows quite good agreement of these results.

ReferencesAitchison T, Ottaway B, Al-Ruzaiza AS. 1991. Summarizing a group of 14C dates on the historical time scale: with a worked example from the Late Neolithic of Bavaria. antiquity 65(246):108-16

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SESSION 6

VARIATIONS IN RADIOCARBON RESERVOIR EFFECTS

ConvenersW. Beck (USA), Q. Hua (AUS), G. Quarta (ITA), G. Siani (FRA)

DescriptionContributions are welcome on the investigation of radiocarbon reservoir effects and their temporal variations over the past 50 ka for various materials including marine and coastal (estuarine, lagoonal) samples, speleothems, terrestrial shells, lake sediments, and freshwater plants and shells. This investigation is not only important for improving the radiocarbon dating method but also gives useful information on climatic and environmental changes and the carbon cycle (ie, ocean circulation changes associated with climate change, and soil-to-speleothem carbon transfer dynamics through the cave system). Modelling studies of temporal variations in the reservoir effects associated with changes in climatic and/or environmental factors (ie, trace elements and stable isotopes) are also encouraged.

KeywordsRadiocarbon reservoir effect, speleothem dead carbon fraction, marine reservoir ages, hard-water effect, climatic and environmental changes.

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S06-P-168

CONSTRUCTING CHRONOLOGIES FOR MARINE RECORDS DURING MIS3 - NEW 14C DATA FROM THE FAROE-SHETLAND CHANNEL, NORTH ATLANTIC

OLSEN J.(1)(2), RaSMUSSen T.l.(3), ReIMeR P.J.(2)

(1) aarhus University, aaRHUS, DenMaRK;(2) Queen’s University belfast, belfaST, UnITeD KInGDoM;(3) University of Tromsø, TRoMSØ, noRWaY

AbstractIn the Greenland ice cores the last glacial period is characterised by millennial-scale Dansgaard-Oeschger (D-O) events of warmer and colder climates. Similar millennial-scale variability (linked to D-O events) is evident from oceanic cores suggesting a strong coupling of the atmospheric and oceanic circulations system. Cooling and sinking of dense saline water originating from the North Atlantic Drift current in the Norwegian-Greenland Sea is essential for the formation of North Atlantic Deep Water. The convection in the Norwegian-Greenland Sea allows for a northward heat exchange and southward transport of cold saline water. This circulation system is highly sensitive to climate change and has been shown to operate in different modes. The different oceanic circulation modes further have a large influence on the carbon exchange between atmosphere and the deep ocean. Such reorganisations of the North Atlantic circulation system and deep water formation cause changes in the 14 C activity of the surface ocean. Here we present 77 new AMS 14 C dates of planktonic foraminifera covering Marine Isotope Stage 3 from the LINK15 core taken from the Faroe-Shetland channel. The Faroe-Shetland channel is situated in the main path of the warm North Atlantic Drift current and further provides an escape route for the cold Norwegian Sea Deep Water. Hence LINK15 has an ideal position for studying paleo variability of 14 C reservoir ages. Based on N. pachyderma δ18O and IRD the LINK15 sediment core has been correlated to the NGRIP ice core (GICC05age scale). Further tie-points to NGRIP are provided by identification of the Vedde, Fugloyarbanki and FMAS-III tephra layers. The correlated GICC05 ages of the LINK15 sediment core are then used to calculate marine reservoir ages (DR) using the marine radiocarbon calibration curve (Marine09). Our results show significant DR variability through the course of 6 D-O events.

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S06-P-169

HYDROLOGICAL CONTROL ON THE DEAD-CARBON CONTENT OF A HOLOCENE TROPICAL SPELEOTHEM

GRIFFITHS M.L.(1), foHlMeISTeR J.(2), DRYSDale R.n.(3), HUa Q.(4), JoHnSon K.R.(1), HellSTRoM J.c.(5), GaGan M.K.(6), ZHao J.X.(7)

(1) Department of earth System Science, University of california, IRVIne, UnITeD STaTeS;(2) Heidelberg acedemy of Sciences, HeIDelbeRG, GeRManY;(3) School of land and environment, The University of Melbourne, PaRKVIlle, aUSTRalIa;(4) australian nuclear Science and Technology organisation (anSTo), KIRRaWee Dc, aUSTRalIa;(5) School of earth Sciences, The University of Melbourne, PaRKVIlle, aUSTRalIa;(6) Research School of earth Sciences, The australian national University, canbeRRa, aUSTRalIa;(7) centre for Microscopy and Microanalysis, The University of Queensland, bRISbane, aUSTRalIa

AbstractOver the past decade, a number of speleothem studies have used radiocarbon dating to address a range of palaeoclimate problems. These have included the use of the bomb pulse to anchor chronologies over the last 60 years, the combining of U/Th and radiocarbon measurements to improve the radiocarbon calibration curve, and linking atmospheric radiocarbon variations with climate changes. An issue with a number of these studies is how to constrain, or interpret variations in, the amount of radioactively dead carbon (i.e. the dead carbon fraction, or DCF) that contributes to speleothem radiocarbon values. In this study, we use radiocarbon measurements, stable-isotope and trace-element geochemistry, and U/Th ages from a previously studied speleothem from Flores, Indonesia, to examine DCF variations and their relationship with above-cave climate over the late Holocene and modern era.A strong association between the DCF and other hydrologically-controlled proxy data is observed for the late Holocene and instrumental periods, suggesting that more dead carbon was being delivered to the speleothem during periods of higher cave recharge (i.e. lower δ18O, δ13C and Mg/Ca values) and hence a stronger summer monsoon. To explore this relationship in more detail, we used a geochemical soil-karst model coupled with 14C measurements through the bomb pulse, to disentangle the dominant components governing DCF variability in our speleothem. We find that the DCF is primarily controlled by limestone dissolution associated with changes in open- versus closed-system conditions, rather than kinetic fractionation and/or variations in the age spectrum of soil organic matter above the cave. Therefore, we infer that periods of higher (lower) rainfall resulted in a higher (lower) DCF because the system was in a more closed (open) state, which inhibited (promoted) C isotope exchange between the karst-water DIC and soil-gas CO2, and ultimately led to a higher (lower) contribution of dead-carbon sourced from the bedrock.

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S06-P-170

VARIATIONS IN MARINE RESERVOIR EFFECT FOR THE SOUTH-WESTERN PACIFIC DURING THE HOLOCENE

HUA Q.(1), Webb G.(2), ZHao J.X.(3), noTHDURfT l.(4), PRIce G.(2)

(1) australian nuclear Science and Technology organisation (anSTo), KIRRaWee Dc, aUSTRalIa;(2) School of earth Sciences, University of Queensland, bRISbane, aUSTRalIa;(3) Radiogenic Isotope laboratory, centre for Microscopy and Microanalysis, University of Queensland, bRISbane,

aUSTRalIa;(4) School of earth, environmental and biological Sciences, Queensland University of Technology, bRISbane, aUSTRalIa

AbstractWe have recently investigated possible variability in the marine reservoir effect for the SW Pacific Ocean during the last 8000 years. This study aims to get a better understanding of ocean circulation changes associated with climate change during the study interval and to improve radiocarbon dating of marine samples. Coral samples used in this study were from shallow cores and storm derived blocks collected on Heron Reef (23º26’S, 151º55’E) in southern Great Barrier Reef and Moreton Bay (27º36’S, 154º40’E) in southern Queensland, Australia. Surface waters at the two study sites are mainly derived from the East Australian Current, which originates from the southern branch of the South Equatorial Current. A total of thirty five unaltered coral samples (based on SEM screening, δ234U and initial 230Th/232Th ratios) were analysed for 230Th/U and 14 C. 230Th dates, which reflect the absolute ages of the corals, were determined by TIMS U-series in the Radiogenic Isotope Laboratory at the University of Queensland with a precision better than 0.5% (2σ). Sub-samples of these dated corals were then taken for radiocarbon analysis. The samples were cut by diamond saw, cleaned in deionised water, oven dried, and homogenised in a mortar and pestle prior to 14 C analysis using the STAR AMS facility at ANSTO. A typical precision for AMS 14 C analysis is <0.4% (1σ). For most of the time, marine reservoir ages of Heron Reef agree well with those of Moreton Bay. The results of this investigation will be compared with the marine reservoir ages previously published for the Pacific, and variations in the marine reservoir effect for the SW Pacific during the Holocene and their possible mechanisms will then be discussed.This work was supported by AINSE grants 09/056, 10/076 and 11/104, and ARC Discovery grant DP1096184.

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377

S06-P-171

SPATIAL AND TEMPORAL VARIABILITY OF THE OLD CARBON EFFECT IN LACUSTRINE SEDIMENTS IN A COLD CLIMATE ZONE, NORTHWEST TERRITORIES (CANADA)

CRANN C.A.(1), PaTTeRSon R.T.(1), ReIMeR P.J.(2), GRIffITH f.(3)

(1) carleton University, oTTaWa, canaDa;(2) Queen’s University belfast, belfaST, IRelanD;(3) University of ottawa, oTTaWa, canaDa

AbstractClimate variability along the 600 km long Tibbitt to Contwoyto Winter Road in central Northwest Territories is poorly understood. With truck traffic projected to increase significantly it is critical that planners and mine developers have reasonable data on the future viability of the road, as alternate transportation costs (e.g. air transport) are prohibitively high. The research presented here is part of a paleoclimate study based on analysis of multiple proxy data derived from freeze cores in lakes along the TCWR, subsampled at very high resolution (mm-scale) using a freeze-core microtome. For accurate determination of the trends and cycles influencing climate in the region it is critical that age models with exceptional precision and accuracy be derived. Complicating the work is a requirement to correct for a highly variable old carbon effect across the region. Thus far, 10-lake sediment freeze cores have been AMS dated at the 14 CHRONO Centre, with 4-17 14 C measurements per core depending on the length (0.5 - 2 m) and quality of the core. Due to the absence of macrofossils, bulk sediments were used for dating. The age models produced in OxCal are internally consistent with realistic sedimentation rates (mm/yr) and few age reversals. However, projected surface ages are rarely close to modern and show high variability (hundreds to thousands of years) from lake to lake. As the sediment-water interface is captured by in situ freezing, this effect is not an artifact of over-penetration during coring. We correct for the old carbon effect on a lake-by-lake basis, but it is unclear whether the correction factor should vary temporally due to the lack of macrofossils for paired dating. To shed light on this concern, we first characterize the spatial variability of the lakes based on:

(A) regional factors such as quaternary and bedrock geology, topography, presence/absence of inlets/outlets, tree line, permafrost, ground cover; and

(B) local factors such as lake shape and size, water depth, sediment properties (geochemistry, grain size, loss on ignition, microfossils, isotopes), and water properties (DIC/DOC, isotopes, geochemistry).

We then characterize the temporal variation in the cores. Seven cores are homogeneous in appearance and age models give no indication that there has been a change in the old carbon effect during Holocene deposition. Three cores show an abrupt shift in sedimentation from lower organic content (OC), coarser grained, grey-green colored sediment to higher OC, finer grained, green colored sediment. This transition in sedimentation occurs at 3,500 cal. yr BP for P26, yet there is no shift in the age model. P34 and P52 show a transition in sedimentation at 6,500 cal. yr BP corresponding to a shift in the age models. Preliminary C/N isotopic data from P34 suggests that there was a very sudden rise of lake levels at ~6500 cal. yr BP and therefore the shift in the age model is most likely due to increased sedimentation rate.

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378

S06-P-172

FRESHWATER RESERVOIR EFFECTS AT MININO, A MESOLITHIC-FOREST NEOLITHIC BURIAL GROUND IN NORTHWESTERN RUSSIA

WOOD R.(1)(2), HIGHaM T.(2), bUZHIloVa a.(3), SUVoRoV a.(4)

(1) australian national University, canbeRRa, aUSTRalIa;(2) University of oxford, oXfoRD, UnITeD KInGDoM;(3) Russian academy of Sciences, MoScoW, RUSSIan feDeRaTIon;(4) Vologda State Museum, VoloGDa, RUSSIan feDeRaTIon

AbstractA hunter-fisher-gatherer lifestyle flourished in northwestern Russia from the early Holocene until the end of the prehistoric period. The earliest of these groups, the Mesolithic and Forest Neolithic, show considerable social, economic and cultural variability. For instance, their burial grounds contain 10s of inhumations with grave goods such as pendants, tools and animal effigies. Variation between burials is startling: some individuals are buried with 200 pendants whilst others have no grave goods. Establishing whether these differences are due to change over time or to variation within one or more groups of contemporary people is key to their interpretation. Burial grounds have little stratigraphy, and so it is imperative that individual inhumations are directly dated. Unfortunately, the input of freshwater resources into the diet introduces a significant reservoir effect. This paper will examine the size of this offset and compare it to stable isotope data. It shows that the size of the reservoir offset is unrelated to stable isotope values.

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379

S06-P-173

GEOCHRONOLOGICAL LIMITATIONS FOR INTERPRETING THE PALEOCLIMATIC HISTORY OF THE TIBETAN PLATEAU

HOU J.(1), D’anDRea W.J.(2), lIU Z.(3)

(1) Institute of Tibetan Plateau Research, chinese academy of Sciences, beIJInG, cHIna;(2) lamont Doherty earth observatory, columbia University, PalISaDeS, nY, UnITeD STaTeS;(3) Department of earth Sciences, The University of Hong Kong, HonG KonG, cHIna

AbstractThe Tibetan Plateau is often referred to as the earth’s third Pole, due to its great elevation, massive size, large quantities of terrestrial ice and its impact on Northern Hemisphere weather patterns. Concern surrounding the impact of anthropogenic global warming on the ice fields of the Tibetan Plateau and the need for accurate projections of future climate have reinvigorated interest in understanding the dynamics that control the climate of the TP. Present day climate on the Tibetan Plateau is chiefly influenced by the East Asian Monsoon, the Indian Monsoon and the circulation of the mid-latitude Westerlies. Despite the large number of paleoclimate records from the region, the spatial patterns of past changes in Tibetan Plateau climate and the associated forcing mechanisms remain poorly understood. Existing paleoclimate records from ice cores, speleothems and tree rings provide a framework for examining past climate dynamics on the TP, but with limited geographical coverage. Lake sediments offer opportunities for higher spatial resolution of paleoclimate records, but inaccuracy of radiocarbon-based age models of sediment accumulation represents a fundamental restriction on the utility of lake-based paleoclimate records. Wehavereviewedthe techniques used to estimate reservoir ages of lake sediments from the Tibetan Plateau. We compile the published reservoir ages determined for Tibetan Plateau lakes, examine their spatial and temporal patterns, and assess their chronological uncertainties. We use two case studies (Bangong Co and Lake Qinghai) to demonstrate that uncertainties in reservoir ages allow equally probable and contrasting interpretations of paleoclimate records from the Tibetan Plateau. More well-dated, high-resolution, quantitative lacustrine records are needed to confidently interpret the mechanisms for the past climate variability on the Tibetan Plateau and we recommend that the full impacts of chronological uncertainty be considered when interpreting existing lake-based paleoclimate records.

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S06-P-174

PLANKTIC FORAM DATES FROM THE INDONESIAN ARC: MARINE RESERVOIR AGE CORRECTIONS AND A VOLCANIC ERUPTION THAT WASN’T

SOUTHON J.(1), MoHTaDI M.(2), De Pol-HolZ R.(3)

(1) University of california, IRVIne ca 92697-3100, UnITeD STaTeS;(2) MaRUM, University of bremen, leobeneR STR. 28359 bReMen, GeRManY;(3) Department of oceanography, Universidad de concepcion, VIcToR laMaS 1290, concePcIon, cHIle

AbstractThe Indonesian Arc extends 6000 km from the Andaman Islands in the Bay or Bengal to the Banda Sea south of western New Guinea, and was formed by the subduction of the Indian-Australian plate beneath Asia. Marine sediment records from the south side of the arc monitor the state of the Indonesian Throughflow, a critical choke point in the surface return path of the Global Conveyor circulation. They also record the effects of catastrophic subduction-related earthquakes and volcanic eruptions, and are therefore of interest to paleoceanographers, tectonicists, and paleoseismologists alike.Here we present regional marine 14 C reservoir ages determined from 14 C dates on planktic forams, using tephra layers from well dated volcanic eruptions as time markers. Gravity cores GeoB 10042-1 and 10043-3, were recovered on the 2005 SO184 cruise of the German R/V Sonne, from a location southwest of the Sunda Strait separating Java and Sumatra. GeoB 10065-7 was collected between Sumba and Sumbawa in the Lesser Sunda Islands east of Java, on the same cruise. Picked samples of planktic forams associated with prominent ash layers from the Krakatau (1883) and Tambora (1815) eruptions yielded radiocarbon ages of 500-700 years for samples of surface-dwelling G.ruber and G.sacculifer. Ages for mixed planktic assemblages containing some upper thermocline species are typically 0 to 200 years older. These results correspond to regional reservoir age corrections (ΔR values) of about +150 years for ruber/sacculifer and +250 year for mixed planktics. The positive ΔR values, and the higher corrections for mixed samples, are consistent with monsoon-driven upwelling of 14 C-depleted subsurface water off Java and Sumatra (Susanto et al., 2001) and its subsequent east-west transport by the seasonally reversing South Java Current.Prior to 1883, GeoB 10043-3 presents an unbroken sequence of sediment for at least 2000 years, providing an opportunity to test for the presence of tephra from a proposed very large 536 AD eruption of Krakatau. It is claimed (Keys, 1999) that this was the source of a historically documented dust veil event (Stothers, 1984) with subsequent cooling similar to, but far more severe than, the 1816 «year without a summer» following the Tambora eruption. Although GeoB 10043-3 contains abundant ash from the 1883 Krakatau eruption, there is no evidence for a 536 AD event, which supposedly involved tephra volumes 20-50 times larger. Since ash from very large eruptions is widely distributed about the source vent regardless of wind direction, we conclude that the catastrophic 536 AD Krakatau eruption is a myth.

References1. Keys, D. 1999. Catastrophe: an Investigation into the Origins of the Modern World. Ballantine, New York.2. Stothers, R.B., 1984. Mystery cloud of 536 AD. Nature 307: 344-3453. Susanto, R.D., Gordon, R.L., Zheng, Q. 2001. Upwelling along the coasts of Java and Sumatra and its relation

to ENSO. Geophysical Research Letters 28, 1599-1602

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381

S06-P-175

VARIABILITY IN THE MARINE RADIOCARBON RESERVOIR EFFECT IN MUSCAT (SULTANATE OF OMAN) DURING THE 4TH MILLENNIUM BC: REFLECTION OF TAPHONOMY OR ENVIRONMENT?

ZAZZO A.(1), MUnoZ o.(2), SalIÈGe J.f.(1), MoReaU c.(3)

(1) UMR 7209 cnRS / MnHn, PaRIS, fRance;(2) UMR 7041 cnRS / Univ Paris I, nanTeRRe, fRance;(3) UMS 2572 cea/Saclay, GIf SUR YVeTTe, fRance

AbstractRadiocarbon (14 C) dating of archaeological coastal sites in arid areas is challenging because of the relative rarity of datable terrestrial artefacts. Marine artefacts provide an abundant source of carbon, which is technically easy to date but radiocarbon dates need to be corrected for local variations from the global average marine 14C reservoir age (DR). In archaeological sites, this is usually done by the comparison of the 14C age measured between coeval pairs of terrestrial and marine samples that have no inbuilt age. Here, we present the results of a study that aims to determine the local 14C marine reservoir effect (MRE) along the Eastern coast of the Arabic Peninsula during the 4th millennium BC, a period of important cultural, demographic and social changes in this region. Previous estimates of the MRE based on associated shells and charcoal vary by about 400 14C yr and this is a serious limitation to the establishment of a precise chronology in the area based on marine material. In order to maximize the chances to obtain contemporaneous terrestrial-marine pairs for a new assessment of the MRE in this region we dated charcoal, shells, fish and turtle bones as well as human bones found in three recently and carefully excavated graves from the site of Ra’s al-Hamra RH5. A large variability was found between charcoals (up to 240 14C yr) and marine specimens (up to 785 14C yr) present in the same grave. This variability was attributed to inbuilt ages, diagenesis and possibly environmental factors although taphonomic processes cannot be excluded. We discarded the oldest charcoals and used the 14C ages obtained on human apatite as a cut-off value to remove the marine outliers. Two out of the three graves provided terrestrial and marine assemblages which did not differ statistically and were used to calculate an average MRE of 645±40 14C yr (DR= 255±55 14C yr). This value is consistent with previous estimates based on the 14C dating of marine sediments off Pakistan and suggests stability of the MRE in the Arabian Sea since the 4th millennium BC.

ReferencesZazzo A., Munoz O., Saliège J.-F., Moreau C. (2012). Variability in the marine radiocarbon reservoir effect in Muscat (Sultanate of Oman) during the 4th millennium BC: reflection of taphonomy or environment? Journal of Archaeological Science (in press).

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S06-P-176

IDENTIFICATION OF MARINE RESERVOIR VARIATION IN ARCHAEO-LOGICAL SHELLFISH REMAINS FROM AN OPEN COASTLINE, PAPUA NEW GUINEA

PETCHEY F.(1), UlM S.(2), DaVID b.(3), McnIVen I.(3), aSMUSSen b.(4), ToMKInS H.(2), DolbY n.(3), alPIn K.(5), RIcHaRDS T.(3), RoWe c.(3), leaVeSleY M.(6), ManDUI H.(7)

(1) Waikato University, HaMIlTon, neW ZealanD;(2) James cook University, caIRnS, aUSTRalIa;(3) Monash University, MelboURne, aUSTRalIa;(4) Queensland Museum, bRISbane, aUSTRalIa;(5) cSIRo, canbeRRa, aUSTRalIa;(6) University of Papua new Guinea, PoRT MoRSebY, PaPUa neW GUInea;(7) national Museum and art Gallery of Papua new Guinea, PoRT MoReSbY, PaPUa neW GUInea

AbstractFor those undertaking archaeological research in coastal areas, marine animals are the logical choice of material remains to investigate issues of culture change and the role of environment and climate. The calibration of radiocarbon dates on marine animals is not straight forward, however, requiring an understanding of habitat and dietary pReferences as well as detailed knowledge of local ocean conditions. Recent advances in our understanding of variation in the marine 14C reservoir indicate that the most complex situations occur where terrestrial influences impinge on the marine environment, such as in estuaries and lagoons, resulting in an enrichment and depletion of 14C (Ulm 2002; Petchey and Clark 2011). Increased precision in radiocarbon technology, combined with the analysis of δ13C and δ18O isotopes, and careful sample selection gives us the ability to identify 14 C variation hitherto obscured. Here we present new research that details high resolution mapping of marine reservoir variation between Gafrarium tumidum, G. pectinatum, anadara granosa, a. antiquata, Strombus luhuanus, S. gibberulus, S. urceus, S. canarium, S. labiatus, S. aurisdianae, lambis lambis, batissaviolacea, Polymesoda erosaand echinoidea from Bogi 1, Caution Bay, southern coastal Papua New Guinea.

References1. Ulm S. 2002 Marine and estuarine reservoir effects in central Queensland, Australia: Determination of ΔR

values. Geoarchaeology 17(4):319-348.2. Petchey F. and G. Clark 2011 Tongatapu hardwater: Investigation into the 14C marine reservoir offset in

lagoon, reef and open ocean environments of a limestone island. Quaternary Geochronology. DOI:10.1016/j.quageo.2011.08.001

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S06-P-177

BULK STABLE CARBON ISOTOPE RATIOS FROM THE POTTERY CRUSTS IN EASTERN FENNOSCANDIA - CHRONOLOGICAL AND GEOGRAPHICAL VARIATION

PESONEN P.(1)(2), caRPelan c.(1), oInonen M.(3), onKaMo P.(2), TallaVaaRa M.(1)

(1) Department of Philosophy, History, culture and art Studies, UnIVeRSITY of HelSInKI, fInlanD;(2) Department of biosciences, UnIVeRSITY of HelSInKI, fInlanD;(3) finnish Museum of natural History, UnIVeRSITY of HelSInKI, fInlanD

AbstractThe prehistory of Eastern Fennoscandia saw a succession of ceramic traditions, beginning from c. 5100 cal BC. The first potters were hunter-gatherers, but during the Late Subneolithic, the food production economy gradually spread in the area. The current chronological frame of the prehistoric ceramic phases is formed mainly by direct AMS radiocarbon dates from food crust and birch bark tar attached in the pots. Performed as an integral part of the radiocarbon dates, measurements of stable carbon isotopic ratios (δ13C) of crust samples possibly carry information on the subsistence strategies of the people. Particularly, large geographical and temporal variation has been observed for these values (Pesonen et al 2012) - consistent with the spatial differences in the use of dietary resources. The material consists of c. 220 AMS crust datings from Finland, Norway and Russia performed over the last 25 years. First, the effects behind the observed isotopic ratios are discussed. Based on this scrutiny, understanding of variability in stable carbon isotope ratios is facilitated by comparing their spatiotemporal trends with the trends in archaeozoological materials linked to resource use and with the present paleoclimatic understanding. In addition, the isotopic data and the food crust dates are compared with that of birch bark tar from the same contexts allowing also for intra-site and multiple paired-sample comparisons of the measurements.The Fennoscandian Shield is almost devoid of limestone and thus the magnitude of the freshwater reservoir effect has been considered minimal in this geological area covering most of Eastern Fennoscandia. On the other hand, the complicated history of the Baltic Sea makes handling of the marine reservoir effect complicated. The dataset allows also for discussing the stable carbon isotope values also in order to further elaborate the reservoir effect correction model (Pesonen et al. 2012).

ReferencesPesonen P, Oinonen M, Carpelan C, Onkamo P. 2012. Early Subneolithic ceramic sequences in Eastern Fennoscandia - a Bayesian approach. Accepted for publication in Radiocarbon.

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384

S06-P-178

DATING POLLEN TO REFINE MARINE RESERVOIR AGE IN THE NORTHWESTERN NORTH ATLANTIC

NEULIEB T.(1)(2), leVac e.(3)(2), SoUTHon J.(4), leWIS M.(5), PenDea f.(6), cHMURa G.(1)(2)

(1) McGill University, MonTReal, canaDa;(2) Global environmental and climate change centre, MonTReal, canaDa;(3) bishop’s University, SHeRbRooKe, canaDa;(4) University of california, IRVIne, UnITeD STaTeS;(5) Geological Survey of canada atlantic, natural Resources canada, bedford Institute of oceanography, DaRTMoUTH, canaDa;(6) lakehead University, oRIllIa, canaDa

AbstractAbrupt cooling events in the early Holocene have been associated with episodic drainage of meltwater from North American proglacial lakes into the northwestern North Atlantic. Marine sediments can provide key evidence for the timing of these short-lived events. Dating of these deposits is complicated by the marine reservoir effect (MRE) which can vary in space and time, and by extended sea ice cover that isolates marine waters from the atmospheric carbon dioxide reservoir. The marine reservoir effect has yet to be adequately investigated in the waters of the northwestern North Atlantic. For example, a cooling episode termed the «8.2 ka event» is attributed to the drainage of glacial Lake Agassiz, yet the event was not well linked chronologically with some of the sedimentary evidence for Lake Agassiz drainage when an estimated correction of 400-450 years based on the current global average MRE of 400 years was applied to the sedimentary marine biogenic radiocarbon dates. Nevertheless, detrital carbonate layers deposited along the Labrador and Newfoundland shelves by the final drainage of Lake Agassiz were dated to 8.15-8.49 cal ka, close to the «8.2 ka event» age, when an additional correction of 200 years was used to account for the longer-than-present sea ice duration in the early Holocene. The additional correction was estimated from early Holocene dinoflagellate cyst record calibrated to modern sea-ice conditions.To assess the MRE more directly, terrestrial material (such as macrofossils) can be used, but such material is usually not available in marine sediments. In this study, terrestrial pollen grains deposited in marine sediments were dated to assess the local reservoir age for the Labrador-Newfoundland shelves where we find sedimentary evidence of rapid meltwater drainage events. Six marine sediment cores were subsampled at the same depth intervals where radiocarbon dates on mollusc shells or foraminifera tests were available. The sediment samples were sieved and the fine fractions chemically processed using HF and HCL. KOH and acetolysis were not used to ensure the integrity of the pollen samples and to avoid additional input of carbon. We used a hand pipetting system to isolate and extract pollen of pine (Pinus) and spruce (Picea) to ensure that old carbon was not introduced via non-pollen plant material. The extracted pollen samples were dated at the University of California Irvine. Initial results suggest that while some pollen dates overlap with the shell or foraminifera dates when they are calibrated, other pollen dates differ. For pollen ages that are older than shell dates, we propose that the sediments integrated pollen rain from a longer time period, possibly due to the extended sea ice cover or reworked pollen grain. Given that pollen grains are smaller than shells or foraminifera, the role of bioturbation will have to be assessed. However, further investigation will be needed to fully interpret the results.

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385

S06-P-179

DEAD CARBON PROPORTION AND MINERALOGY OF FOUR INDIAN SPELEOTHEMS

YADAVA M., RenGaSWaMY R.

Physical Research laboratory, aHMeDabaD, InDIa

AbstractFour speleothem samples growing in different caves were investigated for dead carbon content and mineralogy (calcite/aragonite). These were dated by liquid scintillation spectrometry method which indicates that they cover time span from present to last 3400 yr BP. Two among these, show presence of bomb carbon at the tip part, one growing in a chamber where overlying soil and bedrocks are merely ~3m thick the other one growing below ~30 m thick layers. Remaining two were actively forming and had overlying layers between 8-10 m, they show apparent ages as 880 yr BP and 1320 yr. These results clearly indicate insignificant role of soil and bedrock thickness in controlling the dead carbon content in spleothems. Internal conditions of the seepage pathways seem to be dominant.To explore if precipitation has any control on the mineral structure, these were further taken up for mineralogical studies. As changes in the oxygen isotope ratio (δ18O) in these speleothems are found to respond to precipitation amount, investigation was carried out for those spots where δ18O has extreme values. Out of four only one speleothem sample showed association between δ18O and mineral type: spots having depleted δ18O levels have higher calcite content (60 to 90%) remaining being aragonite. In contrast, the spots showing enriched values in δ18O have more of aragonite (80 to 95%) compared with calcite.

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386

S06-P-180

RADIOCARBON RESERVOIR EFFECT IN FRESH WATER LAKE SEDIMENT, LOESS PLATEAU, NORTH OF CHINA

ZHOU A.

lanzhou university, lanZHoU, cHIna

AbstractRadiocarbon reservoir is a big hamper to reconstruction the past climate change in lake sediment or peat deposit. The reservoir age of a water body is the difference between the radiocarbon ages of the water body and the contemporary atmosphere. Reservoir age changes throughout time are directly linked to changes in reservoir parameters and in atmospheric Δ14C. In order to evaluate bulk organic reservoir in fresh lake sediment, A common method is to date contemporaneous aquatic/bulk organic and terrestrial material to evaluate the reservoir effect. In general fresh water lake sediment thought to be no reservoir effect in radiocarbon dating.Our research present an instance of fresh water lake radiocarbon reservoir in north west of china. Tianchi lake, located on the upper Liupan Mountains, on the southwest Loess Plateau, The dimensions of the lake are 250 m from east to west and 120 m from south to north, and it covers an area of 20,000 m2. The maximum water depth of the lake is 8.2 m. It is a freshwater lake with no surface inflow streams, fed only by precipitation and groundwater. Two 11-m-long parallel sediment cores were taken at Tianchi Lake in September 2007 using a Piston Corer with platform UWITEC at the water depth of 8.2 m. The lithology of the almost whole core is consisted of silty lacustrine sediments with 1-2 mm thickness distinctive organic-detritus lamination. Many terrestrial leaves and twigs were found during the sub-sampling.25 Abies leaf macrofossils were picked out and graphite synthesis was taken in chronology laboratory, Key Laboratory of Western China’s Environmental System, Lanzhou University. Radiocarbon measured by using accelerator mass spectrometry (AMS) at the AMS Dating Laboratory at Beijing University (Beijing, China). To detect the radiocarbon reservoir in Tianchi lake, Four bulk organic with contemporary macrofossils were picked out and send to BETA laboratory to carry out AMS radiocarbon dating.The results shows 25 radiocarbon data from Abies leaf macrofossils with good linearity fitting to the deposition model. Four bulk organic radiocarbon data shows older than contemporary macrofossils, exhibited obviously radiocarbon reservoir, which varied from 350 to 535 radiocarbon reservoir. we suggest the reason of reservoir is Hard water effect (HWE), itself being related to both riverine runoff and the riverine content in «dead» ΣCO2, as well as to the lake water budget, riverine runoff, as well as rock weathering, is able to change the Hard Water Effect and, as a result, the basin reservoir age. Our research proved again, even in a fresh water lake sediment, reservoir effect still existed. Therefore, special caution should be paid to the correction of the 14C reservoir effect by a unique 14C reservoir age in paleoclimatic and paleolimnological study of northwest China. All the Bulk organic 14C chronology should be reevaluated when using in chronology-depth model.

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387

S06-P-181

FRESHWATER RADIOCARBON RESERVOIR EFFECTS IN PREHISTORIC UKRAINE: RADIOCARBON DATES FROM HUMAN, FAUNAL AND FISH SKELETAL COLLAGEN FROM NEOLITHIC SITES IN THE DNIEPER BASIN

BUDD C.(1), lIllIe M.(2), PoTeKHIna I.(3), HIGHaM T.(1)

(1) University of oxford, oXfoRD, UnITeD KInGDoM;(2) University of Hull, HUll, UnITeD KInGDoM;(3) Ukrainian academy of Sciences of Ukraine, KIeV, UKRaIne

AbstractThis poster presents the radiocarbon dates of human, faunal and fish skeletal collagen samples from a number of Neolithic cemeteries located in the Middle and Lower Dnieper Basin, Ukraine. The excavations at a number of Neolithic cemetery sites in this region, such as Dereivka I, Vil’nyanka and Yasinovatka, revealed human interments where faunal and freshwater fish remains were found in close association. Radiocarbon dates were obtained for these human, fish and faunal samples, and the dates produced displayed a disparity in radiocarbon ages of approximately 500-700 years between samples - tentatively suggesting the presence of a freshwater radiocarbon reservoir effect during this period. Stable carbon and nitrogen isotope analysis which was carried out on the human, faunal and fish skeletal assemblages from a number of Epi-palaeolithic to Eneolithic sites in the Dnieper Basin, suggests an increased reliance on freshwater protein resources from the Epi-palaeolithic/Mesolithic period into the Neolithic period, and a shift towards terrestrial based protein at the onset of the Eneolithic period. The increase in freshwater resource consumption during the Neolithic coincides with evidence for a significant Black Sea transgression event, which potentially contributed towards the shift in dietary choices during this period, and perhaps suggests a diet-derived reservoir effect. The purpose of this poster therefore is to highlight the preliminary evidence for a freshwater radiocarbon reservoir effect during the Neolithic period in the Dnieper Basin sites in the Ukraine, and also to further discuss the wider implications of radiocarbon dating skeletal material from the Ukraine and surrounding areas, particularly those which are located in close proximity to the Black Sea.

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388

S06-P-182

USING AN INDEPENDENT GEOCHRONOLOGY BASED ON PALAEOMAGNETIC SECULAR VARIATION (PSV) AND ATMOSPHERIC PB DEPOSITION TO DATE BALTIC SEA SEDIMENTS AND INFER 14C RESERVOIR AGE.

LOUGHEED B.(1), SnoWball I.(1), MoRoS M.(2), Kabel K.(2), MUScHeleR R.(1), VIRTaSalo J.(3), WacKeR l.(4)

(1) lund University, lUnD, SWeDen;(2) leibniz Institute for baltic Sea Research, WaRneMÜnDe, GeRManY;(3) Geological Survey of finland, eSPoo, fInlanD;(4) eTH, ZÜRIcH, SWITZeRlanD

AbstractRadiocarbon dating of sediment cores from the Baltic Sea has proven to be difficult due to uncertainties surrounding the 14C reservoir age of this semi-enclosed shelf sea, combined with a scarcity of macrofossils suitable for dating. Here we present the results of multiple dating methods carried out on cores in the Gotland Deep area of the Baltic Sea. Particular emphasis is placed on the brackish Littorina stage (8 ka ago to the present) of the Baltic Sea and possible changes in the 14C reservoir age of our dated samples. Three geochronological methods are used. Firstly, palaeomagnetic secular variations (PSV) are reconstructed, whereby ages are transferred to PSV features through comparison with varved lake sediment based PSV records. Secondly, lead (Pb) content and stable isotope analysis are used to identify past peaks in anthropogenic atmospheric Pb pollution. Lastly, 14C determinations were carried out on benthic foraminifera (elphidium spec.) samples from the Littorina stage of the Baltic Sea. Determinations carried out on smaller samples (as low as 4 μg C) employed an experimental, state-of-the-art method involving the direct measurement of CO2 from samples by a gas ion source without the need for a graphitisation step (Ruff et al., 2010; Wacker et al., submitted). This is the first time this method has been performed on foraminifera in an applied study. The PSV chronology, based on the uppermost Littorina stage sediments, produced ten age constraints between 6.29 and 1.29 cal ka BP, and the Pb depositional analysis produced two age constraints associated with the Medieval production peak. Analysis of PSV data shows that adequate directional data can be derived from both the present Littorina saline phase muds and Baltic Ice Lake stage varved glacial sediments. Authigenic greigite present in the intermediate Ancylus Lake freshwater stage sediments acquires a gyroremanent magnetisation during static alternating field (AF) demagnetisation, preventing the identification of a primary natural remanent magnetisation. An inferred marine reservoir age offset (ΔR) is calculated by comparing the foraminifera 14C determinations to a PSV & Pb age model. This ΔR is found to trend towards younger values upwards in the core, possibly due to a gradual change in hydrographic conditions brought about by a reduction in marine water exchange from the open sea due to continued isostatic rebound. We also present preliminary results of 14C reservoir age estimates based on 14C determinations carried out on shells of known ages.

References1. Ruff, M., Szidat, S., Gäggeler, H.W., Suter, M., Synal, H.-A., Wacker, L., 2010. Gaseous radiocarbon

measurements of small samples. Nuclear Instruments and Methods in Physics Research Section B: Beam Interactions with Materials and Atoms 268, 790-794.

2. Wacker, L., Lippold, J., Molnár, M., Schulz, H., submitted. Towards single-foraminifera-dating with a gas ion source. Nuclear Instruments and Methods B.

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389

S06-P-183

RATIO OF THE CARBON ISOTOPES IN THE BASIC ELEMENTS OF THE DNIEPER RIVER ECOSYSTEM.

SKRIPKIN V., GlaVaTSKaYa e., KoValIUKH n.

Institute of environment Geochemistry of national academy of Sciences of Ukraine, KIeV, UKRaIne

AbstractThe main aim of the present investigation was to study the possibility of use of hydrophytes and fish as sensitive indicators of water ecosystems contamination with technogenic emissions containing carbon.The river ecosystem’s distinctive characteristic is the radiocarbon reservoir effect. Its rate depends on many factors and influences carbon isotope distribution in the major water system’s elements.The following types of carbon-bearing samples have been studied: dissolved hydro carbonate, hydrophytes, fish, mollusks, and organic matter of the bottom sediments. The samples had been taken during nine years in the River Dnieper 5 kilometers upstream the Prypiat river mouth.As a result of our work a large quantity of radiocarbon analyses of all radiocarbon-bearing components of the water ecosystem’s elements has been made. Radiocarbon analysis was followed by carbon stable isotopes ratio changes. The obtained results give good interpretation of radiocarbon reservoir effect influence on carbon isotope ratio in biological objects depending on the type of strophic nutrition chains and allow selecting optimum group of bioindicators for solving concrete ecological tasks.Basing on the 9-year investigation, it may be concluded that the integral values of the radiocarbon reservoir effect is relatively stable during the vegetation period (May-October).As the most reliable and convenient bioindicators of water ecosystems contamination with technogenic radiocarbon, we suggest using the following objects: plants ceratophyllum submersum Lepesch and Miriophyllum spicatuml and fish species Rutilus rutilus (roach). These bioindicators allow carrying out qualitative retrospective analysis of the dynamics of radiocarbon isotope ratio variations in water ecosystems. Development of the suggested approach might result in creation of effective assessment methods of carbon-bearing technogenic emissions on the water ecosystems.

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390

S06-P-184

SEASONAL AND INTERANNUAL ?14C VARIATIONS OF SEAWATER DIC RECORDED IN CORAL FROM SAN BENEDICTO ISLAND IN THE SUBTROPICAL PACIFIC OCEAN

FERGUSON J.(1), DRUffel e.(1), caRRIQUIRY J.(2), VIllaeScUSa J.(2)

(1) University of california. Irvine, IRVIne, UnITeD STaTeS;(2) Universidad autónoma de baja california, ensenada, enSenaDa, MeXIco

AbstractThe circulation of our oceans has a huge influence on our climate system by transporting heat and nutrients and by affecting atmosphere-ocean exchange of carbon. However we must rely on proxy records to extend our knowledge of changes in ocean circulation beyond the instrumental and satellite records. The radiocarbon content (Δ14C) of seawater dissolved inorganic carbon (DIC) acts as a tracer of ocean circulation because it is produced in the atmosphere and, through air-sea gas exchange, enters surface waters leaving them enriched relative to the deeper ocean. Mixing of surface and deeper waters therefore results in a difference in 14C between atmospheric and surface seawater (radiocarbon reservoir age). Corals have been shown to act as important archives of past seawater Δ14C, and therefore reservoir age, because their aragonite skeletons are formed using seawater DIC. By incremental sampling of the coral skeleton a continuous, high resolution record of radiocarbon reservoir age can be constructed often spanning a century or more.We present a seasonal and biennial record of surface seawater Δ14C reconstructed from a Porites coral collected from San Benedicto Island (19°19’N, 110°49’W) in the transition zone between the subtropical and equatorial North Pacific Ocean. Samples were drilled at bimonthly to biennial resolution then processed and analyzed using accelerator mass spectrometry at the Keck CCAMS facility at UC Irvine. Stable isotope and trace element ratios within the coral show strong seasonal variability in sea surface temperature reflecting the influence of the southward flowing California Current during the winter and the northward flowing Costa Rica Coastal Current in the summer (Villaescusa and Carriquiry 2004). High resolution Δ14C measurements of the coral allow investigation of the amount of seasonal variability in radiocarbon reservoir age which results from the influence of the two different water masses. The longer biennial coral Δ14C record is used to examine the strength of upwelling along the west coast of North America over recent decades as well as major shifts in ocean circulation patterns in the region. These records can also be used in conjunction with those of previous studies to improve our understanding of large scale ocean circulation changes in the Pacific Ocean.

ReferencesVillaescusa, J. A. and Carriquiry, J. D. (2004). Calibración de los paleotermómetros de Sr/Ca y Mg/Ca en el coral Porites sp. de Isla San Benedicto, Archipiélago Revillagigedo, México. Ciencias Marinas 30(04), pp. 603-618.

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391

S06-P-185

SEASONAL VARIABILITY IN RADIOCARBON RESERVOIR AGE DUE TO UPWELLING RECORDED IN MYTILUS CALIFORNIANUS SHELLS

FERGUSON J.(1), JoHnSon K.(1), SanToS G.(1), MeYeR l.(2), TRIPaTI a.(3)

(1) University of california. Irvine, IRVIne, UnITeD STaTeS;(2) Yale University, neW HaVen, UnITeD STaTeS;(3) University of california, los angeles, loS anGeleS, UnITeD STaTeS

AbstractAlong the west coast of North America, climate and marine productivity is strongly affected by seasonal to interannual changes in coastal upwelling intensity. However our understanding of the variability of upwelling on these timescales in the past is limited by the short duration of instrumental records. Changes in upwelling intensity result in variable amounts of mixing of old, deeper water into surface waters resulting in temporal variability in the radiocarbon reservoir age. Marine bivalves form their shells from dissolved inorganic carbon (DIC) in seawater and so may record these seasonal to interannual variations in reservoir age. By analyzing old bivalve shells it may be possible to provide valuable information about the extent of upwelling in these regions in the past.To examine whether the radiocarbon composition of California mussel (Mytilus californianus) shells could be used to produce records of upwelling intensity we collected three living mussels from Newport Beach, CA in 2009 and 2010. Sequential samples were drilled using a New Wave Micromill from the outer calcite layer of these shells at 50-200 μm resolution and analysed for oxygen and carbon isotopic composition. The oxygen isotope profiles were then used to assign an age model for each shell and allowed larger samples for radiocarbon analysis to be drilled at seasonal-resolution. The shell radiocarbon profiles, and δ13C profiles, are compared with instrumental records and a nearby timeseries of seawater DIC 14C and δ13C (Santos et al 2011). We show that seasonal Mytilus californianus shell 14C values allow the reconstruction both of the absolute seawater DIC 14 C values and also the majority of the seasonal range in seawater DIC 14C. Mussel shells could therefore present an easier and cheaper alternative to traditional seawater DIC 14C measurements in coastal regions and could allow seawater DIC 14C reconstruction for the past. Results are also presented from a suite of Mytilus californianus shells, collected from Mexico to Oregon in 1998-1999 as an illustration of how such shells could be used to generate larger scale snapshots of seawater DIC 14C and upwelling along the west coast of North America for the past.

ReferencesSantos, G. M., Ferguson, J. E., Acaylar, K., Johnson, K. R., Druffel, E. and Griffin, S. (2011). Δ14C and δ13C of seawater DIC as tracers of coastal upwelling: A 5-year time-series from Southern California, Radiocarbon 53(4): 669-677.

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392

S06-P-186

RADIOCARBON AGE OFFSET BETWEEN SHELL AND PLANT PAIRS IN THE HOLOCENE LAGOON SEDIMENT AROUND THE MAE-HO LAGOON, EASTERN KOREA

NAKANISHI T.(1), HonG W.(1), SUnG K.S.(1), naKaSHIMa R.(2), naHM W.H.(1), lIM J.(1), KaTSUKI K.(1)

(1) Korea Institute of Geoscience & Mineral Resources, DaeJeon, SoUTH KoRea;(2) advanced Industrial Science & Technology, TSUKUba, JaPan

AbstractThe long term changes of marine reservoir effect are indispensable data for the calibration of radiocarbon ages from geological and archaeological samples which were produced in marine environment. The estimation is difficult around the coastal area in Korea because suitable sample pair representing marine and terrestrial ages is not common. In order to solve this problem, radiocarbon ages of marine shell and terrestrial plant pairs from same horizons were analysed at the AMS system in Korea Institute of Geoscience and Mineral Resources. Approximately 11 m length core of Holocene sediment was obtained from a front of reclaimed land around Lagoon Mae-ho in eastern coast of Korea. The core consisted of three units: sand-gravel alternation, mud bed, and sand-mud alternation from bottom to top. We interpreted these units on the basis of lithology, sedimentary structures, mollusk and diatom assemblages, and land use history, and concluded that they had been formed in three paleoenvironments: small channel, lagoon, and reclaiming by human, respectively. The lagoon sediment consisted of gray to dark gray mud with plants and shells such as lacuna sp., batillaria cumingii (Crosse), crassostrea sp., Potamocorbula sp., and corbiula japonica Prime. These habitants and their δ13C values (-1.3 to -11.4 ‰) indicates marine to brackish environments. The lagoon sediment contained marine to brackish water diatoms such as Paralia sulcata, nitzschia lanceolata, cyclotella striata, cyclotella caspia group. These changes of habitants and δ13C values along the depth supported an increase and then a decrease of salinity. This sediment would be suitable for estimation of marine reservoir effect around this area from radiocarbon ages of shell and plant pairs because it had been formed in stable accumulation rate: about 1 mm/yr. Radiocarbon age offsets of 11 pairs seem to be divided in three stages: 0-500 yrs (7350-5800 yr cal BP), 600-900 yrs (4320-1600 yr cal BP), and 0-400 yrs (1200-390 yr cal BP). This change might indicate the mixing ratio change of brine and freshwater. On the other hands, these reservoir effects of eastern coast during 4320-1600 yr cal BP were larger than ones from western coast of Korea. It might be associated by the seawater circulation and the upwelling of radiocarbon depleted deep-seawater from the northward of the sea among Korea, Japan and Russia.

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393

S06-P-187

MARINE RESERVOIR CORRECTION FOR THE EASTERN COAST OF THE PHILIPPINES BASED ON KNOWN-AGE CORALS

PRIOR C.


Abstract In order to provide reliable calibrated ages for marine samples, is it necessary to know the local regional difference, ΔR, for globally average marine reservoir age, R (Stuiver and Braziunas 1993). Despite ongoing additions to the database of marine reservoir corrections (http://calib.qub.ac.uk/marine), there are still many areas for which no ΔR has been published. Since the marine reservoir correction can have significant local variations over quite small geographic areas, particularly in areas where bays, estuaries and irregular coastlines affect ocean currents, choosing an approximate value from the general area is of limited use. ΔR correction is usually determined by dating pre-bomb known-age mollusc or gastropod shells, but the only way to be certain of the year and location of collection is to acquire samples from museum collections. These are often unobtainable for the locality under study. An alternative is to measure the 14C in pre-1950 growth bands in modern corals. We will present data from a project to determine Δ from modern coral cores acquired along the eastern coast of the Philippines. Two sites were selected in order to study the variability of ΔR as a consequence of whether an area is an upwelling site or not and to attempt to study the effects of climate cycles (El Nino wet and dry years) on ΔR.

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394

S06-P-188

RESERVOIR AGE EVOLUTION IN THE FORMER BLACK SEA «LAKE»

SOULET G.(1), MÉnoT G.(1), GaRReTa V.(1), RoSTeK f.(1), ZaRaGoSI S.(2), leRIcolaIS G.(3), baRD e.(1)

(1) ceReGe, Univ. aix-Marseille, cnRS, IRD & collège de france, TecHnoPole De l’aRboIS bP80, 13545 aIX en PRoVence ceDeX 4, fRance;(2) Université bordeaux I, UMR5805 ePoc, aVenUe DeS facUlTÉS, 33405 Talence, fRance;(3) IfReMeR, centre de brest, Géosciences Marines, bP70, 29280 PloUZanÉ ceDeX, fRance

AbstractProviding robust 14C-based calendar chronologies of the Last Glacial sediments of the Black Sea «Lake» is an arduous task because of issues related to reservoir age. Nevertheless, depending on basin hydrology, reservoir ages represent a tool that could potentially be used to better understand the hydrologic evolution of Black Sea «Lake» during the last glacial. Therefore, reconstructing the Black Sea «Lake» reservoir age evolution is crucial both for better constraining the basin chronological framework and for providing new insights into our understanding of the basin hydrology.To reconstruct the Black Sea «Lake» reservoir age evolution, we have firstly reconstructed the Lake Surface Temperature and provided a qualitative proxy for basin productivity using a long sediment core from the NW Black Sea (MD04-2790). Then, the calendar chronology of the core was obtained by tuning the obtained dataset to a climate reference record. Finally, the chronology is compared to a large AMS radiocarbon dataset (n=51). Pairs of calendar and radiocarbon ages allowed us to compute reservoir ages, and to provide a high-resolution quantitative reservoir age record for the last glacial history of the Black Sea «Lake».The main factor controlling reservoir ages in lakes is the Hard Water Effect (HWE), which is regulated by basin hydrology. Therefore, changes in the reconstructed reservoir age record have been qualitatively interpreted in terms of the hydrologic responses of the Black Sea «Lake» to climate change. Our results allowed us to determine periods of complete isolation or outflow for the Black Sea «Lake» and to reveal phase of water mass stratification. Following the onset of the Bølling-Allerød (BA), factors other than the HWE may have influenced the reservoir age. Finally, we will test the possible impact of clathrate dissociation on reservoir age change at the Oldest Dryas - BA transition by using pairs of δ13C and reservoir age.

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S06-P-189

FRESHWATER RESERVOIR EFFECT VARIABILITY IN NORTHERN GERMANY

PHILIPPSEN B., HeIneMeIeR J.

aMS 14c Dating centre, aaRHUS, DenMaRK

AbstractThe freshwater reservoir effect is a potential problem when radiocarbon dating fishbones, shells, human bones or food crusts on pottery from sites next to rivers or lakes. The reservoir age in rivers containing considerable amounts of dissolved 14C-free carbonates can be up to several thousand years and may be highly variable. For accurate radiocarbon dating of freshwater-based samples, the order of magnitude of the reservoir effect as well as the degree of variability has to be known.The initial problem in this case was the accurate dating of food crusts on pottery from the Mesolithic sites Kayhude at the river Alster and Schlamersdorf at the river Trave, both in Schleswig-Holstein, Northern Germany. Measurements on modern materials from these rivers may not give a single reservoir age correction that can be applied to archaeological samples, but they will show the order of magnitude and variability that can also be expected for the past.Water DIC from different seasons, and from the same season in different years, has been dated because it is the carbon source in photosynthesis and thus at the basis of the rivers’ food webs. The radiocarbon ages of underwater plants and different parts (underwater or floating) of emerging water plants are compared, as it might be expected that the reservoir age is higher for plants that assimilate DIC as for plants or parts of plants that assimilate atmospheric CO2. Mollusc shells as well as flesh and bone collagen of fish are dated as well.Radiocarbon datings of archaeological samples from the two Mesolithic sites will be analysed, considering the insights provided by the study of modern material.

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S06-P-190

COLLAGEN-BIOAPATITE RADIOCARBON AGE DIFFERENCES LINKED TO RESERVOIR EFFECT

FERNANDES R.(1)(2), GRooTeS P.M.(1), naDeaU M.J.(1)

(1) leibniz-laboratory for Radiometric Dating and Isotope Research, KIel, GeRManY;(2) Graduate School Human Development in landscapes, KIel, GeRManY

AbstractRadiocarbon dating represents the most widely used method for the establishment of absolute chronologies, often relying on the dating of human bone material. Reservoir effect is the expression used to denote the presence of a radiocarbon-depleted signal within an aquatic reservoir. Humans with an aquatic diet will incorporate a reservoir effect signal. Radiocarbon dating of this bone material results in apparently older chronologies.The main organic fraction of bone, collagen, is usually preferred for radiocarbon dating. In contrast, bone’s inorganic fraction, bioapatite, is less often radiocarbon dated due to its high susceptibility to diagenesis and contamination. Bioapatite carbonate is in equilibrium with blood bicarbonate, which is derived from respired CO2 (Jim et al. 2004). Thus, bioapatite carbon is routed from the entire dietary mix (Froehle et al. 2010), mostly represented by carbohydrates. In contrast, bone collagen will reflect primarily protein intake. As fish is particularly rich in protein and depleted in carbohydrates, collagen-bioapatite radiocarbon age differences should be observed in fish consumers and provide an estimate of reservoir effect.Based on recently published compiled results of controlled feeding experiments of animals (Froehle et al. 2010), a simple algebraic model is presented establishing the routing of dietary protein and energy (carbohydrates and lipids) towards bone collagen and bioapatite.This model was applied to recently published data (Cherkinsky 2009), consisting of stable isotope analyses (δ13C) and radiocarbon dates of both collagen and bioapatite, on well preserved human remains found in Stone Age shell middens in the Western Cape Province of South Africa. The model was capable of establishing a clear linear relationship between dietary energy intake and individual reservoir effect. It was also capable of accurately predicting the local reservoir effect and the local plant isotopic signal. These results provide the first evidence for collagen-bioapatite radiocarbon age differences linked to reservoir effect, and open the possibility of using the presented model to improve radiocarbon-based chronologies.

References1. Cherkinsky, A., 2009, Can we get a good radiocarbon age from «bad bone»? Determining the reliability of

radiocarbon age from bioapatite, Radiocarbon 51(2), 647-655.2. Froehle, A.W., Kellner, C.M., and Schoeninger, M.J., 2010, FOCUS: effect of diet and protein source on

carbon stable isotope ratios in collagen: follow up to Warinner and Tuross (2009), Journal of archaeological Science 37(10), 2662-2670.

3. Jim, S., Ambrose, S.H., and Evershed, R.P., 2004, Stable carbon isotopic evidence for differences in the dietary origin of bone cholesterol, collagen and apatite: implications for their use in palaeodietary reconstruction, Geochimica et cosmochimica acta 68(1), 61-72.

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397

S06-P-191

EFFECT OF A FOSSIL CO2 ON TREES. DENDROCHRONOLOGICAL, RADIOCARBON AND δ13C ANALYSES ON qUERCUS SP. FROM THE ANSANTO VALLEY (SOUTH ITALY)

CAPANO M.(1)(2), MaRZaIolI f.(2)(3), PIGnaTellI o.(4), MaRTInellI n.(4), PaSSaRIello I.(3)(2), GIGlI S.(1), SIRIGnano c.(3)(2), RIccI P.(3)(2), TeRRaSI f.(3)(2)

(1) Dipartimento di Studio delle componenti culturali del Territorio, Second University of naples, SanTa MaRIa caPUa VeTeRe (ce), ITalY;(2) InnoVa and cIRce (centre for Isotopic Research on cultural and environmental heritage), San nIcola la STRaDa (ce), ITalY;(3) Dipartimento di Scienze ambientali, Second University of naples, caSeRTa, ITalY;(4) Dendrodata s.a.s, VeRona, ITalY

AbstractSince ancient time, the Ansanto valley is a famous place of worship: Mephitis goddess in the I millennium BC, Santa Felicita from the I millennium AD. Originally the cult of Mephitis was linked tosulfur waters. In fact, the main characteristic of the site is the presence of several water springs, where some gases arise from: CO2 (98%), N2 (1.3%), H2S (0.33%) and CH4 (0.23%). During the years many geologists analysed the phenomenon, reaching different conclusions: on one hand, the hypothesis of secondary volcanism phenomena; on the other hand, the superficial origin of the fumes, with the formation of CO2 caused by the decomposition of limestone rock carbonates operated by the sulfuric acid. In any case, independently by the vent origins, fossil CO2 arises from the springs and it diffuses in the valley. Assuming that the intensity and distribution of emissions vary over time, our aim is to quantify them, analysing the radiocarbon content in tree rings. So, some oak trees were cored in the Ansanto valley at an increasing distance from the main emitting lake. The tree-ring sequences were dendrochronologically measured and cross-dated to validate the dating of each ring. Selected rings from each tree were radiocarbon analyzed with the AMS system of CIRCE laboratory (Caserta, Italy), covering the last 40 years; δ13C analyses were made too. The F14C of our samples was compared with the Bomb spike curve (a mean of northern hemisphere zone 1, Jungfraujoch data and data from the NOAA ESRL/GMD, Niwot Ridge Forest, Colorado) and the fossil dilution was calculated applying an isotopic mass balance.Preliminary analyses in the rings corresponding to the last decade years show high dilution percentage (ranging between 16% and 29%) at about 30m from the emitting spring and confirm the variability over time in intensity and spatial distribution.

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S06-P-192

RADIOCARBON WIGGLE-MATCH DATING OF VARVED LAKE SEDIMENTS IN SOUTHERN SWEDEN

MELLSTRÖM A., MUScHeleR R., SnoWball I., nInG W., HalTIa-HoVI e.

lund University, lUnD, SWeDen

AbstractAccurate and precise chronologies are essential for correlation of different geological archives that aim to investigate the temporal and spatial development of climate change. One way to achieve accurate chronologies is to apply the 14C wiggle-match dating technique. The technique is facilitated by periods of major anomalies or ‘wiggles’ in the 14C calibration curve, which, for example, occurred around 2800-2600 cal. BP and 2400-2200 cal. BP.When dating lake sediments, terrestrial macrofossils are generally considered to yield more reliable 14C age estimates than bulk sediments. This is because the bulk sediments can be influenced by a hard-water reservoir effect, or input of old carbon; both processes result in excessively old ages. Unfortunately, there are not always enough terrestrial macrofossils available for dating and bulk sediments must be used instead. In such cases the wiggle-match dating technique can offer a possibility to quantify the reservoir effect and provide accurate ages. Motivated by major climate and geomagnetic field changes around 3000-2000 cal. BP we applied the 14C wiggle-match dating technique to date bulk sediments from a lake in southern Sweden.The study site - Gyltigesjön - is a lake with annually laminated sediments. The varves are biogenic and consist of two seasonal laminas. The advantage of the annually laminated record is the known numbers of years between the bulk samples that were selected for 14C analyses. In addition, macrofossils were available for comparison to the bulk sediments. The purpose was to construct an accurate chronology for the Gyltigesjön sediments between 3000 and 2000 cal. BP with the wiggle-match dating approach. The inferred bulk sediment ‘reservoir’ effect can then be crosschecked via comparison to the results of the macrofossils dating. Our study shows that it is possible to obtain accurate age estimates and to infer a 14C lake ‘reservoir’ effect based solely on the 14C wiggle-matching of bulk sediment samples.

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399

S06-P-193

HIGH RESOLUTION RESERVOIR AGE RECONSTRUCTIONS FROM COLD-WATER CORALS IN THE NORTH-EASTERN ATLANTIC DURING THE HOLOCENE (~ 1700 - 4800 CAL YR BP)

DOUARIN M.(1), ellIoT M.(1), MoReTon S.G.(2), SInclaIR D.(3), noble S.R.(4), lonG D.(5), RobeRTS J.M.(6)

(1) The univerity of edinburgh, eDInbURGH, UnITeD KInGDoM;(2) neRc Radiocarbon facility (environment), eaST KIlbRIDe, UnITeD KInGDoM;(3) Marine biogeochemistry & Paleoceanography Group, Institute of Marine and coastal Sciences, Rutgers University, neW bRUnSWIcK, UnITeD STaTeS;(4) neRc Isotope Geosciences laboratory, british Geological Survey, KeYWoRTH, UnITeD KInGDoM;(5) british Geological Survey, eDInbURGH, UnITeD KInGDoM;(6) centre of Marine biodiversity & biotechnology, School of life Sciences, Heriot-Watt University, eDInbURGH, UnITeD KInGDoM

AbstractCoupled U-series and radiocarbon dating were performed on cold-water corals (lophelia pertusa) from the North-eastern Atlantic. The coral fragments come from 2 sediment cores (+56-08/929VE and +56-08/930VE with 3.61 m and 5.25 m recovery, respectively) retrieved from shallow inshore coral reefs from the Mingulay Reef Complex (~56°N, 7°W and 120-190 m water depth).The 40 U-series dates show that coral fragments within the cores are in chronological order and span the mid-late Holocene (1700 - 4800 yr BP). The sediment cores show exceptionally high accumulation rates around 5 - 6 mm yr-1 which is higher than those estimated for reefs along the Norwegian shelf (2 - 3 mm yr-1) and an order of magnitude greater than from the coral carbonate mounds of the European continental margin (~ 0.2 mm yr-1 for the Holocene).Reservoir ages were reconstructed from 18 paired U-series and 14C dates measured on the same coral fragments. This high resolution dating, about one analysis every 150 yrs, allows reconstructions of high frequency changes in ventilation and ocean circulation patterns in this region. The reservoir ages estimated range from 170 yrs to 630 yrs with a mean value around 360 years. Our results also suggest cyclic circulation changes in the North-eastern Atlantic: 3 periods, around 2800, 3400 and 3750 yr BP are characterized by lower values 208, 171 and 215 yr, respectively. One prominent increase of reservoir age is observed at about 3250 yr BP with values reaching 629 yr. The lower reservoir ages are relatively well correlated with lower δ18O values recorded by planktonic foraminifer G. bulloides and reduced coral reef accumulation rates within the Mingulay Reef Complex.This study suggests that cyclic circulation changes occurred in the North-eastern Atlantic during the mid-late Holocene every 400 - 500 yrs. Further studies with records of similar resolutions would be needed to determine if these changes in reservoir ages are related to local and/or global environmental changes. This study demonstrates that cold-water corals constitute a powerful alternative to provide accurate reservoir ages with unprecedented temporal resolutions.

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400

SESSION 7

RADIOCARBON DATING AND THE PALAEOLITHIC

ConvenersC. Barshay-Szmidt (CA), N Conard (DEU), T. Higham (GBR), H. Valladas (FRA)

DescriptionRadiocarbon dating of material covering the Middle and early Upper Palaeolithic is very challenging. Even small amounts of contamination affect dating reliability. Dating is, however, crucially important if we are to understand important issues relating to modern human dispersals. How can we improve this situation? This session will be concerned with developments in the reliable dating of material from MOIS3 in Eurasia, the sub-continent and Africa (Middle and Late Stone Age). This will include improvements in laboratory and archaeological/field methodology (pre-screening, pre-treatment, methods to select samples from the least disturbed zones and well linked to human activity) and the interpretation of results, laboratory intercomparison issues, background corrections and the development of novel sample types that offer improvements in reliability. Papers could also embrace the question of previous results and their reliability. Papers discussing recent results from the period and their archaeological significance will also be welcomed. For instance, including such improvements may have had an impact on the dates of a particular site, affected a regional chronological framework or had implications as to potential interaction, dispersals or links between industries.

KeywordsPalaeolithic, MOIS 3, pretreatment chemistry, background corrections, contamination, measurement reliability, sample selection criteria for radiocarbon dating, Eurasia, Africa.

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S07-P-194

DYNAMICS OF SIBERIAN PALAEOLITHIC COMPLEXES (BASED ON ANALYSIS OF RADIOCARBON RECORDS): THE 2012 STATE-OF-THE-ART

KUZMIN Y.(1), KeaTeS S.G.(2)

(1) Institute of Geology and Mineralogy, noVoSIbIRSK, RUSSIan feDeRaTIon;(2) [email protected], lonDon, UnITeD KInGDoM

AbstractThe corpus of 14C dates from Siberian Palaeolithic sites as of late 2011 includes ca. 800 values. After thorough evaluation based on the «chronometric hygiene» principal, about 19% of the 14C values were rejected mainly due to: 1) inversions in age-depth profiles; 2) infinite ages (greater than); 3) uncertainties of association with cultural components and lack of documentation; and 4) dating of megafauna from mass accumulations («mammoth cemeteries») often only very loosely related to human presence. About 650 reliable 14C dates are used for the updated reconstruction of the Palaeolithic population dynamics in Siberia. The approach follows Kuzmin & Keates (2005), and occupation episodes were counted for the time span of ca. 49,000-10,000 BP.Compared to our previous study (Kuzmin & Keates 2005), several new features can be detected: 1) at ca. 32,000-21,000 BP, the intensity of occupation is higher (average 12.3 episodes per 1000 yrs) than in the 2005 analysis (average value 7.9); 2) the almost exponential increase in occupation began at ca. 20,000 BP (compared to ca. 16,000 BP); and 3) no clear decrease in occupations is observed for the Last Glacial Maximum (LGM), neither in the narrow (ca. 20,000-18,000 BP) nor broader (ca. 22,000-16,000 BP) sense of the LGM duration.The distribution of raw 14C dates mainly follows frequencies of occupation episodes. However, for some 1000 yr slices, definite artefacts are observed: there is a very high number of 14C dates for ca. 28,000-27,000 BP (36 values) and ca. 22,000-21,000 BP (28 values). This «phenomenon» is due to a large extent to the 14C dates generated for the Yana RHS (the former slice) and Malta (the latter one) sites, compared to far less 14C dates for the adjacent 1000 yr spans. Occupation frequencies for these time periods are 16 and 14, respectively. It is clear that in order to avoid an artificial increase in the frequencies of 14C dates, the normalisation of initial 14C records is necessary, and an occupation episode approach (sensu Kuzmin & Keates 2005) seems to be feasible in this respect.Concerning the correlation between occupation frequencies and climatic fluctuations at ca. 53,000-11,000 cal BP (GISP2 Greenland ice core records and Lake Baikal core), no direct correspondence is observed. For example, a steady rise in occupations is typical for ca. 40,000-30,000 cal BP, despite several large climatic fluctuations. The peak at ca. 32,000-31,000 cal BP does not correspond to either a warm (Dansgaard-Oeschger event) or cold (Greenland stadial) interval. At the LGM, ca. 26,000-19,000 cal BP, there is a relatively stable population (average occupation frequency: 10.7 per 1000 yr), with a minimum at ca. 24,000-23,000 cal BP (6 occupations). Therefore, the relationship between climate and Palaeolithic humans in Siberia was nonlinear as suggested earlier (e.g. Fiedel & Kuzmin 2007).

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S07-P-195

NON-DESTRUCTIVE PORTABLE TECHNIqUES FOR CARBON IN-SITU SCREENING IN PREHISTORIC ROCK PAINTINGS

BECK L.(1), GenTY D.(2), TeReYGeol f.(3), laHlIl S.(4), lebon M.(5), ReIcHe I.(4), VIGnaUD c.(4), laMbeRT e.(4), VallaDaS H.(6), PlaSSaRD f.(7), MenU M.(4), PaIlleT P.(5)

(1) cea, GIf SUR YVeTTe, fRance;(2) lSce-cnRS, GIf SUR YVeTTe, fRance;(3) laPa-cnRS, GIf SUR YVeTTe, fRance;(4) c2RMf, PaRIS, fRance;(5) MnHn, PaRIS, fRance;(6) lSce-cea, GIf SUR YVeTTe, fRance;(7) GRoTTe De RoUffIGnac, RoUffIGnac, fRance

AbstractDirect dating of prehistoric paintings is playing a major role in Palaeolithic art studies. Very few figures can be directly dated since the necessary condition is that they contain organic carbon-based material. Furthermore, it seems to be very important to check the presence of organic carbon-based material in situ before sampling in order to protect the visual integrity of the paintings or drawings.We have tested and compared three different portable analytical systems which can be used in cave environment for detecting carbon in prehistoric paintings.The first one is a commercial X-ray fluorescence (XRF) system (Niton XL3). This handheld XRF analyzer is very compact, uses rechargeable battery and is consequently very well adapted in cave environment. Elemental analysis can be performed in a few minutes and elements from Ni to U can be detected. The possible presence of C is deduced from the absence of Mn in black figures. This portable XRF has been used in the Villars cave (Dordogne, France) on black spots and drawings in order to select samples suitable for 14C dating. Radiocarbon results were obtained from five torch spots: two of them gave ages of 17.1-18.0 and the three others, ages of 20.4-22.1 ka cal. BP (D. Genty et al., this conference).The second system is a commercial portable micro-Raman spectrometer(Jobin-Yvon Horiba). The measurements were performed without contact thanks to a 50x Nikon long-working-distance objective. This technique is very sensitive to carbon by emitting two intense bands at 1390 and 1590 cm-1. Raman spectrometry has the advantage to directly detect and distinguish mineral and organic carbon-based materials. The device is relatively heavy (60 kg) but easily portable. Contrary to the previous system, it needs power supply. Black figures (mammoths, rhinoceros) and a black line crossing a mammoth on the «Grand Plafond» were investigated in the Rouffignac cave (Dordogne, France) in order to identify possible carbon-based drawings. Carbon signals have been measured only in the line and in some microscopic contaminations. All the prehistoric figures have been revealed to be drawn with manganese oxides and direct radiocarbon dating remains impossible.In the same cave, a small portable camera for infrared (0.9 - 1.7µm) reflectometry has also been tested. This camera provideshigh-resolution, high-speed images revealing differences between carbon and manganese pigments.In conclusion, these various portable systems have successfully demonstrated their capabilities to identify carbon in pigments. These carbon screening methods can be applied in situ, in various types of environments, even in sites of high humidy such as prehistoric caves.

This study was partially funded by the french Research agency (anR) in the framework of the MaDaPca project.

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S07-P-196

DATING THE VILLARS CAVE PREHISTORIC OCCUPATION AND PAINTINGS (SOUTH-WEST FRANCE) - MULTIDISCIPLINARY APPROACH AND COMPARISON WITH PALEOCLIMATIC CONTEXT

GENTY D.(1), VallaDaS H.(1), becK l.(2)(3), TeReYGeol f.(4), DellUc b.(5), DellUc G.(5), HellSTRoM J.(6), blaMaRT D.(1), KalTnecKeR e.(1), MoReaU c.(7), DUMoUlIn J.P.(7)

(1) lSce - cnRS, GIf-SUR-YVeTTe, fRance;(2) cea, Den, Service de Recherches de Métallurgie Physique, laboratoire JannUS, GIf-SUR-YVeTTe, fRance;(3) centre de recherche et de restauration des Musées de france (c2RMf), Palais du louvre, 14 quai f. Mitterrand, PaRIS, fRance;(4) laPa SIS2M UMR 3299 cea-Saclay, SaclaY, fRance;(5) Département de Préhistoire du Muséum national d’Histoire naturelle, UMR 7194 du cnRS (Histoire naturelle de l’Homme préhistorique), PaRIS, fRance;(6) School of earth Sciences, The University of Melbourne, VIc 3010, MelboURne, aUSTRalIa;(7) laboratoire de Mesure du carbone 14, UMS 2572, cea, GIf-SUR-YVeTTe, fRance

AbstractThe Villars Cave, a South-West France 10km long karstic network, possesses several prehistoric paintings and human remains whose ages, until now, were not precisely known. Except for one 14C dating result made on a burned bones fifteen years ago (16480 ± 210 years 14C BP, unpublished) and chronological hypotheses based on the painting style (looking like Lascaux) and the few tools found on the floor (Delluc and Delluc, 1974), no other dating investigation have been made so far. About 60 km far from the Lascaux Cave and close to several well studied prehistoric sites, the Villars Cave is part of this SW-France caves network where fundamental findings have been made since the XIXth century. Therefore a better knowledge of the human occupation chronology in this cave appears of first importance. We present here dating results obtained on human occupation evidences like charcoals and reindeer bones collected on the floor and black torch spots found on the walls; we also dated by the U series and C-14 methods speleothems that grew on stalagmites (which were possibly broken by prehistoric men) and on the archaeological level. The prehistoric drawings found in this cave depict 1 man and some animals (7 horses, 3 bison, 3 ibex, 1 rhinoceros), geometrical signs, punctuationsand lines made with black matter whose composition was not known everywhere. Our approach was first to check, using a portable X-ray fluorescence apparatus (see Beck et al., this conference), if this black material contains manganese or not. This allowed us to sort out carbon-based figures for which 14C analyses were made. Radiocarbon results spread between 17.1 and 23.2 ka cal BP: black torch traces on walls display two sets of ages, one at 17.1-18.0 and the other one at 20.4-22.1 ka cal BP, the bone ages also display two sets, at 18.9-20.2 and 21.5-23.2 ka cal BP.The Villars dating results are discussed and replaced in a regional paleoclimatic context which was reconstructed thanks to stable isotopes analysis and uranium-thorium dates on stalagmites from the same cave (Genty, 2008). We observe that the Villars prehistoric human presence occurred during the coldest period of the last 50 ky, as testified by the growth hiatus observed between 30 and 16 ka in many stalagmites from the cave, due to the stop of infiltration because of frost. The charcoals found near the discovery entrance, 0.8 ka cal. BP old, likely fell from the close surface through fissures during a forest fire of the medieval period.This study was partially funded by the French Research Agency (ANR) in the framework of the MADAPCA project.

References1. Delluc, B., and Delluc, G. (1974). La grotte ornée de Villars. Gallia Préhistoire17, 1-67.2. Genty, D. (2008). Palaeoclimate Research in Villars Cave (Dordogne, SW-France). International Journal of

Speleology 37, 173-191.

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S07-P-197

RADIOCARBON DATING UPPER PALAEOLITHIC MODERN HUMANS USING THE AMINO ACID HYDROXYPROLINE

MAROM A.(1), MccUllaGH J.S.o.(1), HIGHaM T.f.G.(1), SInITSYn a.a.(2), HeDGeS R.e.M.(1)

(1) University of oxford, oXfoRD, UnITeD KInGDoM;(2) Institute of the History of Material culture, Russian academy of Sciences, ST. PeTeRSbURG, RUSSIan feDeRaTIon

AbstractRadiocarbon dating of Palaeolithic bones has frequently resulted in severe underestimates of the real age, but direct dating of Neanderthal and modern human fossil remains is crucial in order to understand the mechanics of the extinction of the former and the initial wide dispersal of the latter. Here we report the application of the previously described method for radiocarbon dating bones using the amino acid Hydroxyproline [1] to bones from the key sites of Sungir and Kostenki in Russia. The Kostenki 14 (Markina Gora) human skeleton was excavated near Voronezh, Russia. Whilst the specimen is strongly suspected of being Palaeolithic in age, direct radiocarbon dates are much younger (~3.7-13.6 ka BP). The Kostenki bone C:N atomic ratios are outside the usual thresholds, indicating exogenous carbon. We extracted bone powder from the right tibia of the skeleton and attempted a new direct date using the Hyp method. The resulting date of 33,250 ± 500 BP is in excellent agreement with its chrono-stratigraphic position. At Sungir, another key Russian Upper Palaeolithic site, several spectacular burials were excavated. Direct radiocarbon dating of three of the skeletons was attempted previously in Oxford, Arizona and Kiel, but the results were highly inconsistent, both between the laboratories and between the different individuals dated. Using the Hyp method we dated two of the skeletons that were interred in same grave, as well as a mammoth bone that came from the same occupation area. The new dates are consistent with a single event as expected archaeologically, and together with the Kostenki 14 date are the earliest direct ages for the presence of anatomically modern humans on the Russian Plain.The new Upper Palaeolithic dates presented here contribute greatly to our understanding of human dispersals during this, and the subsequent Gravettian period. In addition, they demonstrate the power of the method to provide reliable chronologies and help resolve longstanding archaeological questions.

References[1] McCullagh, J. S. O., A. Marom, R .E. M Hedges (2010). «Radiocarbon dating of individual amino acids from archaeological bone collagen.» Radiocarbon 52(2): 620-634.

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S07-P-198

INTERPRETING RADIOCARBON DATES FROM THE PALAEOLITHIC LAYERS OF THE THEOPETRA CAVE IN THESSALY, GREECE

FACORELLIS Y.(1), KaRKanaS P.(2), HIGHaM T.(3), bRocK f.(3), nTInoU M.(4), KYPaRISSI-aPoSTolIKa n.(2)

(1) laboratory of Physico-chemical Methods and Techniques, faculty of fine arts and Design, Department of antiquities and Works of art conservation, Technical educational Institute of athens, aghiou Spyridonos, 12210 egaleo, aTHenS, GReece;(2) ephorate of Palaeoanthropology and Speleology of Southern Greece, ardittou 34b, 116 36, aTHenS, GReece;(3) oxford Radiocarbon accelerator Unit, Research laboratory for archaeology and The History of art, Dyson Perrins building, South Parks Rd, oX1 3QY, oXfoRD, UnITeD KInGDoM;(4) Hellenic open University, PaTRa, GReece

AbstractThe long known Theopetra cave (21°40’46’’E, 39°40’51’’N) is a unique prehistoric site for Greece, as the Middle and Upper Palaeolithic, Mesolithic and Neolithic periods are present here, bridging the Pleistocene with the Holocene.During the more than twenty years of excavation campaigns, evidence of human activity, such as charcoal samples from hearths suitable for 14C dating were collected from all anthropogenic layers, including the Palaeolithic ones. Most of the samples were initially dated in the Laboratory of Archaeometry of NCSR «Demokritos». The removal of any carbon compounds of non-archaeological origin was performed there using the ABA chemical pre-treatment. Then they were converted to CO2 and conventionally measured inside cylindrical gas proportional counters.The 14C results showed that the earliest limit of human presence probably exceeds 48,000 years BP, thus reaching the age limits of the radiocarbon dating method. However, ten burnt flint specimens unearthed in the II4 layer, corresponding to the lower part of the Middle Palaeolithic sequence of Theopetra cave, which have been dated by the TL method gave ages ranging between ca. 110 and 135 ky ago. In addition one burnt flint from layer II11 gave a TL age of ca 57 ky ago. These results are in disagreement with the 14C dates, which support a much later date for the Middle Palaeolithic layers.In order to clarify the situation further 14C dating of hand-picked charcoal fragments from layers II4 to II11 identified by anthracological analysis for the wood species were also radiocarbon dated by AMS in the Oxford Radiocarbon Accelerator Unit using the acid-base-wet oxidation (ABOx) pretreatment and analytical protocol.The purpose of this study is to present all the 14C dates from the Theopetra cave Palaeolithic layers obtained by both laboratories and discuss the implications of a probable charcoal diagenesis to the radiocarbon results of these very old samples.

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S07-P-199

CHRONOLOGY OF THE EARLY UPPER PALAEOLITHIC SITE MARKINA GORA (KOSTIENKI AREA, CENTRAL RUSSIA) BASED ON PAIRED ABA AND ABOX DATES.

HAESAERTS P.(1), DoUKa K.(2), SInITSYn a.a.(3), DaMblon f.(1), HIGHaM T.(2), PIRSon S.(4), Van DeR PlIcHT J.(5)(6)

(1) Royal belgian Institute of natural Sciences, bRUSSelS, belGIUM;(2) oxford Radiocarbon accelerator Unit, Research laboratory for archaeology and the, oXfoRD, UnITeD KInGDoM;(3) Institute for the History of the Material culture, ST. PeTeRSbURG, RUSSIan feDeRaTIon;(4) Service Public de Wallonie DG04, naMUR, belGIUM;(5) centre for Isotope Research, University of Groningen, GRonInGen, neTHeRlanDS;(6) faculty of archaeology, leIDen, neTHeRlanDS

AbstractLocated along the western slope of the Don Valley, south of Voronezh, the Upper Palaeolithic site of Markina Gora (Kostienki 14) has provided one of the best documented Middle to Late Pleniglacial pedosedimentary successions in Central Russia. The record encompasses several cultural layers, from Gravettian to early Upper Palaeolithic, as well as two independently dated markers: the Campanian ash, related to an Aurignacian assemblage and the Laschamp event recorded in between the cultural layers IVa and IVb (Sinitsyn, 1996; Velichko et al, 2009). The chronological background of the Markina Gora sequence has been based on a long series of radiocarbon dates on charcoal ranging from 23 to ca 38 ka uncal BP mainly produced during the last decades in the Groningen laboratory, but some of the ages were undoubtedly underestimated regarding their stratigraphic context (Haesaerts et al., 2004; Sinitsyn, Hoffecker, 2006). In order to reinforce the chronological background of the sequence a set of paired dating was produced recently in the Oxford laboratory, applying ABA and ABOx methods on charcoal samples previously dated prior to 30 ka BP in Groningen (Douka et al., 2010, Wood et al. in press). This complementary approach allows the establishment of a consistent correlation scheme with the Greenland ice sequence, in good agreement with the inferred radiocarbon chronology of the Campanian ash and the Laschamp event as recorded at Markina Gora.

Acknowledgments

The loess research in Kostienki is a contribution to the Sc-09 and MO/36/021 research projects of the Belgian Science Policy, with complementary funding from the INTAS 2000-879 research project. The Oxford dates were funded by a NRCF-NERC grant (NF/2009/1/19); we are grateful to Rachel Wood and Fiona Brock for processing the samples.

References1. Douka, K., Higham, T., Sinitsyn, A.A., 2010. The influence of pretreatment chemistry on the radiocarbon dating of Campanian Ingnimbrite-aged charcoal from Kostienki 14 (Russia). Quaternary Research, 73(3), 583-587. 2. Haesaerts, P., Damblon, F., Sinitsyn, A.A., van der Plicht, J., 2004. Kostienki 14 (Voronezh, Central Russia): new data on stratigraphy and radiocarbon chronology, Acts of the XIVth UISPP Congress (Liège, 2001), BAR International Series Oxford, 1240, 169-180. 3. Sinitsyn, A.A., 1996. Kostienki 14 (Markina Gora): data, problems and perspectives. Préhistoire Européenne Liège, 9, 273-313. 4. Sinitsyn, A.A., Hoffecker, J.F., 2006. Radiocarbon dating and chronology of the Early Upper Paleolithic at Kostenki.Quaternary International, 152-153, 164-174. 5. Velichko, A.A., Pisareva, V.V., Sedov, S.N., Sinitsyn, A.A., Timireva, S.N., 2009. Palaeogeography of Kostienki-14 (Makina Gora). Archaeology, Ethnography & Anthropology of Eurasia, Elsevier, 37 (4), 35-50. 6. Wood, R.E., Douka, K., Boscato, P., Haesaerts, P., Sinitsyn, A., Higham, T.F.G. Testing the ABOx-SC method: dating known age charcoals associated with the Campanian Ignimbrite. Quaternary Geochronology, in press.

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S07-P-200

RADIOCARBON DATING THE EARLIEST UPPER PALAEOLITHIC OF THE IBERIAN PENINSULA

WOOD R.(1)(2), aRRIZabalaGa a.(3), beRnalDo De QURIoS f.(4), caMPS M.(5), foRTea J.(6), IRIaRTe M.J.(3), MaRoTo J.(7), De la RaSIlla M.(6), SanTaMaRIa D.(6), SoleR J.(7), SoleR n.(7), HIGHaM T.(2)

(1) australian national University, canbeRRa, aUSTRalIa;(2) University of oxford, oXfoRD, UnITeD KInGDoM;(3) Universidad del País Vasco, VIToRIa, SPaIn;(4) Universidad de leon, leon, SPaIn;(5) George Washington University, WaSHInGTon, UnITeD STaTeS;(6) Universidad de oviedo, oVIeDo, SPaIn;(7) Universitat de Girona, GIRona, SPaIn

AbstractLike much of Europe, the study of the Middle to Upper Palaeolithic transition of the Iberian Peninsula has been hindered by an inaccurate and imprecise radiocarbon chronology. On typological grounds, the Peninsula can be divided into northern and southern regions. To the north, the transition appears broadly similar to the rest of Western Europe. The Châtelperronian, a ‘transitional’ complex whose authors are not securely known, is followed by the Proto and Early Aurignacian techno-complexes, probably produced by modern humans. In addition, a second transitional industry, the Transitional Aurignacian, is found in Cantabria. However, debates still rage over whether this industry is ‘real’ or whether it is an illusion created by a palimpsest. To the south, these early Upper Palaeolithic industries are absent, and the later Evolved and Late Aurignacian techno-complexes are scarce.This paper will discuss the implications of new radiocarbon dates on ultrafiltered collagen from L’Arbreda, Labeko Koba, La Viña and El Castillo for:* the timing of the early Upper Palaeolithic industries in the north* the reality of the Transitional Aurignacian* the timing of the arrival of modern humans in the south* reasons why modern humans appear later in the south than the north of the Peninsula

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S07-P-201

NEW DATES FOR THE MIESENHEIM IV ELK (RHINELAND, GERMANY): AN INTER-LABORATORY TEST OF COLLAGEN DATING PROTOCOLS

FIEDEL S.(1), KUZMIn Y.(2), STReeT M.(3), Van DeR PlIcHT J.(4), HIGHaM T.(5), TaYloR R.e.(6), SoUTHon J.(7), naDeaU M.J.(8)

(1) louis berger Group, RIcHMonD, UnITeD STaTeS;(2) Institute of Geology & Mineralogy, Siberian branch of the Russian academy of Sciences, noVoSIbIRSK, RUSSIan feDeRaTIon;(3) Romisch-Germanischen Zentralmuseum, neUWIeD, GeRManY;(4) centre for Isotope Research, University of Groningen, GRonInGen, neTHeRlanDS;(5) oxford Radiocarbon accelerator Unit, University of oxford, oXfoRD, UnITeD KInGDoM;(6) Department of anthropology, University of california, Riverside, RIVeRSIDe, ca, UnITeD STaTeS;(7) Keck carbon cycle aMS laboratory, University of california-Irvine, IRVIne, ca, UnITeD STaTeS;(8) leibniz-labor, christian-albrechts University, KIel, GeRManY

AbstractRadiocarbon dating of bone samples continues to be problematic. As the true age of a sample usually is unknown, it is difficult to evaluate the accuracy of dating results. Various laboratories currently use different pretreatment methods to extract collagen. The relative efficacy of these techniques has not been tested. Fiedel and Kuzmin (2010) proposed a new, independent inter-lab test of the reliability and reproducibility of collagen-based dates for Late Glacial fauna. We suggested re-dating of the Miesenheim IV elk (alces alces), one of the rare samples of known age (terminus ante quem in this case). This nearly complete skeleton from the Rhineland in Germany was buried, soon after the animal’s death, by tephra from the Laacher See volcanic eruption (LST). This eruption occurred ~ 13,050 years cal BP (200 years prior to the onset of the Younger Dryas episode). Previously, three samples of the elk were dated at Oxford’s ORAU Lab, with a mean age of 11,230 ±55 BP (Hedges et al. 1993:149-50). However, tree-ring dates now suggest a radiocarbon age of ~11,060 BP for the LST. New samples of elk bone have been processed and AMS-dated by Groningen, Kiel, University of California-Irvine, and Oxford laboratories. Here we report preliminary results and discuss their implications.

ReferencesFiedel SJ, Kuzmin YV. 2010. Is more precise dating of Paleoindian expansion feasible? Radiocarbon 52:337-45.Hedges REM, Housley RA, Bronk Ramsey C, van Klinken GJ. 1993. Radiocarbon dates from the Oxford AMS System: Archaeometry Datelist 16. Archaeometry 35:147-67.

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S07-P-202

CAN WE USE CALCINED BONES TO RADIOCARBON DATE THE PALAEOLITHIC?

ZAZZO A.(1), lebon M.(2)(3), neSPoUleT R.(4), cHIoTTI l.(4), ReIcHe I.(2)(3)

(1) UMR 7209 cnRS / MnHn, PaRIS, fRance;(2) UMR 171 cnRS - c2RMf, PaRIS, fRance;(3) UMR 8220 cnRS / UPMc, IVRY-SUR-SeIne, fRance;(4) UMR 7194 cnRS / MnHn, leS eYZIeS-De-TaYac, fRance

AbstractBurnt bones are frequently found in archaeological records and provide an important source of information on human activities (e.g., cooking, fuel management, or burial practices). The composition and structure of bone is modified during combustion: the organic phase (lipids, collagen) is degraded at low temperature (<300°C), while the mineral phase is reorganized above 600°C. This recrystallisation of biological apatites makes the structural carbonate of calcined bones particularly resistant to post-burial alteration. Recent work has shown convincingly that the inorganic carbon of calcined bones provides a reliable support for 14C dating. These results were obtained on relatively recent (Holocene) sites, and until today, no data is available for older (Palaeolithic) samples. To test the reliability of calcined bones through deep time, we dated a series of calcined bones coming from the site of the Abri Pataud (Dordogne, France). The Abri Pataud site is perfectly suited for this purpose for different reasons: it provides a key archaeological sequence for the upper Palaeolithic in Europe; it presents a rich stratigraphic sequence containing 14 archaeological layers from the Aurignacian to the Gravettian; recent radiocarbon dating programme has provided a coherent and reliable chronologyfor this site (Higham et al 2011).A special attention was paid to sample selection prior to analysis. Fifty-eight samples were selected in the Museum collection on the basis of their macroscopic features (colour, presence of calcination cracks). These samples were then analysed by FTIR spectroscopy and stable isotope mass spectrometry. For each sample, the heating state was determined on the basis of bone crystallinity (splitting factor SF) and δ13C value. Samples showing higher SF and lower δ13C values were considered to have been exposed to higher temperatures, and were thus expected to be the best candidates for 14C dating. Unheated samples and samples with intermediate SF and δ13C values were also selected for comparison. In total, 23 samples coming from four different levels dated between 22 and 33 000 years BP were prepared for radiocarbon dating.The comparisonbetween the dates obtained in this study and the recently published dates for the same levels will allow us to assess the potential of calcined bones for 14C dating of the Upper Paleolithic.

ReferencesHigham, T.F.G., Jacobi, R.M., Basell, L., Bronk Ramsey, C., Chiotti, L. and Nespoulet, R. 2011. Precision dating of the Palaeolithic: A new radiocarbon chronology for the Abri Pataud (France), a key Aurignacian sequence. Journal of Human Evolution 61(5): 549-563.

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S07-P-203

CONTINUITIES AND DISCONTINUITIES IN THE EAST EUROPEAN UPPER PALAEOLITHIC ACCORDING TO RADIOCARBON CHRONOLOGY: THE KOSTENKI MODEL

SINITSYN A.

Inst.for the History of Material culture, SaInT-PeTeRSbURG, RUSSIan feDeRaTIon

AbstractThe radiocarbon database for the East European Upper Paleolithic, which comprises more than 1100 dates, provides a basis for identifying phases characterized by gradual colonization of the landscape and periods when the human population was almost entirely absent.The predominance of single-component open-air sites on the Russian Plain precludes evaluation of absolute dates by stratigraphic sequence or relative chronology. For more than 50 years, two sequences based on multi-layered sites have been critical for the East European Upper Palaeolithic: Molodova and Kostenki. The principal focus of this paper is the chronology at Kostenki (or «Kostenki model»), which differs from Molodova because it is based on sequences at a number of sites that mutually complement and correct each other.The more than 250 dates and their ranges for the Kostenki Upper Paleolithic (UP) may be grouped by associated cultural units into four chronological groups as follows:I - Initial UP-stratum: Spitsynean and Kostenki 14 (IVb): 42 (?) - 40 /kaCal/ (37-36 nonCal);II - Early UP: Aurignacian and a local transitional culture, Streletskian: 40 - 37 /kaCal/ (36-32 nonCal);III - Early Gravettian and a local East European culture, Gorodtsovian: 32 - 30 /kaCal/ (29-27 nonCal);IV - Recent Gravettian together with assemblages of non-Gravettian attribution: 28 - 24 /kaCal/ (24-20 nonCal).The radiocarbon chronology may be evaluated in terms of internal consistency and degree of variability, as well as with respect to other sources of information on chronology (e.g., stratigraphy, palynology, paleomagnetism, OSL dating). A wide range of dates, obtained at different stages in the development of the radiocarbon method, on different materials, and in different laboratories, often is characteristic of a single cultural layer, and there is no basis for preferring one date over another. When considered in the context of other sources of information on chronology, however, the oldest dates on an individual cultural layer generally appear to be more accurate. Additional criteria for evaluating dates have been developed in recent years with new methods of sample pretreatment.Major issues that require attention in the Kostenki model include: (a) the problem of a temporal gap at 27-24 ka /nonCal/, and (b) the question of an absence of population during the LGM period at Kostenki.(grant rfbr:11-06-12007-ofi-m-2011)

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S07-P-204

RADIOCARBON CHRONOLOGY OF THE EAST EUROPEAN GRAVETTIAN

BESSUDNOV A.

Institute for the History of material culture, Russian academy of Science, SaInT-PeTeRSbURG, RUSSIan feDeRaTIon

AbstractThis paper addresses the problem of the 14C chronology of the East European Gravettian as a basis for reconstruction of human population dynamics. In the past, 14C dates were used to support or critique interpretations of archaeological data. The situation has changed during the last decade owing to the volume of dates. Archaeological chronology has gradually been transformed into 14C chronology, and the latter has acquired an independent existence. 14C dates must be evaluated, nevertheless, by statistical criteria and by their stratigraphic context.Statistically meaningful samples are not common and chiefly available for settlements of the Kostenki-Avdeevo culture (e.g., Kostenki 1(I), Avdeevo, Zaraysk). The distribution of the dates provides evidence of the lower temporal boundary, while the upper boundary is difficult to determine because of the wide scatter of younger dates.The earliest Gravettian appearedon the Russian Plain abruptly at 29-28 ka (Kostenki 8(II), Mezhigirtsy, Buran-KayaIII (17-18)), almost simultaneously with the West and Central European Early Gravettian (Geissenklösterle (Ia/Ib), Maisieres-canal, Temnata cave (3d), etc.). The Early Gravettian disappeared at 26 ka. It probably had no connection with later Gravettian industries.In the Late or Evolved Gravettian, dated to 24-20 ka, at least seven variants of the technocomplex are recognized. Some could represent various phases of one or more cultures. The question of whether they represent successive or coexisting entities remains controversial. Three variants (Kostenki 21(III), 11(II), Borshchevo 5(I) - Kostenki 9) have been identified only at Kostenki. The most widespread is the Kostenki-Avdeevo culture. The temporal boundaries, based on 14C dates, for sites of this culture (Kostenki 1(I), 14(I), 18) extend from 25.5 to 14 ka. Statistical analysis indicates that dates in the interval of 24-21.5 ka probably are closest to the actual age of the culture. Comparative analyses of the distribution of 14C dates suggest that the occupation layer at Avdeevo is slightly younger than the Kostenki 1(I) occupation. Zaraisk is thought to be one of the most recent manifestations of the Kostenki-Avdeevo culture. Four occupation levels were identified at the site, the youngest of which dates to18-16 ka. Khotylevo 2 is coterminous with Kostenki 1(I) and probably indicates the earliest appearance of LateGravettian in the Desna basin. The site of Gagarino, often combined with Khotylevo 2 in one sub-cultural group, is slightly younger in age, and may be correlated with Pushkari 1. Although the other Gravettian sites lack representative 14C series, they could be not older than 23-22 ka.The main problem under discussion is the temporal relationship among these sites, and whether the occupations were simultaneous or diachronic. Neither 14C dating nor stratigraphy provides an adequate basis for resolving this problem.The research was supported by grant RFBR (11-06-12007-ofi-m-2011).

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S07-P-205

PENA CANDAMO CAVE (ASTURIES, SPAIN): NEW DATING OLD PROBLEMS

VALLADAS H.(1), KalTnecKeR e.(1), PonS bRancHU e.(1), TISneRaT laboRDe n.(1)(1), MoReaU c.(2), coRcHon S.(3), GaRaTe MaIDaGan D.(4), becK l.(5), bonnaIllIe P.(5), HeRnanDo alVaReZ c.(3), lebon M.(6), RIVeRo VIla o.(7)

(1) laboratoire des Sciences du climat et de l’environnement, GIf-SUR-YVeTTe, fRance;(2) laboratoire de mesure du carbone 14, GIf-SUR-YVeTTe, fRance;(3) Universitad de Salamanca, SalaManca, SPaIn;(4) Museo arqueologico de bizkaia, bIlbao, SPaIn;(5) cea/Den/SRMP -cen, GIf-SUR-YVeTTe, fRance;(6) MnHn, PaRIS, fRance;(7) cReaP, Univ. Toulouse, ToUloUSe, fRance

AbstractThe cave of La Peña (Candamo, Asturies) discovered at dawn of the XX century, contains one of the more significant sets of paleolithic parietal art of the Cantabrian region. Unfortunately, the cavity has undergone diverse processes of alteration due to its use as a refuge during the Spanish Civil War and its aggressive preparation to become a tourist operation. In 2008 the cave was declared a World Heritage site by UNESCO. That same year the integral study of the parietal art was undertaken under the direction of S. Corchón and D. Garate.In 1993 and 1997 parietal black pigments sampled by the late Pr. J. Fortea were AMS 14C dated. Samples taken independently in series of black points superimposed to two yellow aurochs and therefore presumably attributed to the same pattern were dated by the LSCE (Gif sur Yvette, France) and by the Geochron (Chelmsford,USA). Unexpectedlythe two laboratories obtained different results: 33,910 ± 840 and 32,310 ± 690 BP at the LSCE and 15,870 ± 90 and 15,160 ± 90 BP at the Geochron (Fortea, 2000/01). This disagreementwas tentatively explained by the scientific community (Pettitt, Bahn, 2003; Valladas, Clottes, 2003): the heterogeneous composition of the samples, the small amount of colouring matter available and their possible contamination by extraneous carbon due to alterations undergone by the cavity could be at the origin of the large dispersion of these results.Our current project of integral study of the cavity gives us the opportunity to revisit the chronological study of the palaeolithic occupation. In December 2011, black spots superimposed to the two yellow aurochs already studied were sampled for chemical composition analyses and for 14C AMS measurements. At the same time several speleothems formations were sampled for the U /Th method. The dating results so far obtained will be discussed in order to understand the discrepancy of the previous results and to determine when the cave of La Peña was occupied by prehistoric man.

References1. Pettitt P, Bahn P. 2003. Current problems in dating Palaeolithic cave art: Candamo and Chauvet. antiquity,

77(295).2. Valladas H, Clottes J,, 2003, Style, Chauvet and Radiocarbon, antiquity, 77(295).

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S07-P-206

DATING OF FRENCH AND SPANISH PREHISTORIC DECORATED CAVES IN THEIR ARCHAEOLOGICAL CONTEXTS

VALLADAS H.(1), KalTnecKeR e.(1), QUIleS a.(1), TISneRaT laboRDe n.(1), PaTeRne M.(1), aRnolD M.(2), MoReaU c.(3)

(1) laboratoire des Sciences du climat et de l’environnement, GIf-SUR-YVeTTe, fRance;(2) ceReGe, aIX en PRoVence, fRance;(3) laboratoire de mesure du carbone 14, GIf-SUR-YVeTTe, fRance

AbstractRadiocarbon dating of Paleolithic paintings and drawings remains exceptional firstly because of the conservation and preservation of parietal art concern and secondly becauseof the scarcity of organic pigments.Therefore the results are not numerous and are often challenged. Reservations concern the cave wall taphonomic evolution and especially the possible presence of extraneous organic materials which can contaminate the parietal representations and then distort the dating results. The temporal connection between the dated samples and the paintings’ or drawings’ realization period is another difficulty. How to be certain that the death of the tree, whose charcoals were being used by prehistoric man, is contemporaneous with the realization of the parietal representations?To discuss this recurrent question, the LSCE research’s program, in collaboration with the archaeological teams, combines the chronological studies of both the archaeological context and the direct dating of representations.Our purpose is to show how this multidisciplinary approach, including statistical analyses, allows us to obtain valuable chronological arguments about the parietal representations’ realization period. First, we will present the dates so far obtained in several French (Arcy-sur-Cure, La Bastide, Lascaux...) and Spanish (Garma, Nerja, La Pileta, Urdiales...) prehistoric caves and we will discuss the consistency of these results and their contribution to the evolution of Palaeolithic art knowledge.

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S07-P-207

BIśNIK CAVE (SOUTHERN POLAND) - THE RESULTS OF RADIOCARBON DATINGS OF THE MIDDLE PALAEOLITHIC CULTURAL LEVELS

SUDOł M., CYREK K., CZYżEWSKI L.

nicolaus copernicus University in Torun, ToRUn, PolanD

AbstractThe Biśnik Cave is located in Smoleń-Niegowonice Range, situated in the central part of the Kraków-Częstochowa Upland. The cave consists of several chambers joined by corridors, and several entrances. The Biśnik Cave is currently the oldest known cave site in Poland with a well-preserved sequence of sediments formed during a period of numerous climatic changes, starting with the time proceeding the Drenthe Glaciation to the Holocen. The most interesting Middle Palaeolithic sequence of the cave inhabitation comprises at least 17 cultural levels preserved in the form of stone and bone artifacts concentrations, hearth remains and fragments of post-consumptional animal bones.Due to the high value of the site, the attempts to establish the age of particular layers with the uranium-thorium, electronic paramagnetic resonance and thermoluminescence dating methods are crucial.The application of new technologies based on measurement of the age of collagen separated from bones allowed to achieve successive data for the youngest Middle Palaeolithic layers of Biśnik Cave. The correlation of new data with other absolute dating results provided valuable evidences for interpretation of the youngest settlement sequences of the site.Scientific value of the Biśnik Cave,enriched with the results of several methods of absolute dating, places that cave among the most important Middle Palaeolithic sites in this part of Europe.

ReferencesKrzysztof Cyrek, Paweł Socha, Krzysztof Stefaniak, Teresa Madeyska, Joanna Mirosław-Grabowska, Magdalena Sudoł, Łukasz Czyżewski, Palaeolithic of Biśnik Cave (Southern Poland) within the environmental background, Quaternary International, Volume 220, Issues 1–2, 15 June 2010, Pages 5-30, ISSN 1040-6182, 10.1016/j.quaint.2009.09.014. (http://www.sciencedirect.com/science/article/pii/S1040618209003115)

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S07-P-208

NEW STRATIGRAPHIC, CHRONOLOGICAL AND PALAEOENVIRON-MENTAL RESULTS FROM THE PALAEOLITHIC SEqUENCE OF BURAN KAYA III (CRIMEA, UKRAINE)

PUAUD S.(1), Van DeR PlIcHT J.(2), VallaDaS H.(3), DRUcKeR D.(4), cRÉPIn l.(1), PaToU-MaTHIS M.(1), YaneVIcH o.(5), PRaT S.(6), PÉan S.(1)

(1) Muséum national d’Histoire naturelle / UMR 7194 cnRS, PaRIS, fRance;(2) center for Isotope Research, Groningen University / faculty of archaelogy, leiden University, GRonInGen / leIDen, neTHeRlanDS;(3) laboratoire des Sciences du climat et de l’environnement / IPSl cea-cnRS-UVSQ, GIf-SUR-YVeTTe, fRance;(4) Department of Geosciences, University of Tübingen, TÜbInGen, GeRManY;(5) national academy of Sciences of Ukraine, archaeological Institut, KIeV, UKRaIne;(6) laboratoire Dynamique de l’evolution humaine, UPR 2147 cnRS, PaRIS, fRance

AbstractBuran-Kaya III is a rockshelter located in Crimea (Ukraine). Discovered in 1990, the site has been excavated by several international teams (Janevic, 1998; Chabai et al., 2004). It provides an exceptional stratigraphic sequence extending from the Middle Palaeolithic to the Neolithic. Nine Palaeolithic layers have been attributed to Szeletian, Micoquian, Aurignacian, Gravettian and Swiderian cultural traditions. The human remains from the richest Gravettian layer (6-1), directly dated to 31.9 ky BP, are among the oldest anatomically modern humans in Europe (Prat et al., 2011).The aim of this study is to present a palaeoenvironmental interpretation of the stratigraphic sequence of Buran-Kaya III based on the new geological data and radiocarbon dating. Since 2006, with the support of French programs (ANR, MNHN), new investigations have been carried on in the frame of a multiproxy approach: zooarchaeology, anthropology, techno-typology, geology, biogeochemistry and radiocarbon dating.During our new excavations (2009-2011), sediment, bones and teeth from each stratigraphical layer, were sampled for sedimentological, geochemical analyses and radiocarbon dating. Other osseous samples from 2001 excavations were also analysed. AMS 14C dating was both performed at the Center for Isotope Research of Groningen and at the Laboratoire des Sciences du Climat et de l’Environnement of Gif-sur-Yvette. Thus, several samples were cross-dated. The validity of the chemical parameters was evaluated by biogeochemical analyses of the collagen.The sedimentological analyses and micromorphological observations reveal a sequence of diamicton layers divided in two main sedimentary units. The lower part is characterized by limestone fragments and reduce unsorted silty matrix. In the upper part, coarse fraction is less abundant and the matrix is better sorted. This sequence could be interpreted as periglacial deposits under increasingly dry climatic conditions. These two units are separated by a cultural sterile level underlying the layer 6-1. It could be interpreted as a short cold and dry episode such as a Heinrich event.Sedimentological and chronological data are mutually consistent and agree to range the Palaeolithic human occupations at Buran-Kaya III during the end of MIS 3 and MIS 2. These results bring a new chronological and palaeoenvironmental framework for the human settlements in Eastern Europe during the late Middle and the Upper Palaeolithic.

References1. Janevic A, 1998 - Buran Kaya 3 Neue Angaben zur Kulturgliederung des Jungpaläolithikums des Krim.

Préhistoire européenne13: 133-148.2. Chabai VP, Monigal K & Marks AE, (eds) 2004 - The Middle Paleolithic and Early Upper Paleolithic of Eastern

Crimea. Liège: ERAUL 104: 482 p.3. Prat S, Péan S, Crépin L, Drucker D, Puaud S, Valladas H, Laznickova-Galetova M, van der Plicht J & Yanevich

A - The oldest anatomically modern human from far southeast Europe: direct dating, culture and behaviour. Plos one 6(6): e20834.

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S07-P-209

THE PALEOLITHIC AND RADIOCARBON DATING OF COLLAGEN: ADDING FLUORESCENCE TO THE MIX

TUROSS N.

Harvard University, caMbRIDGe, UnITeD STaTeS

AbstractIn Paleolithic vertebrate calcified tissue there is a well documented challenge in obtaining reliable radiocarbon dates from the major protein, collagen. Comparisons in decalcification methods, collagen isolation and molecular weight separation, as well as methods that characterize the resultant product (FTIR, C/N and amino acid analysis) provide a complicated matrix for analytical decisions. To the array of approaches and analyses, I’ll add fluorescent spectroscopy to address the issues of the less than 5% problem: current methods do not currently identify any nonproteinaceous carbon containing project that might be associated with collagen.

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S07-P-210

DATING THE UPPER PALAEOLITHIC LEVELS AT MANOT CAVE, ISRAEL: A SEALED CAVE AND A SEALED CONTEXT?

BOARETTO E.(1), baRZIlaI o.(1)(2), beRna f.(3), fRUMKIn a.(4), HeRSHKoVITZ I.(5), MaRDeR o.(2), baR-MaTTHeWS M.(6), WeIneR S.(1), YaSUR G.(6), YeSHURUn R.(7), SHaHacK-RoSS R.(1), GUR-aRIeH S.(8)

(1) Kimmel center for archaeological Science, Weizmann Institute of Science, ReHoVoT, ISRael;(2) Israel antiquities authority Pob 586, JeRUSaleM, ISRael;(3) MicroStratigraphy lab, Dept. of archaeology, boston University, boSTon, UnITeD STaTeS;(4) Department of Geography, The Hebrew University of Jerusalem, Mt. Scopus, JeRUSaleM, ISRael;(5) The Dan David laboratory, Sackler faculty of Medicine, Tel aviv University, RaMaT aVIV, ISRael;(6) Geological Survey of Israel, JeRUSaleM, ISRael;(7) Institute of archaeology, Zinman Institute of archaeology, University of Haifa, MoUnT caRMel, ISRael;(8) bar Ilan University, ReHoVoT, ISRael

AbstractManot Cave is an active speleothem cave with prehistoric remains in the western Galilee (Israel). The cave sealed by rock falls for thousands of years was discovered in 2008 during construction works. The cave has been subjected to an archaeologicalfield survey (2008) and two excavation seasons (2010-2011). To date the field work revealed a rich archaeological and human remains characteristic to the Middle Palaeolithic, Upper Palaeolithic and the Epi-Palaeolithic periods. Notable are the Upper Palaeolithic remains from excavation Area C where «Ahmarian» and «Aurignacian» traditionsof the Levantine Upper Palaeolithic were retrieved. As no later remains were recovered during the excavation, it seems that the cave was not inhabited after the Epi-Palaeolithic period.The cave entrances were indeed sealed by rock falls and clay-rich sediments forming a steep talus from there toward the center of the cave. The stratigraphy in the cave is therefore very complex since cultural elements (charcoal, stone tools and bones) were mixed with the intrusive soil. A dating strategy needed to be setup to determine the age of the settlement and artifacts.An integrative approach was adopted for the collection of 14C charred remains and bones based on sediments and material analysis to define the in situ nature of the samples. Associated flowstone and stalagmites were dated with U-Th. The 14C dates collected from archaeological horizons in Area C indicate a range between 35,000-38,000 Cal BP and the U-Th dates from the flowstone surfaces which sealed these horizons give a terminus ante quem from 35 to 26,000. All dates will be discussed with respect to the material cultural component in Area C (i.e. lithics, bone tools, groundstone tools, fauna etc.).

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SESSION 8

ARCHAEOLOGY - EURASIA AND AFRICA

ConvenersC.J. Bae (USA), H. Bocoum (SEN), m. Fontugne (FRA), Y. Kuzmin (RUS)

DescriptionDue to major advances in the application of radiocarbon dating methods and new archaeological discoveries in the past few decades, a number of significant changes have occurred in the Old World Holocene archaeological record. For instance, the meaning of the term “Neolithic” in archaeology has become more obscure. Pottery is now known in East Asia from the Terminal Pleistocene (ca. 14,800–13,300 BP) and associated with complex of hunter-fisher-gatherers. However, in the Levant it is generally accepted that agriculture preceded pottery-making. Other major contributions radiocarbon dating has provided prehistoric archaeology is a deeper understanding of the timing and nature of behavioral transitions (e.g., Neolithic-Bronze Age, Bronze Age-Iron Age, etc.), the spread of new technologies (e.g., diffusion of agriculture technologies across Europe, diffusion of iron metallurgy across Africa, both events that likely accompanied large scale human population movements), and the complex relationship between past climatic conditions, various ecological processes, and human activities.Our session aims to bring together archaeologists, radiocarbon specialists, palaeogeographers, and geoarchaeologists, to discuss recent findings in chronology and palaeoeconomy of a number of different topics currently being debated in Terminal Pleistocene-Holocene archaeology. For instance, presenters will discuss the earliest Neolithic (both pottery- and agriculture-bearing) complexes in Eurasia, in order to understand spatio-temporal patterns of the emergence of two key Neolithic phenomena (pottery and agriculture) and to understand the influence (or not) of climatic changes on these cultural transitions. Other speakers will present recent findings from other spatio-temporal points and topics (e.g., spread of plant and animal domesticates across regions like Africa and Europe and Oceania).

KeywordsOld World (Europe, Africa, Asia); Pleistocene-Holocene Transition; Marine Isotope Stages 2-1 Transition; Neolithic; Bronze Age; Iron Age; Plant and Animal Domestication

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S08-P-212

RADIOCARBON DATES FROM THE JAR AND COFFIN BURIALS IN THE CARDAMOM MOUNTAINS, CAMBODIA REVEAL A PREVIOUSLY UNRECORDED MORTUARY RITUAL IN THE LATE- TO POST-ANGKOR PERIOD

BEAVAN N.(1), TeP S.(2), HalcRoW S.(1), McfaDGen b.(3), HaMIlTon D.(4), bUcKleY b.(5), SHeWan l.(6), oUK S.(7), fallon S.(8), MIKSIc J.(9), o’ReIllY D.(8), DoMeTT K.(10), cHHeM K.R.(11)

(1) University of otago, DUneDIn, neW ZealanD;(2) Royal University of fine arts, PHnoM PenH, caMboDIa;(3) arch.Research, WellInGTon, neW ZealanD;(4) SUeRc Radiocarbon Dating laboratory, eaST KIlbRIDe, ScoTlanD, UnITeD KInGDoM;(5) columbia University, lamont Doherty earth observatory, PalISaDeS, UnITeD STaTeS;(6) University of Sydney, SYDneY, aUSTRalIa;(7) Ministry of culture and fine arts, PHnoM PenH, caMboDIa;(8) australian national University, canbeRRa, aUSTRalIa;(9) national University of Singapore, SInGaPoRe, SInGaPoRe;(10) James cook University, ToWnSVIlle, aUSTRalIa;(11) Ulm University, UlM, GeRManY

AbstractWe present the first radiocarbon dates from a previously unrecorded, secondary-burial mortuary ritual in the Cardamom Mountains, Cambodia. The mortuary practice incorporates imported ceramic jars and log coffins as bundling containers, which were set out on exposed rock ledges in a series of eight known sites in the eastern Cardamom massif. The suite of 25 radiocarbon ages from four of the sites (Khnorng Sroal, Phnom Pel, Damnak Samdech, and Khnom Thanan) provide the first estimation of the overall time depth of the practice. We consider the most reliable age ranges from this mortuary sample (c 1395AD to the mid-1600’s AD) and its place in and relationship to the known funerary rituals during a late- to post-Angkorian period (14th to 17th centuries AD).

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S08-P-211

DATING RITUAL MONUMENTS IN THE ALTAY MOUNTAINS: THE HYPOTHESIS OF BRONZE AGE ‘VIRTUAL DWELLINGS’

GHEYLE W.(1), De lanGHe K.(1), DVoRnIKoV e.P.(2), loUTe S.(1), MalMenDIeR a.(1), PleTS G.(1), STIcHelbaUT b.(1), Van STRYDoncK M.(3), VeRlInDen c.(1), boURGeoIS J.(1)

(1) Ghent University, GenT, belGIUM;(2) Gorno-altaysk State University, GoRno-alTaYSK, RUSSIan feDeRaTIon;(3) Royal Institute for cultural Heritage, bRUSSelS, belGIUM

AbstractAlthough many aspects of the archaeology of the Altay Mountains are well known, including the discovery of frozen Scythian tombs (Parzinger 2006), a whole series of other monuments remain unclear and mysterious. This is certainly true for a series of geometrical stone settings, that appear to be ritual monuments. A Belgian-Russian team recorded over 500 of these structures in the Yustyd Valley (Kosh-Agatch region, Russian Altay) (Gheyle, 2009) while an American-Mongolian team noticed their common presence in the Mongolian Altay (Jacobson-Tepfer, et al., 2010). Though sometimes not easily recognizable due to sedimentation and land cover, they are very typical. The most common layout takes the form of a square or rectangular stone setting with one or two entrances in East and West and a stone platform, mostly in the northern part of the enclosure. Quite often, a larger standing stone is placed at its eastern entrance. They are sometimes referred to as ‘virtual dwellings’, but their function is unknown. The monuments are generally placed in NZ-rows that often run parallel, with sites having up to 70 monuments.Dating the structures is not easy. Generally, a (late) Bronze Age date is suggested, based on the topographical proximity with kereksurs and other Bronze Age monuments. Until recently, excavations did not yield datable information. A targeted excavation of two of these monuments in the Yustyd Valley (2011) revealed the presence (as was already shown in Tuva and Mongolia) of a small central charcoal pit with some burned or cremated bone (report in preparation).Four radiocarbon dates, two on each of the charcoal pits, allowed to place the first monument in the 20th century BC and the second in the 19th-18th century BC (resp. 3595±30BP and 3565±30BP; 3510±30BP and 3475±30BP) . The dates appear to be reliable, and if they can be confirmed by other excavations of the different virtual dwelling types, it would place the phenomenon in the early Bronze Age, which is characterised by the Karakol culture in the Altay area, and the Okunev culture in Tuva. Interestingly, dwellings would then be amongst the first monuments to appear in Yustyd, even before the construction of the large kereksurs, which are generally dated to the late Bronze Age.This would completely change our interpretation of how the landscape in the Bronze Age, and later in the Iron Age, has been used by succeeding cultures.Also sampling for OSL-dating was done but this analysis is still in progress.

References1. Gheyle, W. 2009. Highlands and Steppes. an analysis of the changing archaeological landscape of the altay

Mountains from the eneolithic to the ethnographic Period. PhD dissertation, Ghent University, Ghent.2. Jacobson-Tepfer, E., Meacham, J., & Tepfer, G. 2010. archaeology and landscape in the Mongolian altai: an

atlas. Redlands, California: ESRI Press.3. Parzinger, H. 2006. Die frühen Völker eurasiens vom neolithikum bis zum Mittelalter. München: Verlag C.H.

Beck oHG.

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S08-P-213

DETERMINATION THE AGE OF HEPU ANCIENT TOMB USING 14C

RUAN X.(1), XIonG Z.(2)

(1) Guangxi University, nannInG, cHIna;(2) Guangxi Provincial Institute of culture Relica and archaeology, nannInG, cHIna

AbstractHepu is located in south of Guangxi province, It is a famous city in Han Dynasty, It is the departure harbor of maritime trading routes in ancient China. In 2003, two tombs of Han Dynasty were founded. In one tomb, there are fish bones and chicken bones. In order to determine the age, the 14C of the fish bone was measured. In another ancient tomb, the corn was founded. The age of corn was also measured with 14C. The exact ages of the bone and corn are benefit for the study of history of Han Dynasty. The result will be reported in the conference.

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S08-P-215

CHRONOLOGICAL PROBLEMS WITH NEOLITHIZATION OF POVOLZHYE

VYBORNOV A.(1), KUlKoVa M.(2), JUll T.(3), GoSlaR T.(4), SZMYT M.(4), ReSZel M.(4)

(1) Samara State academy of Social Sciences and Humanities, SaMaRa, RUSSIan feDeRaTIon;(2) Herzen State Pedagogical University, ST.PeTeRSbURG, RUSSIan feDeRaTIon;(3) University of arizona, TUcSon, UnITeD STaTeS;(4) University of Poznan, PoZnan, PolanD

AbstractThis research is supported by RHF, grant 10-01-00-393 and grant 10-01-00553a/B, RFBR, grant 10-06-00096aNeolithization is connected with the southern areas that include steppe and forest-steppe Povolzhye. The crucial issue is the chronology of the Neolithic for which conflicting data were obtained. Coaly soil from Kairshak III is dated to 6950±190BP, and soil from Tenteksor site - 5500±150BP. In 2007 the following dates were obtained on organic matter in pottery from Kairshak III -7780±90, Tenteksor - 6640±80, on coal in pottery - 6695±40 on AMS in Uppsala. At once there is a date on bones from Kairshak III - 7190±80 close to the dates on coaly soil. It was necessary to sort out this contradiction. In 2011 the date 5560±100 (Spb- 315) was obtained on charred bones from Tenteksor that coincides with the date on coaly soil. The date on bones from Kairshak III coincides with the date obtained in 2007. The date 7775±42 on organic matter in pottery from Kairshak III on AMS in Uppsala confirmed the dates from Kiev laboratory. The date 6540±100 (Spb-315a) was derived on the Tenteksor uncharred bones, and on pottery - 6650±100 (Spb-423). The latter corresponds with the dates on coal and on organic matter in pottery. The date 7700±120 (Spb-377) was received on food crusts on Kairshak III pottery that confirmed the Uppsala and Kiev laboratories dates on organic matter in pottery. The date 7100± 200 (Spb 425) on later Kairshak I was obtained in support of the date 7180±80. Thus the southern Povolzhye neolithization was from 7800 to 6600 BP. The situation with Early Neolithic Elshanskaya culture chronology is not less contradictory in the forest-steppe Povolzhye. The dates on shells from Chekalino IV site are: 8050±120BP, 7940±140BP, from Ivanovskaya site on bones - 8020±90 and on pottery-7930±90. There are series of dates on pottery from other several Elshanskaya culture sites: Iliinskaya - 6940±90. Series of dates are obtained on pottery, soil and shells for this culture of IV millennium BC: Chekalino IV-5910±90, Lebyazhinka IV-5950±70, Vyunovo Lake I-5790±130. The process of neolithization extended for two thousand years. This contradicts with archaeological idea about this phenomenon. That is why the work was continued in 2011. The date on organic matter in Elshanskaya culture pottery from Chekalino IV is -7660±200 (Spb-424), and from B. Rakovka II-7790±200 (Spb-426). They coincide with the dates on shells, bones and pottery. Thus, the dates for Elshanskya culture at the beginning of IV millennium BC don’t correspond with the necessary criteria. In addition 7250±60 (Poz 42051) is the date on coal in point bottom shred from Chekalino IV on AMS Poznan and from Vyunovo Lake I on AMS Arizona - 7222±58 (AA 96017). The dates of the beginning of V millennium are confirmed by the similar ones on food crusts from the similar pottery of Podonye. Thus, the process of neolithization of forest-steppe Povolzhye was in the first quarter VI - V millennium BC.

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S08-P-216

RADIOCARBON DATING OF CANOES IN GUANGXI, CHINA

GUAN Y.(1), RUan X.(1), XIonG Z.(2), WanG H.(1), TeRRaSI f.(3)

(1) Guangxi University, nannInG, cHIna;(2) Guangxi Provincial Institute of cultural Relics and archaeology, nannInG, cHIna;(3) Second University of naples, naPleS, ITalY

AbstractThree ancient canoes were excavated in Guangxi Zhuang Autonomous Region, China. Six wood samples are collected from different canoes for 14C dating. Radiocarbon measurements on wood samples were performed at the Peking University AMS facility (PKU-AMS) and the Centre for Isotopic Research for Cultural and Environmental Heritage (CIRCE) at Naples Second University. The samples are pretreated with acid-alkali-acid method. The result of the 14C age of canoe excavated in Hepu is 365 BP. The 14C age of other two canoes excavated in Qinzhou are 499BP and 520BP, respectively. With the calibration curve of tree ring, calibrated ages were obtained with code CALIB5.

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S08-P-217

CHRONOLOGY OF THE LATE PLEISTOCENE - EARLY HOLOCENE SITES IN NORTHEASTERN SIBERIA: AN UPDATE

KUZMIN Y.(1), DIKoVa M.(2)

(1) Institute of Geology & Mineralogy, Siberian branch of the Russian academy of Sciences, noVoSIbIRSK, RUSSIan feDeRaTIon;(2) northeastern Multidisciplinary Research Institute, far eastern branch of the Russian academy of Sciences, anaDYR, RUSSIan feDeRaTIon

AbstractToday, the Yana RHS site near the coast of the Arctic Ocean is the oldest known in Northeastern (NE) Siberia, and is dated to ca. 28,500-27,000 BP (Pitulko and Pavlova 2010). The age of the Berelekh site is now considered to be ca. 11,500 BP, and possibly earlier (Ibid.). The earliest possible age for the Dyuktai Culture of Yakutia (south of the Arctic coast) is thought to be ca. 23,000-22,000 BP.Unfortunately, pre-Holocene sites from the Kolyma River basin and Chukotka are almost unknown, besides an occupation at ca. 13,200 BP of the Siberdik site and possibly pre-8300 BP at the Uptar site. An attempt to establish the age of the Ulkhum site on Chukotka, which was originally designated as Upper Palaeolithic, gave unexpected results (charcoal collected by N.N. Dikov in 1994): 1310 ± 40 BP (AA-60205) (depth of 0.60 m), and 6850 ± 70 BP (AA-60206) (depth of 0.90 m, hearth). However, in the light of the assumption by Pitulko and Pavlova (2010) about the late survival of the Dyuktai Culture in the High Arctic, it might be the true age of the early component of the Ulkhum.Some new 14C dates were recently obtained for the final Upper Palaeolithic complexes on Kamchatka. The Ushki site cluster, Layer 7 at the Ushki 5 site was dated to 11,060-11,320 BP (Ponkratova 2007). Three sets of 14C dates were generated for Layer 7 at the Ushki 1 site: ca. 11,185-11,220 BP (Goebel et al. 2010); ca. 11,070 BP (our data); and ca. 11,800 BP (Krenke et al. 2011). The second final Palaeolithic site on Kamchatka, Anavgai 2 with a typical microblade assemblage yielded the following charcoal 14C dates: 10,870 ± 40 BP, 11,060 ± 60 BP, and 10,600 ± 50 BP (Ptashinski 2010); and 10,020 ± 75 BP (AA-83692) (upper hearth, depth of 0.38 m) and 10,030 ± 60 BP (AA-83693) (lower hearth, depth of 0.49 m).

References1. Goebel, T., S.B. Slobodin, and M.R. Waters. 2010. New dates from Ushki-1, Kamchatka, confirm 13,000-cal-

BP age for earliest Paleolithic occupation. Journal of archaeological Science 37:2640-9.2. Krenke, N.A., E.V. Leonova, I.V. Melekestsev, and M.M. Pevzner. 2011. New data on the stratigraphy of the

Ushki sites in the valley of the River Kamchatka. Rossiiskaya arkheologiya 3:14-24.3. Pitilko, V.V., and E.Y. Pavlova. 2010. Geoarchaeology and Radiocarbon chronology of the Stone age of the

north-east asia. St.-Petersburg, Nauka Publishers.4. Ponkratova, I.Y. 2007. The Ushki 5 site: studies in the last years, problems, and perspectives. In Kolymsky

Gumanitarny almanakh. Vypusk 2, edited by A.I. Shirokov, pp. 13-20. Magadan: Kordis Press.5. Ptashinski, A.V. 2010. Finds of late Ushki Upper Palaeolithic culture in the Bystrinsky County of Kamchatka

Province. In Mezhdunarodny Sympozium «Pervonachalnoe osvoenie chelovekom Kontinentalnoi i ostrovnoi chasti Severo-Vostochnoi azii», edited by A.P. Derevianko and A.A. Vasilevsky, pp. 109-117. Yuzhno-Sakhalinsk: Sakhalin State University.

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S08-P-218

RADIOCARBON DATING OF THE TRANSITION INTO THE BRONZE AGE IN SOUTHEAST ASIA

HIGHAM C.(1), HIGHaM T.(2)

(1) Department of anthropology, University of otago, DUneDIn, neW ZealanD;(2) oxford Radiocarbon accelerator Unit, oXfoRD, UnITeD KInGDoM

AbstractEstablishing the chronological framework for the transition into the Bronze Age in Southeast Asia has aroused controversy and uncertainty since claims for the earliest copper-base metallurgy in the world were published in the 1960s and 70s. The two prehistoric sites in question, Non Nok Tha and Ban Chiang, comprised cemeteries that spanned the Neolithic-Bronze Age transition. Radiocarbon determinations were derived from unspeciated charcoal, and many samples were accumulated from uncertain cultural contexts. The problem of inbuilt age and disturbed contexts provided internally contradictory results.In order to clarify the chronology of Ban Chiang, where the excavators suggested that early bronzes dated to about 3600 BC, White (1997) turned to the organic temper in the clay of mortuary vessels. Three pretreatments were employed, and seven determinations derived from crushed potsherds are the basis for a revised chronology, which saw the early Bronze Age beginning in about 2000 BC. We note that clay can contain carbon, and that this dating method can be unreliable.In the meantime, we have dated the same transition at the site of Ban Non Wat, about 280 km south of Ban Chiang, on the basis of 76 determinations, the majority derived from freshwater shells placed with the dead as mortuary offerings. We used Bayesian modelling to derive posterior density estimates for the sequence, concluding that the first Bronze Age phase dates in the late 11th century BC (Higham and Higham, 2009).The millennium separating the same event in these two sites is archaeologically challenging. If the Ban Chiang chronology is correct, then deriving the knowledge of copper smelting and casting from Chinese states is ruled out, and White and Hamilton (2009) have suggested in a controversial model that the Ban Chiang metallurgical tradition was introduced by a 2500 km passage to Thailand from Siberia. The later chronology is compatible with the transmission of copper technology from established Chinese sources.In order to resolve this dilemma, we have obtained AMS radiocarbon determinations from the bones of the Neolithic and early Bronze Age inhabitants of Ban Chiang together with associated pig bones. Again employing Bayesian modelling and ultrafiltration pretreatment, we have established a new chronological framework for Ban Chiang showing reliably for the first time, the date of the transition into the Bronze Age.

ReferencesHIGHAM C.F.W. & T.F.G. HIGHAM 2009. A new chronological framework for prehistoric Southeast Asia, based on a Bayesian model from Ban Non Wat. antiquity 82: 125-44.WHITE, J.C. 1997. A brief note on new dates for the Ban Chiang cultural tradition. bulletin of the Indo-Pacific Prehistory association 16: 103-6.WHITE J.C. & E. Hamilton 2009. The transmission of early Bronze Age technology to Thailand: new perspectives. Journal of World Prehistory 22: 357-97.

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S08-P-219

DATING THE END OF INDUSTRY: USING IN-SLAG CHARCOALS AS AN INDICATOR OF TERMINAL IRON PRODUCTION WITHIN THE MEDIEVAL CITY OF PREAH KHAN OF KOMPONG SVAY, CAMBODIA

HENDRICKSON M.(1), HUa Q.(2)

(1) Department of anthropology, University of Illinois at chicago, cHIcaGo, UnITeD STaTeS;(2) australian nuclear Science and Technology organisation (anSTo), KIRRaWee Dc, aUSTRalIa

AbstractIron was a key material in the expansion of the medieval Khmer Empire, which spread across mainland Southeast Asia from the capital of Angkor (9th to 15th centuries A.D.). The Industries of Angkor Project (INDAP) represents the first rigorous investigation of the procurement, production and distribution of iron. Currently, Preah Khan of Kompong Svay (Preah Khan) is the only Angkorian period city with evidence of iron smelting inside its enclosure walls with over thirty iron slag concentrations recorded by INDAP. The assumption has been that Preah Khan was producing iron to meet the peak building and political requirements of the Khmer elite at Angkor between the 11th and 13th centuries. The sheer number and size of these sites, however, precludes the use of excavation to document the entire history of iron production within Preah Khan. This paper explores the use of AMS dating in-slag charcoals from surface collections to assess ‘terminal’ iron production at individual sites and across the entire city. A total of twenty in-slag charcoals from fourteen sites were dated using the STAR AMS Facility at ANSTO with a typical precision of ≤0.4% (1σ). Comparable results obtained from seven excavated and two in-slag charcoals at the Boeng Kroam Location 1 site indicate that this method is a reliable indicator for identifying the end of industrial activities. Contrary to the initial hypothesis only two sites appear to have stopped producing within peak of the Angkorian period while the remaining slag concentrations were last used in the Post-Angkorian era (15th to 18th centuries A.D.). While these results downplay the role of Preah Khan in the expansion of empire, they are extremely valuable by providing the first evidence of Post-Angkorian sites dated via AMS and, more significantly, point to the continued activity of Khmer cities after the purported collapse of Angkor and its Empire in the early 15th century. Overall, the use of in-slag charcoals is viewed as an effective and cost-efficient approach for identifying the spatial distribution of final smelting events and also highlighting target sites for extensive subsurface testing.This work was supported by Ainse grant 11/003 and ARC Discovery grant DP0987878.

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S08-P-220

BUILDING A RELIABLE CHRONOLOGY FOR THE ANCIENT TOWN OF UFA-II: IS THIS THE ELUSIVE «BASHKORT» OF MEDIAEVAL SOURCES?

SUNGATOV F.(1), leVcHenKo V.(2)

(1) academy of Sciences of Republic of bashkortostan, Ufa, RePUblIc of baSHKoRToSTan, RUSSIan feDeRaTIon;(2) anSTo, lUcaS HeIGHTS, nSW, aUSTRalIa

AbstractBuilding a reliable timeline for the mound of the ancient fortified settlement of Ufa-II is the foremost task for archaeology of the Southern Ural region. Without it the relation of the settlement to other archaeological sites of the Southern Ural cannot be established. Also, attributing the ancient town of «Bashkort», mentioned in a few mediaeval sources as situated in the area well before the arrival of the first Russian settlers in mid 16th century AD, to the studied archaeological site cannot be done without establishing a good timeline. Regrettably, archaeological chronology built on scarce and not definitive artefacts is not accurate enough. The site is situated in the historical centre of Ufa - the capital of Bashkortostan Republic, Russia - on the right bank of Belaya River next to the confluence of Karaidel and Dema tributaries. It was preserved relatively undisturbed. The archaeological dig commenced in 2006.Radiocarbon dating, based on charcoal and wood samples from the deposit sequence, was chosen to construct the chronology. 16 samples were collected starting from the underlying sterile ground and 2.5 m up through layers ending ~ 0.5 m below the present surface. When collecting, attention was paid to pick up pieces originating from small twigs and branches to minimise inherited age. Three charcoal samples were dedicated to determining the period of existence of a plank boardwalk, whose remnants were uncovered in the dig, by bracketing its layer as close as possible from top and bottom. Upon collection, samples were packed in clean bags and mailed to ANSTO. Charcoal went through the standard ABA pretreatment, and exhibited relatively low presence of humic acids. Wood was treated to extract holocellulose. Pretreated samples were combusted in evacuated sealed quartz tubes in the presence of purified CuO and Ag. CO2 was converted to graphite by reduction in excess hydrogen over iron catalyst to produce targets for AMS measurements. 14C determinations were done on the AMS installation STAR to a precision of ~0.35%, which resulted in overall 14C age errors of 30 to 40 years. Age calibration was done by the OxCal 4.1 program. The calendar dates span from late 2nd - early 3rd to 7th century AD and agree with that expected from archaeology, with only one outlier of about 100 years older, which can be easily explained by the presence of «old wood» - probably due to unfortunate selection of a charcoal piece from the inner sections of a log. With the outlier excluded, the date sequence was used to create by Bayesian methods the age-depth model for the dig, thus providing the site with robust chronology. Samples bracketing the plank boardwalk narrow down the period of its existence to ~75 years at the turn of 6th to 7th century AD.More 14C tests are planned for the new season dig, for some wooden and bone artefacts uncovered, and also to resolve the remaining 0.5 m of soil on top of the deposit layers.

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S08-P-221

RECONSTRUCTION OF THE DIET SYSTEM OF THE RUSSIAN TOWN ANCIENT POPULATION BEFORE THE MONGOL INVASION: THE ISOTOPE ANALYSIS OF BONE SAMPLES

ENGOVATOVA A.

Russian academy of Sciences, MoScoW, RUSSIan feDeRaTIon

AbstractThe use of isotopic analysis allowed reconstructing the diet of thepopulation of the medieval town of Yaroslavl on the example. We identified the values of δ13C and δ15N, which are usually used for determining the share of plant and animal food in averaged nutrition histories of people. The chronology was based on both the radiocarbon dates and historical evidences.A total of 120 analyses of human and animal bones from 5 collective burials have been analyzed. The selection includes the samples of human bones (men’s, women’s and children’s) and samples of bones of various domestic animals (cows, horses, pigs and dogs) from 5 burials.The sanitary burials are a unique historical source which allows analyzing the local diet system on the eve of the Mongol invasion.In Yaroslavl, the large scale excavations in the medieval Kremlin gave unique archaeological data about the early history of the town. They also opened the layers which show the attack by the army of Batu Khan which had stormed the town in 1238, burning it down and killing the inhabitants. Radiocarbon analysis has now confirmed the historical dates.The excavations revealed nine collective sanitary burials containing human remains (about 500 individuals). The burials were in cellars and household pits. Many of the skeletons show chopped and stab wounds. All the sanitary burials also contained skeletons of domestic animals (cows, horses, pigs, dogs, etc); the animals died during the fighting or soon afterwards.The entire selection from five places of compact burial showed a stable carbon delta of circa -20,03±0,1‰, which points to a mixed diet including temperate-zone plants, a small proportion of grains, and also meat of local herbivorous land animals.The data on δ15N accumulation shows the presence of proteins in the diet, with the main source being the meat of land or aquatic animals of different trophic levels (van der Merwe, 1989). δ15N is 11,81±0,72‰, showing that meat of land mammals was the basic source of protein. The few individuals with δ15N higher that 13‰ must have regularly consumed freshwater fish.Comparison of the average isotope values for different locations shows a similarity of diet for the whole population group.The analyses showed there was no difference in the diet of men and women. This means that the diet traditions of the Old Russ town were not gender-specific.δ15N for bone tissue of breastfed children (until two years on average) shows isotopic fractionation for individuals with a mainly protein diet. The figure for children aged 2-3 years old and younger is about 12,7‰, which is a little higher than for the adult population. Yet the differences are on the same trophic level. We can assume that the medieval people of Yaroslavl consumed a relatively large amount of meat. There was no protein deficit, unlike the situation in some of the rural regions in the Russian North.

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S08-P-222

AT THE EVE OF URBANIZATION - BAYESIAN MODEL DATING FOR MEDIEVAL TURKU

OINONEN M.(1)(2), HIlaSVUoRI e.(3), MeHTonen H.(1), UoTIla K.(4)(2), ZeTTeRbeRG P.(5)

(1) finnish Museum of natural History, UnIVeRSITY of HelSInKI, fInlanD;(2) Docent, UnIVeRSITY of TURKU, fInlanD;(3) finnish environmental Institute, HelSInKI, fInlanD;(4) Muuritutkimus ky, KaaRIna, fInlanD;(5) laboratory of Dendrochronology, UnIVeRSITY of eaSTeRn fInlanD, fInlanD

AbstractRadiocarbon concentration in atmosphere has been varying over time. This variation is stored by the wood in tree rings and incorporated into the radiocarbon calibration curves (e.g. Reimer et al 2009). The variation results in a certain loss of precision when transforming the radiocarbon ages to calendar years. For example, individual radiocarbon dates becomes practically useless for the 14th century contexts - the calendar year distributions spread out to be even 100 years wide.The eve of urbanization in Finland has been traditionally placed within this challenging era. Therefore, the scientific dating of early phases of medieval contexts - towns, castles and churches - in Finnish territory has been mainly relying on dendrochronology. However, prerequisite for using dendrochronology is existing master ring width chronologies and sufficient preservation of finds. Lively-discussed radiocarbon dating of mortar suffers also from the 14th century wiggles. On the other hand, if archaeology can provide information on successive chronological layers (wood samples, stratigraphical layers), one may use these as a priori information to exclude impossible calendar years through Bayesian principle (Buck et al 1996, Bronk-Ramsey 2009).Archaeological excavations performed during 2009-2010 at the Aboa Vetus museum in Turku yielded large amount of a priori information and datable material. The excavation recorded multitude of archaeological layers on top of an empty clay layer and thus illustrated the start of the urbanization at the Aurajoki river bank. We have performed individual 14C dates of short-lived material (nutshells, skin, animal bones) for the five lowest layers and utilized the stratigraphical information within the Bayesian approach to obtain the chronology of the early phases of the site. Based on the work, the individual century-wide calendar-year distributions get 5-10 times narrower and thus demonstrate the power of model datings for the 14th-century contexts.

References1. Bronk Ramsey C 2009a. Bayesian analysis of radiocarbon dates. Radiocarbon 51: pp. 337-360.2. Buck C E, Cavanagh W G, Litton C 1996. bayesian approach to Interpreting archaeological Data. Wiley &

Sons Ltd. ISBN 978-0-471-96197-0.

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S08-P-223

ON CORRESPONDENCE BETWEEN RADIOCARBON DATES ON POTTERY AND OTHER MATERIALS OF THE NEOLITHIC IN RUSSIA

VYBORNOV A.(1), KoValIUKH n.(2), SKRIPKIn V.(2), ZaITSeVa G.(3), KUlKoVa M.(4), PoSSneRT G.(5), VYboRnoVa M.(1)

(1) Samara State academy of Social Sciences and Humanities, SaMaRa, RUSSIan feDeRaTIon;(2) The Institute of the Geochemistry of environment, national academy of Sciences of Ukraine, KIeV, UKRaIne;(3) Institute for History of Material culture, ST.PeTeRSbURG, RUSSIan feDeRaTIon;(4) Herzen State Pedagogical University, ST.PeTeRSbURG, RUSSIan feDeRaTIon;(5) University of Uppsala, UPPSala, SWeDen

AbstractThe research is supported by the RHF, grant 10-01-00393 and grant10-01-00553a/B, RFBR, grant 10-06-00096a and A. PapshevaUsing a special procedure dating the samples of the Neolithic and Eneolithic pottery from the Urals to Upper Povolzhye started in 2007. More than 300 dates have been obtained by now. Since the start of work some archeologists have suggested the imperfection of this procedure. Such opinions were justified. First, now and then the obtained dates differed from the usual idea about the chronology of both separate sites and cultures integrally. For example, the Neolithic on soil of the Caspian Sea area was dated to 6950-5500BP and on pottery – 7800-6660BP. The Middle Volga Neolithic is dated to 8000-7800BP on shells, and on pottery – 6000-5800BP. Second, it wasn’t clear what organic matter the pottery contains and if it corresponds with the date of its making. Lack of organic matter for dating at sites in some regions favoured the extension of the work and procedure development. There are reasons to claim that there are organic compounds in pottery forming paste that have no geological origin. Earlier dates were confirmed on the materials from the Caspian Sea area on AMS, on food crusts and on coal. Thus the dates on food crusts from Kairshak III are - 7700±120BP (Spb377), on pottery on AMS-7775±42(Ua 41359), on coal from Tektensor 6695±40 (Ua35227), on bones 6540±100 (Spb 315a) and on pottery 6640±80. Dates for Koshkinskaya culture of the Urals are -7050 (Ле 7883) on coal, on pottery-7010, on coal 6380±120 (Ле 4344), on pottery 6470±90; for Jangar culture in Kalmykia-6870±130 on coal, on pottery-6780±90; on coal for Hvalinskaya in Lower Povolzhye 6000±150, on pottery-6070±90; on bones 5920(ОхА 4313), on pottery -5980; for Mullino in Pre-Urals-6260 (Ле1514), on pottery-6290; Koshkinskaya site on the Vyatka on coal-6160 (Ле 5549), on pottery-6110; Kotchurovskaya on coal-5410 (Ле 1345), on pottery-5330±80; for Elshanskaya culture of Middle Povolzhye on shells-7940±140 (Ле 4784), on bones 8020±90 (Ле 2343), on pottery 7930±90Кi; 7790±200 (Spb 426), for Upper-Volga culture on food crusts 6760, 6650, on pottery 6740,6690, for pit-comb culture on coal 5980, on pottery-5960, the date obtained in Kiev laboratory on pottery for Varfolomeevka layer 2Б on the Lower Volga is 7070±90, in Uppsala laboratory 7034±41, for layer 2А 6860 and 6540, 6693±39 and 6544±38 respectively, for Middle Don culture 6340±80 on coal and 6190±100 on pottery. Thus on further development of the procedure one can state its definite efficiency.

References1. Zaitseva G., Skakovsky E., Possnert G., Vybornov A., Kovaliukh N., Skripkin V. Organic matter in pottery:

nature, organic components and reliability of radiocarbon dates // Proceedings of III All-Russian archaeological conference. 2011

2. ZaitsevaG., SkripkinV., Kovaliukh N., Possnert G., Dolukhanov P.,Vybornov A. Radiocarbon dating of Neolithic pottery Radiocarbon. 2009

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S08-P-224

THE CONSTRUCTION OF qASR EL-BINT, PETRA, JORDAN: NEW AMS RADIOCARBON DATES

AL-BASHAIREH K.

Yarmouk University, IRbID, JoRDan

AbstractThis research aims at AMS radiocarbon dating samples of wood wedges and sticks embedded between the stone rows of the walls of the Temple of Qasr el-Bint, Petra, south Jordan. The authors surveyed the structure and noticed the wood pieces, mostly wedges, in July, 2010. The Temple of Qasr el-Bint is one of the most famous structures of the ancient city of Petra, south Jordan. It is the only free-standing structure at the city that survived from the earthquakes’ destruction. The results showed that the youngest date after which the temple probably was constructed is 1915±40BP (AD29-130). The date concords with the archaeological data that the construction of the temple took place during the rule of Malichus II (AD 40/44-70) and with Al-Bashaireh and Hodgins (2011).

ReferencesAl-Bashaireh, Kh. - Hodgins, G. W. L., AMS 14C Dating of Organic Inclusions of Plaster and Mortar from Different Structures at Petra - Jordan, Journal of Archaeological Science 30, 2010, 1-7.

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S08-P-225

STONES, BONES AND HILLFORT - RADIOCARBON DATING OF KIVUTKALNS BRONZE-WORKING CENTRE

OINONEN M.(1), laVenTo M.(2), VaSKS a.(3)

(1) finnish Museum of natural History, UnIVeRSITY of HelSInKI, fInlanD;(2) Department of Philosophy, History, culture and art Studies, UnIVeRSITY of HelSInKI, fInlanD;(3) Institute of latvian History, UnIVeRSITY of laTVIa, laTVIa

AbstractNeolithic traditions of amber and flint working in Latvian territory started to change gradually after introduction of bronze within the Lake Lubãns Depression in eastern Latvia. Early Bronze Age settlements Abora I and Laga’a around the Lake Lubãns still show importance of flint and amber as exchange items. At Brikuli hillfort - also at Lake Lubãns - amber artefacts are already completely missing and bronze metallurgy have gained importance. Eventually, one third of the archaeological artefacts found at Kivutkalns hill-fort in the lower Daugava river are related to bronze working (Vasks 2010). According to excavations the hill-fort was built on top of a cemetery, from which burials of more than 230 individuals have been found. This settlement has been considered as the largest Late Bronze Age bronze-working centre in Latvia. In this contribution, we discuss the 14 C chronologies of the hill-fort and the cemetery based on the new AMS radiocarbon datings of the animal and human bones (8 pcs) and existing conventional 14 C datings on charcoal (7 pcs). Particularly, we take a glance on the possible contemporary use of two contexts and implement archaeological a priori information into such an analysis by Bayesian approach. According to the individual bone dates, the hill-fort and the cemetery have been used around the era of the radiocarbon plateau during the 1st millennium BC. The posterior calendar year probability distributions narrow significantly if ordering of contexts is taken into account. The carbon and nitrogen stable isotope ratios indicate the mixed use of terrestrial and marine dietary resources. Therefore, we also discuss the possible reservoir effect on the human bone dates on the basis of isotopic ratios. Use of partly marine diet and the enhanced use of bronze emphasize the importance of river Daugava as one of the most important routes towards the far-away source areas of resources.

ReferencesVasks A 2010. Latvia as part of a sphere of contacts in the Bronze Age. Archaeologia Baltica 13: pp. 153-160.

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S08-P-226

THE qUESTION OF THE TRUE INTERPRETATION OF THE RADIOCARBON DATES ON THE EXAMPLE OF THE SERIES OF DATES FROM THE BRONZE AGE SETTLEMENT ON THE RIVER OKA

SAPRYKINA I.

Institute of archaeology RaS, MoScoW, RUSSIan feDeRaTIon

AbstractReport presents results of investigation of the series of 29 radiocarbon dates obtained from the soil and pottery samples and its true interpretation on the example of the multilayer settlement Dmitrovskaya Sloboda 2 (bank of river Oka) that is dated according to the archaeological findings to the third quarter of the 2 mill. BC.The settlement occupied first above flood-plain terrace and is characterized by the wash conditions. The investigations of soils morphology (Alexander et al., 2008) have shown that the cultural layer of the settlement is marked by the high degree of the soil substances migration and organizatwion of the pseudofiber 1 m below of day. Phosphates analyses has also shown significant degree of the phosphorus washed from the layer; on the other hand such parts of the layer as pits have shown quite a large quantity of the phosphorus and carbonate (CaCO3). The greatest part of the pottery and soil intended for 14C analyses have been gathered from such pits. It is well known that carbonates influenced both the geochemical atmosphere of the cultural layers and the safety and characteristics of the archaeological findings (first of all pottery) that for a long time had been under the conditions described above (Drebuschak et al., 2006). Beside that safety and characteristics of the pottery are also depended on the other factors that should be considered while using it as a material to date and to read of the gathered evidences (Saprykina, Zelentsova, Voronin, 2010. P. 143, 144).The samples of organic stuff (charcoal, humus) and pottery were dated in the Radiocarbon Laboratory (Kiev, Ukraine) and IGAN (Moscow, Russia). The pottery gave 10 radiocarbon dates that is turned to be more ancient than 19 dates obtained from the cultural layer; at the same time the date’s variation are equal to 1500 years. The layer dates obtained in Kiev in its turn are younger than the dates that were derived from the pottery in the same Laboratory. On the other hand the charcoal dates from IGAN could be compared to the pottery dates originated from the Radiocarbon Laboratory in Kiev

ReferencesAlexander et al. (2008) report (in Russian)Debruschak et al (2006) report (in Russian)Saprykina I., Zelentsova O., Voronin K., 2010. What is it that we date when dating pottery? View of archaeologist // 38th International Symposium on Archaeometry. May 10-14, 2010. Program and Abstracts. University of South Florida. Tampa, Florida, USA.

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S08-P-227

INTEGRATING SERIATION INTO RADIOCARBON-BASED MODELS OF EARLY EGYPT

DEE M.(1), lee S.(1), WenGRoW D.(2), SHoRTlanD a.(3), STeVenSon a.(1), bRocK f.(1), HooD a.(1), bRonK RaMSeY c.(1)

(1) University of oxford, oXfoRD, UnITeD KInGDoM;(2) University college, lonDon, UnITeD KInGDoM;(3) cranfield University, SHRIVenHaM, UnITeD KInGDoM

AbstractSeriation is a relative dating technique that is used widely in archaeology, particularly where there is a lack of vertical stratigraphy. It involves the ordering of artefacts in a manner that reflects incremental stylistic or compositional changes and hence the passage of time. One of its first and most famous applications was by Flinders Petrie in the late 19th Century AD. His seriation of Egyptian Predynastic and Early Dynastic ceramics was so successful that a modified version of it is still in use today. However, several shortcomings remain with this form of chronological analysis. These include difficulties in assigning relative dates in the absence of diagnostic pottery, problems in estimating the absolute duration of cultural phases, and the issue of potential time lapses between equivalent contexts at different sites. On the Leverhulme Formation of the Egyptian State Project, we have begun an analysis of Egyptian seriation with two main aims in mind. Firstly, radiocarbon dates are being made on organic materials directly associated with artefacts that have been assigned specific relative dates by seriation. In this way, the general reliability of the relative dating method is being evaluated. Secondly, the tendency of both relative dating techniques and unmodelled radiocarbon dates to appear to elongate phases is also being examined. Indeed, it has become apparent that, even where ceramic series do indeed reflect temporal change, the overlap between successive classes is considerable. As a result, the newly developed ‘trapezoidal’ phase in OxCal is being employed to model the associated cultural phases. Early indications suggest that this approach should yield the most realistic and informative estimates for the various cultural transitions of the Predynastic period.

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S08-P-228

THE RAMESES III GIRDLE AND THE ORIGIN OF COMPOUND WEAVING

GOOD I.(1), Dee M.(1), cooKe a.(2), bRonK RaMSeY c.(1), PollaRD M.(1)

(1) University of oxford, oXfoRD, UnITeD KInGDoM;(2) World Museum, lIVeRPool, UnITeD KInGDoM

AbstractCompound weave structures are an advanced form of weaving which require a complex piece of weaving apparatus known as a drawloom. They have either complimentary or supplementary warps and/or wefts. In the history of textiles, there are competing theories on the origins of the method. The prevailing belief is that it developed exclusively in China (ca. 400 BCE), first as warp-faced compound tabby and then as compound twills. Weft-faced compound weaves, made of wool were then adopted in western Asia several centuries later. A second theory reasons that compound weaves developed independently in both China and the ancient Near East. In 1982, Collingwood argued that an Egyptian textile known as the Rameses III Girdle was constructed using a compound weave. However, to date no one has picked up on the significance of this assertion. If the Girdle does date to the time of Rameses III (1184-1153 BCE) then it is by far the earliest example of the method anywhere in the world. We obtained small sections of thread from the tassels of the Girdle, which is housed at Liverpool’s World Museum. Here we present the results of our own examination of the structure of the cloth, and an AMS date of the sample. The findings from this unique study provide significant insights into the development and transmission of early weaving technologies.

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S08-P-229

CAN RADIOCARBON DATING MATCH DENDROCHRONOLOGY?

TYERS C.(1), MaRSHall P.(2), cooK G.(3), bRonK RaMSeY c.(4), baYlISS a.(2)

(1) University of Sheffield, SHeffIelD, UnITeD KInGDoM;(2) english Heritage, lonDon, UnITeD KInGDoM;(3) Scottish Universities environmental Research centre, GlaSGoW, UnITeD KInGDoM;(4) oxford Radiocarbon accelerator Unit, oXfoRD, UnITeD KInGDoM

AbstractIn England, scientific dating forms an integral part of the process of assessing the significance of historic buildings, either for their protection or their informed conservation. Many buildings are sampled for dendrochronology, but in a significant number of cases tree-ring dating is unsucessful. The ability to provide chronologies from wiggle-matching that enjoy a similar level of accuracy to those derived from dendrochronology is therefore desirable.Recent work, however, has shown that in some periods further structure may be present in the radiocarbon calibration curve than is revealed by the existing data (McCormac et al. 2001; 2008). For some periods, and for high-precision applications, these differences may make a substantive difference to archaeological interpretation, particularly when absolute accuracy is required on the calendar scale to integrate radiocarbon-based chronologies with the historical or dendrochronological timescale (Kromer et al. 2001; 2010).To test whether the resolution of the current radiocarbon calibration curve, beyond the limit of the single-year data (Stuiver 1993), is a practical limitation in the accuracy that can be provided by wiggle-matching in the period AD 1140 - AD 1540, a series of wiggle-match studies have been undertaken on known-age tree-ring sequences.

References1. Kromer, B, Manning, S W, Kuniholm, P I, Newton, M W, Spurk, M, and Levin, I, 2001 Regional 14CO2 offsets

in the troposphere: magnitude, mechanisms, and consequences, Science, 294, 2529-322. Kromer, B, Manning, S, Friedrich, M, Talamo, S, and Trano, N, 2010 14C calibration in the 2nd and 1st millennia

BC-Eastern Mediterranean Radiocarbon Comparison Project (EMRCP), Radiocarbon, 52, 875-863. McCormac, F G, Bayliss, A, Baillie, M G L, and Brown, D M, 2004 Radiocarbon calibration in the Anglo-Saxon

period: AD 495 - 725, Radiocarbon, 46, 1123-54. McCormac, F G, Bayliss, A, Brown, D M, Reimer, P J, and Thompson, M M, 2008 Extended radiocarbon

calibration in the Anglo-Saxon Period, AD 395-485 and AD 735-805, Radiocarbon, 50, 11-175. Stuiver, M, 1993 A note on single-year calibration of the radiocarbon time scale, AD 1510 - 1954, Radiocarbon,

35, 67-72

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S08-P-230

RADIOCARBON DATING OF LIME LUMPS FROM THE BAPTISMAL FONT OF THE S. LORENZO CATHEDRAL OF ALBA (CUNEO, ITALY)

MICHELETTO E.(1), PeSce G.l.a.(2), QUaRTa G.(3), UGGÈ S.(1), DecRI a.(4), calcaGnIle l.(3)

(1) Soprintendenza for the archaeological Heritage of Piedmont, TURIn, ITalY;(2) University of bath, baTH, UnITeD KInGDoM;(3) ceDaD (centre for Dating and Diagnostic), Department of Innovation engineering, University of Salento, lecce,

ITalY;(4) Ipsilon s.c.r.l., Genoa, ITalY

AbstractSaint Lorenzo cathedral of Alba is a Romanesque church located in Alba (Cuneo, Piedmont), North West of Italy. The church, built on the site of a previous structure probably founded in the late antiquity, has a Latin cross with three naves and a late Gothic architectural style. Since 2007 it has been subject to renovation works and archaeological excavations.During the excavations, remains of a baptismal font have been found in the aisle, in front of the Blessed Sacrament chapel. In particular, thanks to the archaeological researches have been unearthing the lower part of the basin and the drainage pipe of water.The whole structure has been built in stones, bricks and lime mortar, laid on a surface of about three square meters. A hydraulic plaster made of air lime and brick powder (cocciopesto) still covers the inner surface of the basin whereas the drainage structure has been made of clay pipes laid on lime mortar beds.Thermoluminescence dating has been carried out on some of the ceramic elements used in both, the pipe and the basin. Results suggest that some of these elements may have been reused from previous structures.In order to verify these dating seven lumps of pure lime have been taken from the lime mortar used in different parts of the structure and have been treated to date them with the radiocarbon method using the «pure lime lumps» technique (Pesce et al. 2009).Results are in agreement with some of the results obtained with the thermoluminescence method and also show a good mutual consistency. This paper will address the problem of the radiocarbon dating of pure lime lumps collected in the baptismal font and will discuss the obtained results in comparison woth the results obtained with the thermoluminescence and with the archaeological record.

ReferencesPesce, GLA, Quarta, G, Calcagnile, L, D’Elia, M, Cavaciocchi, P, Lastrico, C, Guastella, R., 2009. Radiocarbon dating of lumps from aerial lime mortars and plasters: methodological issues and results from the S. Nicolò of Capodimonte Church (Camogli, Genoa - Italy).Radiocarbon. 51(2), pp.867-872.

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S08-P-231

DATING AND ANALYZING FOOD HABITS IN THE EARLY NEOLITHIC PERIOD IN NORTHEAST ASIA

KUNIKITA D.(1), SHeVKoMUD I.(2), YoSHIDa K.(3), onUKI S.(1), YaMaHaRa T.(4), MaTSUZaKI H.(5)

(1) faculty of letters, The University of Tokyo, ToKYo, JaPan;(2) Khabarovsk Scientific center of feb RaS, KHabaRoVSK, RUSSIan feDeRaTIon;(3) University Museum, The University of Tokyo, ToKYo, JaPan;(4) obihiro centennial city Museum, HoKKaIDo, JaPan;(5) School of engineering, The University of Tokyo, ToKYo, JaPan

AbstractThe objective of this research is to clarify the dates and reconstruct food habits of the early Neolithic period in the Russian Amur River basin and the Japanese island of Hokkaido. It is known that the Northeast Asian region was the site of the world’s earliest emergence of pottery (about 15,000 caIBP, as at the Oudai Yamamoto Site No. 1 in Aomori Prefecture). The precipitating factors for the emergence of pottery are believed to be related to ecological changes accompanied by climatic changes from the end of the Pleistocene period to the early Holocene period. Many proposals have been offered about the functions and uses of pottery in the early Neolithic period in Northeast Asia on the basis of pottery shapes (capacity and type) and stone artifact composition, changes in the natural environment, the beginning of river fishing, and the use of nuts. The emergence of pottery was a groundbreaking event in prehistoric East Asia, and elucidating the process will be extremely significant for understanding the subsequent years of the Neolithic period.In this study, we attempted to reconstruct food habits through radiocarbondating, carbon-to-nitrogen isotope analysis, and C/N analysis of matter adhering to the insides of pottery from Amur River sites in Russia (Novotroitskoye Site No. 10, Gontyaruka Site N° 1, Kondon Site No 1) and a site in Hokkaido, Japan (Taisho Site No. 3). We obtained dates of about 12,500 to 10,000 BP for these sites. At present, there are no major differences in the carbon-nitrogen isotope ratios and the C/N ratios at these sites, and the nitrogen isotope ratio tends to be somewhat higher than that in domains with C3 vegetation and herbivorous animals. There are also data that show a tendency of having a somewhat higher carbon isotope ratio, suggesting that the people made use of anadromous fish such as salmon and trout. Thus, there is a high probability that the contents of the pottery that were boiled at these sites were river fish, which included anadromous salmon or trout. However, data from these sites differ slightly from the results obtained from the authors’ previous research into the other Neolithic periods. Moreover, it is believed that in the initial stages of the emergence of pottery, the food boiled in the pots was the same as the findings mentioned above. In this report, we also add certain comparative considerations of the value of previously reported materials from the same period in Japan.

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S08-P-232

DATING ANOMALIES IN THE ARCHAEOLOGY OF THE 7TH CENTURY BC

PORTER R.(1), Dee M.(2), fRIGG S.(3)

(1) Retired, cRoYDon, UnITeD KInGDoM;(2) University of oxford, oXfoRD, UnITeD KInGDoM;(3) Stiftsbibliothek, ST Gallen, SWITZeRlanD

AbstractTaylor et al. (2010) published an anomalous set of carbon dates on human bones from the destruction of Nineveh, the ancient capital of Assyria which was destroyed in 612 BC (a rock-solid historical date). Despite the fact that they took every precaution, their results for the destruction were consistently about 180 years too early. Manning and Kromer (2011) published a final set of radiocarbon dates for a destruction level at Gordion in central Turkey. In this case, the result was about 130 years earlier than the early 7th century BC date previously accepted on archaeological and historical reasoning (however, that reasoning was never totally secure). In order to further investigate these 7th century anomalies, we made a single AMS radiocarbon measurement on a piece of ancient Egyptian mummy wrapping, from a sarcophagus that is securely dated stylistically to the first half of the 7th century BC.

References1. Taylor R. E., Beaumont W. C., Southon J., Stronach D. and Pickworth D. (2010). Alternative Explanations for

Anomalous 14C Ages on Human Skeletons Associated with the 612 BCE Destruction of Nineveh. Radiocarbon 52(2): 372-382.

2. Manning S. W. and Kromer B. (2011). Radiocarbon Dating Iron Age Gordion and the Early Phrygian Destruction in Particular. In C.B. Rose and G. Darbyshire (eds.), The new chronology of Iron age Gordion, 123-153. Philadelphia: University of Pennsylvania Museum of Archaeology and Anthropology.

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S08-P-233

ARCHAEOLOGICAL EXCAVATION OF JARE AREA KHOZESTAN, AND OSL DATING REPORT OF SAMPLES FROM JARE DAM SOUTWEST,IRAN

SHARIFI M.

Iranian center for archaeology research, TeHRan, IRan

AbstractThis region has been the bed of formation of important human settlement from pre-history to the present. Although the region of ramhoemoz,jare, has witnessed/experienced several cultural-political events as well as developments during history, we face insufficiency of cultural materials, documents and information for studying and learning more about this region during historical time. Therefore, the materials and data obtained from the site excavation of jare in ramhormoz province would clarify some cultural-material ambiguities and explain the state of cultural interactions of the region.Jare region, in ramhormoz plain, is located 33 km north of ramhormoz in a mountainous region with the geographical coordinates of E: 39R0377264, N:3480342.In this site, after mapping and gridding operations over two seasons of surveying and excavation 7 trenches were dug in different dimensions;we will explain the architectural data, potteries and historical influences of the mentioned trenches in three square sections. The «locus» system has been used to excavate and numbering the layers. The vertical documentation of artifacts and layers has been conducted utilizing Matrix Haris method, and the horizontal documentation has been done with planning and recording the remnants’ situation on the plan. Totally, two phases have been discovered in this site:The 1st phase: including an Islamic period.The 2nd phase: including stone architecture/rubble work associated settlement floors, historical period.In this site we had old dam in jare,that we done dating and isometric maps from dam.The samples were collected by myself using the particular instruction that was given to dr fattahi as sampling procedure the samples were collected in metal tubes and both end were sealed and covered by aluminium foils and stored in light tight bages .these are assumed were not exposed to mixing or light-exposure during sampling or transportation until processed.the osl signal of sediment is roduced with exposure to light,thus care must be taken not to expose the sediment to light during sampling, transportation and sample preparation.Dating is relatively new technique used to determine the date at which mineral grains in the sediment were last exposed to sunlight.after burial,radiation accumulates due to the decay of trace amounts of radioactive isotopes found all soils and sediments.This article provides a brief summary of the procedures employed and results obtained for samples.optically stimulated luminescence (OSL).

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S08-P-234

GEOCHEMISTRY OF EARLY HOLOCENE POTTERY: EVIDENCE FROM TIN TARTAïT ROCK-ART SHELTER (TASSILI N’AJJER, CENTRAL SAHARA)

MESSILI L.(1), QUeRRÉ G.(2), SalIÈGe J.f.(3), boUQUIllon a.(4), blanc-ValleRon M.M.(5), RoMaIn o.(1), GalleT X.(1), fRoHlIcH f.(1)

(1) UMR 7194 cnRS / MnHn, PaRIS, fRance;(2) UMR 6566 cnRS / Univ Rennes I, RenneS, fRance;(3) UMR 7209 cnRS / MnHn, PaRIS, fRance;(4) UMR 171 cnRS - c2RMf, PaRIS, fRance;(5) UMR 5143 cnRS / MnHn, PaRIS, fRance

AbstractThis paper aims at setting out first-hand data from pottery in the Tin Tartaït rock-art shelter (Tassili n’Ajjer, SE Algeria). Particular attention will be paid to taxonomic, compositional, plant contents, δ13C geochemistry and 14C dating inputs. Cross-referencing transversal data shows that the series belongs to the earliest pottery-bearing cultures in the Tassili n’Ajjer - Tadrart Acacus area (World Heritage list). Decorative motifs and techniques are of pre-Pastoralpattern, as archaeologically evidenced elsewhere inthe Central Saharan massifs (Libya, Algeria, Niger), Tenere and Azawagh (Niger and Mali). As far as human settlement in arid zone environments is concerned, compositional data clearly contrast the highlands - where the archaeological material has been excavated (the Inner Tassili n’Ajjer outcrops: Cambrian-Ordovician sandstones) - with the Tassili foothills and lowlands, most likely to be the area where the pottery raw materials originate (Precambrian granites of the Saharan shield). Unexpectedly, the good state of conservation of the potteryplant contents- macro-remains, epidermal tissues, «in situ» phytoliths, determinable casts - contrast with this 9th-8th millennium cal. BP coarse, low-fired earthenware. Indeed, 14C dating thus obtained directly from pottery samples, and δ13C values, are in concordance with the chronocultural and ethnobotanical framework (pollen and macroremains) from the neighbouring Tadrart Acacus area (SW Libya), also evidencing an increasing relevance of Poaceae/Panicoïdeae (wild Gramineae) in archaeological contexts since the early Holocene.

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S08-P-235

RADIOCARBON DATING AND CALENDAR TIME SCALES OF LEAD AND SILVER METALLURGY INDUSTRY RECORDED IN THE PEAT PROFILES FROM THE UPPER SILESIA

PAZDUR A.(1), HenSel Z.(2), cHRÓST l.(3), TUDYKa K.(1)

(1) Institute of Physics, Silesian University of Technology, GlIWIce, PolanD;(2) Institute of archaeology and ethnology, Polish academy of Sciences, WaRSaW, PolanD;(3) laboratory for ecological Research, Measurements and expertise eKoPoMIaR, GlIWIce, PolanD

AbstractThe increased amount of lead in the old peat deposits was first detected near Wolbrom (Upper Silesia, southern Poland). According to radiocarbon dating it corresponded to 9th century AD. Further, large scale multi-proxy studies involving radiocarbon dating, elemental analysis and charcoal content were carried out on multiple peat deposits located in the Upper Silesia. Those studies occurred to be very valuable. In 5 out of 15 investigated peat cores the increased amount of metals was identified and this increase was dated back to 3000 BC with use of radiocarbon method. Particularly the peat deposits situated near the drainage basin of the Brynica river (Upper Silesia) were found to be important sites, because some charcoal chunks were found in the peat from this region. The charcoal chunks and metal content (Pb, Zn, Cu) have been in a good correlation since this time. In 8 out of 15 investigated peat cores significant amounts of metals concentration (Pb, Zn, Cu, Ag) have been noticed and dated to 830 AD.The calendar chronology of lead and silver metallurgy is the first study based on radiocarbon dating for the Upper Silesia Region. From the historical point of view, the precise determination of the beginning of local smelting based on Pb and Zn ores rich in Ag is very important as the history and prehistory of metallurgy in this region is very poorly known.

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S08-P-236

ACCELERATOR MASS SPECTROMETRY 14C DATING OF MORTARS:METHODOLOGICAL ASPECTS AND FIELD STUDY APPLICATION AT CIRCE (ITALY)

LUBRITTO C.(1)(2), MaRZaIolI f.(2), nonnI S.(3), RUGGIeRo G.(4), eRaMo G.(4)

(1) University of naples, caSeRTa, ITalY;(2) Dep. environmental Science cIRce II Univ. naples, caSeRTa, ITalY;(3) Dipartimento di Scienze della Terra, Università la Sapienza, RoMa, ITalY;(4) Dipartimento Geomineralogico, Università degli Studi di bari., baRI, ITalY

AbstractMortars represent a class of material basically constituted by a mixture of different phases and are widely used for constructive uses and artworks. The possibility of accurate radiocarbon dating for mortars represents one of the major issues in archaeology studies.In this paper results coming from a multidisciplinary approach will be discussed with the main aim to reconstruct the absolute chronology of a Late Roman cemetery complex found at Ponte della Lama (Canosa di Puglia, Italy), putting a specific emphasis on the Basilica. This building is particularly interesting for the coexistence of different interpretations on its age, its role in the complex and an eventual attendance of rehashes.Radiocarbon dating of mortar lime lumps were performed by means of a new protocol (CryoSoniC, developed at CIRCE - Centre for Isotopic Research on Cultural and Environmental heritage) and coupled with archaeological and mineralogical analyses in order to compare independent age estimations. Two or more mortar samples from the same wall stratigraphic units were taken. In particular, a petrographic characterization performed by means of of thin section observations, showed the coexistence of different sources of carbonates (i.e. calcination relics, calcareous rock fragments and original lime putty), which could affect age estimation introducing the «dead carbon effect». Hereby, a comparison between the absolute chronology of samples performed by lime lumps, mortar and charcoal (when found) will be shown, with the aim of a preliminary reconstruction of the chronology of the basilica development. Accuracy of the procedure was tested applying the CryoSoniC dating procedure for lumps to a funerary inscription of well constrained age.

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S08-P-237

SOCIAL ARCHAEOLOGY IN THE MEDIEVAL SITE OF ZABALLA (SPAIN): RADIOCARBON DATING AND PALEODIETARY STUDIES

LUBRITTO C.(1), QUIRoS caSTIllo J.a.(2)

(1) Dep. environmental Science cIRce II Univ. naples, caSeRTa, ITalY;(2) Departamento de Geografía, Prehistoria y arqueología, Universidad del País Vasco, VIToRIa GaSTeIZ, SPaIn

AbstractThe medieval archaeological site of Zaballa is a rural settlement located in the province of Álava (Basque Country, Northern Spain). The site has been escavated in the context of a rescue archaeology project, in an area of about 6ha, and has allowed to recognize an occupation of the site in a period of time which ranges from 6th to the 15th century.The archaeological analysis has showed how the village was organized, the importance of the spaces of production (cultivation, storage areas, craft areas) and of the S. Tirso church with the adjoining cemetery.In this paper, using a multidisciplinary approach, we present the results of the studied aimed at the social analysis of the archaeological record of the site in Zaballa, with the aim of understanding the articulation of the peasant community, the presence of political and economic power in the village that has influenced the morphology and the economic structure of the village itself.Measurements of different parameters (stable and radioactive isotopes, bioarchaelogical records,) and studies based on the systematic use of the material sources (archaeological materials, human remains, archaeological contexts, written evidence) are discussed.In particular, radiocarbon dating of different organic remains (charcoal, bone), and analysis of C and N stable isotopes of bone collagen, give us an important key to study the absolute chronologically reconstruction and dietary habits of studied populations. In particular it was noted that the site was occupied by a small farm from the 6th century, and was transformed into a village with many residents from the 8th century. Then in the 10th century a church was built in town: the archaeological markers and the paleodiet analysis confirm the existence of a strong social hierarchy outside the village community (incomes lordship). These social differences are also visible in the contexts of 11th-12th century. During the 13th century the village falls under the sway of a powerful local family, which determines the partial abandonment by leaders of the local community, and then the site has turned into a farm with a oriented production of a few agricultural products. Finally, the village is completely abandoned in the 15th century.

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S08-P-238

CHRONOLOGY OF THE PIT-GRAVE CULTURE IN THE AREA BETWEEN VOLGA AND URAL RIVERS BASED ON RADIOCARBON DATING AND PALEOPEDOLOGICAL RESEARCH

KHOKHLOVA O.(1), MoRGUnoVa n.(2)

(1) Institute of physicochemical and biological problems in soil science of the Russian academy of Sciences, PUSHcHIno, RUSSIan feDeRaTIon;(2) orenburg pedagogical State University, oRenbURG, RUSSIan feDeRaTIon

AbstractOver the last 10 years in Orenburg region, Russia it has investigated 3 kurgan groups of the Pit-Grave culture using complex archaeological, paleopedological approaches and radiocarbon dating. 20 kurgans and 21 burials were generally known. In addition, the radiocarbon dating for other monuments of the Eneolithic and Early Bronze Ages within Volga and Ural region from excavations of the second half of the twentieth century has been carried out.Based on investigation of paleosols buried under kurgans, four chrono-intervals have been allocated from which the first two are two stage of the developed Pit-Grave culture period, the third – the transitional time between developed and late periods of that culture and the forth – the late stage of the Pit-Grave (Poltavkivo) culture. In general, the first three stages were characterized by favorable climatic conditions with more humid climate than at present. The initial signs of aridity become noticeable in the final stage of the Pit-Grave culture.Radiocarbon dating has been carried out using all possible carbonaceous materials including humic horizon of buried soils; tree, human and animal bones, ceramics from burials in different radiocarbon laboratories. More than 50 14C-dates for kurgans of the Pit-Grave culture within Volga and Urals steppe region have been received.For burials of the first allocated stage within developed period of the Pit-Grave culture (Shumaevo, Mustaevo archaeological sites) the following 14C-dates have been obtained: 4300 ± 150; 4290 ± 80; 4480 ± 100; 4330 ± 100 and others (3300 – 3000 ВС). For the second stage of the developed period (Shumaevo, Mustaevo and Skvortsovka archaeological sites) - 4100 ± 40; 4060 ± 120; 4030 ± 120; 4070 ± 45; 4080 ± 100; 4200 ± 60; 4090 ± 90 BP and others (3000 – 2500 ВС). The third stage (Skvortsovka archaeological site) - 3920 ± 90; 3940 ± 70; 3810 ± 25; 3810 ± 40; 4080 ± 60 BP (2600 – 2200 ВС). And the final stage of the culture (Poltavkino stage) has been dated by 3790 ± 90; 3610 ± 190 BP (2200 – 2000 ВС).The Early period of the Pit-Grave culture has been dated by ceramics from burials and settlements of Repino type: dates from 5140 ± 70 till 4730 ± 90 BP (4000 – 3400 ВС)The Pit Grave culture in the Volga region formed on the basis of the Khvalynskaya Eneolithic culture in the development of which the kurgan burial rite originated. The time of kurgans appearance in the region has been determined within the framework of 4500-4000 BC.Thus, the study of archaeological typology of funeral monuments of the Pit-Grave culture against the paleopedological determination of relative chronological order of kurgans construction together with radiocarbon dating allowed us to fix the chronological limit for all the Pit-Grave culture, sequence and duration of separated stage of its development in steppe area between Volga and Ural region.

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S08-P-239

EARLY SETTLEMENT OF ICELAND, ARCHAEOLOGICALLY UNACCEPTABLE?

THEODORSSON P.

Science Institute, ReYKJaVIK, IcelanD

AbstractIn the history of radiocarbon dating, there are many examples of initial rejection of results that gave significantly higher age than expected, results that that were considered archaeologically unacceptable and debated hotly for many years. One of the last and most prolonged of these, still disputed after 35 years, is the dating of the beginning of settlement in Iceland. Trustworthy radiocarbon measurements in the 1970s strongly indicated a beginning of settlement shortly after AD 700. This was considered unacceptable as it has always been believed that it began about AD 870, as vividly described in detail in a medieval text, which was written about AD 1120.The high radiocarbon results were first rejected on the basis of a hypothesized local depression in the 14C concentration over Iceland. When measurements disproved it about 15 years later, it was soon replaced by a new one that assumed that the first generations of settlers collected for fuel very old dead birch branches that were assumed to be abundant on the bottom of the woods. A study apparently confirmed the new hypothesis and it was declared that wood samples from the settlement time period do not give the true date of human occupation. The hypothesis is evidently false, the authors failed to take into account the fact that dead branches decay in a few years. This has nevertheless seriously affected radiocarbon dating in Icelandic archaeology as practically only negligible own-age animal bones have been dated during the last 10 years. However, these are rarely found in ancient house ruins where charcoal is usually abundant. Despite various other convincing evidence of early settlement the some reluctant scientists still believe that the high radiocarbon ages of charcoal can be explained by old birch wood used for fuel. By quantitative analysis it is shown that the influence of the own-age of the dated charcoal samples is more complex than usually assumed and that it can not affect the main conclusion of early settlement.

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S08-P-240

DATING AND STABLE ISOTOPE ANALYSIS OF CHARRED RESIDUES ON THE INCIPIENT POTTERY IN THE JOMON PERIOD.

YOSHIDA K.(1), KUnIKITa D.(2), MIYaZaKI Y.(1), MaTSUZaKI H.(1)

(1) The University of Tokyo, ToKYo, JaPan;(2) The University of Tokyo, KITaMI, JaPan

AbstractAbout 50 ruins of the Incipient stage in the Jomon period are around Tsunan-machi in Niigata prefecture where Shinano River and the Kiyotsu River flow together. Pottery sherds of 8 ruins in the above area and 3 ruins in the other region were analyzed. Radiocarbon dates of charred residues on pottery sherds were measured for more than 50 samples. Furthermore, carbon and nitrogen stable isotope analysis were conducted about those samples for dietary reconstruction.The Incipient stage may be divided into 4 terms by change of pottery type. It is thought that the analyzed samples belong to 2nd~3rd terms based on pottery type. The radiocarbon dates are distributed in 12,700 BP - 10,500 BP, and are divided into the old group of about 12,500 BP, and a group newer than 12,000 BP. The group of dates is well in agreement with the difference in pottery type.Stable isotopic ratios of carbon (δ13C) and nitrogen (δ15N) and carbon nitrogen atomic ratios (C/N) were measured by EA-IRMS system. Several residual substances are considered to have produced as a result of cooking the foods containing marine products. Since ruins are far from the sea, having boiled an ascension fish like a salmon or a trout is presumed. The result will be discussed as compared with the result of the flame style pottery used in the Middle stage of the Jomon period in the same area.

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S08-P-241

FIRST 14C DATES FOR ALTERNATIVE BURIAL RITUALS OF THE DOLMEN CULTURE IN THE WESTERN CAUCASUS

ZAYTSEVA G.(1), TRIfonoV V.(1), Van DeR PlIcHT J.(2), boURoVa n.(1), SeMenTSoV a.(1), RISHKo S.(1)

(1) Institutute for History of Material culture, ST.PeTeRSbURG, RUSSIan feDeRaTIon;(2) center for Isotope Research, GRonInGen, neTHeRlanDS

AbstractFrom the end of the 4th/beginning of the 3rd through the last quarter of the 2nd millennium BC, the western slopes of the Caucasus Mountains were occupied by archaeological cultures known by dolmens. These megalithic constructions are distributed on both slopes of the Great Caucasus range and the Black Sea coastline from the Taman Peninsula in the NW to the Kolkhida Depression in the SE.At present, over 3,000 dolmens are known. They are characterised by a porthole opening at the front. It is generally accepted that the Caucasian dolmens were used as collective tombs, and recent discoveries reveiled detailed dolmen burial rituals.The radiocarbon dates obtained for the «Kolikho» dolmen (Tuapse region, Black Sea, Russia) show that this single dolmen was in use for about 450 years during 1800 - 1300 BC. During this period, more than 70 bodies were accumulated in the burial chamber of the dolmen. At Kolikho, the bodies were stored until they were de-fleshed and held together by residual ligaments, allowing the subsequent final deposition of the remains into the burial chamber through the porthole. This opening (25-45 cm in diameter) is large enough to push through a body or set of bones, including the skull.The question now is whether this dolmen burial ritual was the only one of its kind, or that people of the dolmen culture practiced different burial rituals at the same time.Fortunately, about 1 km SW of the Kolikho dolmen, a cemetery was discovered by chance in 2008. Like the dolmen, it was buried under a 5 m thick alluvial deposit. Two ground cist-type single burials were investigated. The remains of two partially de-fleshed bodies were deposited in one of the cists, while in the other one skeleton of young man in supine position was found. The same kind of pottery was found as in the Kolikho dolmen. Raiocarbon dates for the single graves were obtained from St.Petersburg and Groningen. They correspond to the same period when the Kolikho dolmen was in use.For the first time, the territorial, cultural and chronological identity of collective burials in dolmen and single burials in cist-type tombs clearly demonstrate the coexistence of two alternative burial rituals of the dolmen culture in the Western Caucasus during the second millennium BC.What lies behind the different customs: were the single graves for lower class people, or simply for those who did not follow the megalithic tradition and had their own ways of honoring the dead?

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S08-P-242

THE SETTLEMENT DATE OF ICELAND REVISITED. EVALUATION OF 14C DATES FROM SITES OF THE FIRST SETTLERS IN ICELAND BY BAYESIAN STATISTICS

SVEINBJORNSDOTTIR A.E.(1), RaMSeY c.(2), HeIneMeIeR J.(3)

(1) Institute of earth Sciences, University of Iceland, ReYKJaVIK, IcelanD;(2) oxford Radiocarbon accelerator Unit, University of oxford, oXfoRD, UnITeD KInGDoM;(3) aMS 14c dating centre, Department of Physics and astronomy, aarhus University, aaRHUS, DenMaRK

AbstractThe settlement time of Iceland has been debated for years as 14 C dates of charcoal samples have been interpreted to give earlier age than the Sagas, i.e. written sources from the 12th century (AD 874) and 14 C reservoir corrected dates of human remains of early settlers (Sveinbjörnsdóttir et al., 2009). Old wood effect for the charcoal has been suggested to explain this controversy (Sveinbjörnsdóttir et al. 1994). Supporting that explanation is the exact date AD 871±2 from Grönvold et al. (1995), for the tephra layer that is located in soil profiles where change in land use due to settlement is recognized. Most of the charcoal samples are taken above this tephra layer (Settlement tephra layer) and therefore their earlier 14 C age cannot be reflecting the true age of the soil layers they are found in.We have used a Bayesian model, implemented in the OxCal program (Ramsey, 1995, 2001), which takes into account the stratigraphic constraints on samples. This gives us information on the likely age of the wood used in construction, and on the possible range of dates for key events.

References1. Grønvold K, Óskarsson N, Johnsen SJ, Clausen C, Hammer CU, Bond G, Bard E. 1996. Ash layer from Ice- land

in the Greenlandic GRIP ice core correlated withoceanic and land sediments. Earth and Planetary Science Letters 135:149-55.

2. Ramsey C. 1995. Radiocarbon Calibration and Analysis of Stratigraphy: The OxCal Program. Radiocarbon 37(2): 425-30.

3. Ramsey C. 2001. Development of the radiocarbon calibration program OxCal. Radiocarbon43(2A): 355-63.4. Sveinbjörnsdóttir AE, Heinemeier J, Gudmundsson G. 2004. 14C datings and the settlement of Iceland.

Radiocarbon, 46, 387-394.5. Sveinbjörnsdóttir ÁE, Heinemeier J, Arneborg J, Lynnerup N, Ólafsson G, Zoega G. 2010. Dietary reconstruction

and reservoir correction of 14C dates on bones from pagan and early Christian graves from Iceland. Proceedings of the 20th international Radiocarbon Conference, edited by A.J.T, Jull. Radiocarbon 62, 682-696.

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S08-P-243

THE OCCUPATION HISTORY ON ISHIGAKI ISLAND, OKINAWA, JAPAN, DURING THE LATE PLEISTOCENE AND EARLY HOLOCENE

YONEDA M.(1), GaKUHaRI T.(1), TaKIGaMI M.(2), naITo Y.(3), ITaHaSHI Y.(1), IToH S.(4), KobaYaSHI K.(4), DoI n.(5), KaTaGIRI c.(6), YaMaSaKI S.(6), fUJITa M.(6)

(1) The University of Tokyo, ToKYo, JaPan;(2) Yamagata University, YaMaGaTa, JaPan;(3) JaMSTec, YoKoSUKa, JaPan;(4) Paleo labo co., ltd., KIRYU, JaPan;(5) University of Ryukyus, oKInaWa, JaPan;(6) okinawa Prefectural Museum & art Museum, oKInaWa, JaPan

AbstractThe maritime adaptation of early modern humans is an important issue to understand the human dispersal from Africa to Asia. In 2008, a series of Pleistocene human remains were recovered from the Shiraho-saonetabaru cave on Ishigaki Island, Okinawa Prefecture, Japan and we determined their antiquity by direct measurements of their radiocarbon ages around 20 ka BP (Nakagawa et al. 2010). Here, we will report the preliminary results of radiocarbon dating on the new materials from the 2010 excavation at the site to reconstruct the occupational history on a remote small island during the late Pleistocene and early Holocene.

ReferencesNakagawa, R., N. Doi, Y. Nishioka, S. Nunami, H. Yamauchi, M. Fujita, S. Yamazaki, M. Yamamoto, C. Katagiri, H. Mukai, H. Matsuzaki, T. Gakuhari, M. Takigami, and M. Yoneda (2010). The Pleistocene human remains from Shiraho-Saonetabaru Cave on Ishigaki Island, Okinawa, Japan, and their radiocarbon dating. anthroplogical Science 118(3), 173?183.

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RADIOCARBON DATING THE EXPLOITATION PHASES OF THE «GROTTA DELLA MONACA» CAVE IN CALABRIA, SOUTHERN ITALY: A PREHISTORIC MINE FOR THE EXTRACTION OF IRON AND COPPER

QUARTA G.(1), laRocca f.(2), D’elIa M.(1), calcaGnIle l.(1)

(1) ceDaD,, DePT. of enGIneeRInG of InnoVaTIon, UnIVeRSITY of SalenTo, lecce, ITalY;(2) centro Regionale di Speleologia «e. De Medici, RoSeTo caPo SPUlIco (cS), ITalY

AbstractThe cave named «Grotta della Monaca» is a carsic cavity located in Calabria-Southern Italy. In this cave recent researches and systematic archaeological excavations, carried out by the University of Bari, allowed to recognize an extensive prehistoric mining activity, aimed at the exploitation of iron and copper minerals. Iron minerals extracted were identified as goethite (an iron hydroxide) and the lepidocrocite, a polymorph of goethite. Copper minerals were extracted mainly as carbonates (malachite and azurite). These mineral resources, which were largely present in the cavity, were extracted in portions of the cave up to 200 m from the entrance, in hardly accessible and completely dark areas. Several mining tools, made of bones and stone, were found in an excellent preservation status together with clear traces of the extraction activities along the veins of minerals. The mining site of Grotta della Monaca represents, in the Mediterranean area, a contexts of great importance for the reconstruction of the ancient strategies for the catchment of mineral resources.In order to identify and absolutely date the different exploitation phases several charcoal and bone samples were selected and submitted to AMS radiocarbon dating at CEDAD, University of Salento. The samples were taken in different areas of the cave and for the bone samples, from different burials found in the cave. The radiocarbon dating results revealed an extremely long period of exploitation and occupation of the cave which started in the Upper Paleolithic (about 20 ka cal BP) to become more intense in more recent periods, particularly during the 5th and 4th millennium BC.

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S08-P-245

THE STRANGE CASE OF THE ANKHPAKHERED MUMMY: RESULTS OF THE AMS 14C DATING

QUARTA G.(1), MalGoRa S.(2), D’elIa M.(1), calcaGnIle l.(1), MaRUccIo l.(1), Gaballo V.(1), bRaIone e.(1), coRVaGlIa c.(1)

(1) ceDaD,, DePT. of enGIneeRInG of InnoVaTIon, UnIVeRSITY of SalenTo, lecce, ITalY;(2) curator egyptian Section of buonconsiglio castle, Trento, and co-director Mummy Project, MIlano, ITalY

AbstractThe Ankhpakhered mummy and the wooden sarcophagus which contained it are part of the collection of the Archaeological and Paleontological Museum in Asti, Italy. The anthropomorphic sarcophagus, has been dated, on the base of archaeological consideration connected to the construction features to the period between the 22th and the 23th dynasties (945-715 BC). A hieroglyphic inscription found on the sarcophagus allowed to attribute it to a man named Ankhpakhered, a priest of the Min god. In the sarcophagus a 165 cm long mummy was found with unusual features which were soon recognized during the restoration works and the following radiological and X-Ray tomography analyses. In fact these analyses demonstrated that wrapped in the bandages there was a skeleton more than a mummified body. Furthermore the skeleton was not in anatomical order but the different bones were put together in a quite rough manner laying of a twenty-one reeds. On the base of these analyses a possible re-use of the sarcophagus was suggested. To verify this hypothesis different kind of materials were selected from the skeleton and the inner part of the sarcophagus, sampled with endoscopic tools and submitted to 14 C AMS radiocarbon dating analyses at CEDAD. FTIR (Fourier Transform Infrared) analyses were also carried out in order to check the preservation status of the bone collagen and to identify some organic residues found associated with the skeleton. All the analyzed samples (bones, reeds, bandages, teeth) gave overlapping radiocarbon ages dating to the skeleton and its wrapping to the 4th-2nd centuries BC which were thus well younger than the sarcophagus in which it was found.

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BERENIKE: DATING THE FLUCTUATING FORTUNESOF A PTOLEMAIC AND ROMAN PORT TOWN

KOTARBA-MORLEY A.(1), Dee M.(1), TRZcInSKI J.(2)

(1) University of oxford, oXfoRD, UnITeD KInGDoM;(2) University of Warsaw, WaRSaW, PolanD

AbstractBerenike was the most important harbour on the Egyptian Red Sea during the Ptolemaic and Roman Periods. Its geographic position was extraordinarily propitious due to the fact that it possessed two natural harbours, both of which were protected against the prevailing northern winds, and because it was located on the large peninsula of Ras Benas - an ancient viewshed. The city prospered for over eight centuries, from its foundation in the 3rd century BC by Ptolemy II Philadelphus to the 6th century AD. This poster aims to provide an updated archaeological interpretation of Berenike from a geoarchaeological auger hole and coastal geomorphological surveys recently undertaken at the site. Sedimentological analyses have been used to recreate the palaeoenvironments of the site, with radiocarbon dates obtained to anchor these changes in time. The work is re-writing the story of the first settlement of Berenike in Ptolemaic times, the subsequent occupational hiatus, and the ultimate re-occupation of the site in the Early Roman period. The results are also providing information on relative sea level change in the Red Sea and its potential effect on the harbour city. Berenike was an influential emporium which played a significant and leading role in long-distant trade routes between the Mediterranean, the Indian sub-continent, Arabia and sub-Saharan Africa. Therefore, the importance of understanding the chronological pattern of the development and decline of this harbour city should not be underestimated.

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454

S08-P-247

RADIOCARBON WIGGLE-MATCH DATING OF AN UNUSUAL MID-SECOND MILLENNIUM BC TREE-RING GROWTH ANOMALY

MANNING S.(1), bRonK RaMSeY c.(2), WIlD e.(3), PeaRSon c.(1), GRIGGS c.(1), bRocK f.(2)

(1) cornell University, ITHaca, UnITeD STaTeS;(2) oxford University, oXfoRD, UnITeD KInGDoM;(3) University of Vienna, VIenna, aUSTRIa

AbstractAn unusual growth anomaly (with growth surges of 200-700% of normal) has previously been reported in a large group of wood samples recovered from archaeological excavations at Porsuk, Turkey (Manning et al. 2001; Pearson et al. 2009). Over 61 different samples (trees) register this anomaly, including three different conifer species (Juniperus, Pinus and cedrus), and trees of widely varying ages from 19 to 237 years old at the time of the growth anomaly. This growth anomaly has previously been dated to c. 1650 BC by dendrochronological methods comparing the tree-ring growth patterns in the Porsuk series versus those in the near-absolutely dated (high-precision radiocarbon wiggle-match) Gordion tree-ring series. In order to check the dendrochronological placement of the Porsuk series, and to obtain an independent assessment of the date of the growth anomaly, we have undertaken a radiocarbon wiggle-match study on samples of juniper from the Porsuk tree-ring series. Pretreatment and dating issues will be reviewed, and the best placement of the Porsuk tree-ring series proposed on the basis of both radiocarbon evidence and dendrochronology. We end with a consideration of possible associations for this unusual growth anomaly.

References1. Manning, SW, Kromer, B, Kuniholm, PI & Newton, MW 2001. Anatolian tree-rings and a new chronology for

the east Mediterranean Bronze-Iron Ages. Science 294:2532-2535. 2. Pearson, CL, Dale, DS, Brewer, PW, Kuniholm, PI, Lipton, J & Manning, SW 2009. Dendrochemical analysis of

a tree-ring growth anomaly associated with the Late Bronze Age eruption of Thera. Journal of archaeological Science 36: 1206-1214

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455

14C MORTAR DATING: THE CASE OF THE MEDIEVAL SHAYZAR CITADEL, SYRIA

NONNI S.(1)(2), MaRZaIolI f.(1)(3), Secco M.(4), PaSSaRIello I.(1), caPano M.(1)(5), lUbRITTo c.(1)(3), MIGnaRDI S.(6), TonGHInI c.(7), TeRRaSI f.(1)(3)

(1) cIRce laboratory - InnoVa, caSeRTa, ITalY;(2) Dottorato di Ricerca in Scienze applicate alla Protezione dell’ambiente e dei beni culturali c/o Dipartimento Scienze della Terra - Sapienza Università di Roma, RoMe, ITalY;(3) Dipartimento di Scienze ambientali - Seconda Università degli Studi di napoli, caSeRTa, ITalY;(4) Dottorato in Scienze della Terra c/o Dipartimento di Geoscienze - Università degli Studi di Padova, PaDUa, ITalY;(5) Seconda Università degli Studi di napoli, SanTa MaRIa caPUa VeTeRe, ITalY;(6) Dipartimento Scienze della Terra - Sapienza Università di Roma, RoMe, ITalY;(7) Dipartimento di Studi sull’africa e sull’asia Mediterranea - Università ca’foscari di Venezia, VenIce, ITalY

AbstractThis paper reports on the application of a new protocol of 14C mortar dating on some lime mortars from Shayzar Castle (Syria). Shayzar, a citadel built on a rock massif, is one of the most important examples of medieval fortifications in the Middle East. The archaeologists worked to collect all information aiming the reconstruction of the building chronology that goes from the second half of X century to the beginning of XV century AD, although the use of the site brings written accounts from the II millennium to the early twentieth. The aim of this study is to confirm the archaeological expectation, attributed with the analysis of construction phases and historical evidences, by radiocarbon measurements on mortars. It is known that radiocarbon dating of mortars requires the determination of 14C concentration in carbon, derived from atmospheric CO2 incorporated in mortar carbonates during their hardening process. In this case, a method of samples preparation developed at CIRCE (Centre for Isotopic Research on Cultural and Environmental heritage) and capable to provide a reliable mortar dating was applied. The CryoSoniC protocol (cryobraking, Sonication and centrifugation), is able to remove contributions potentially affecting the measured radiocarbon age, such as dead carbon (deriving from different sources like unburned limestone or carbonate aggregates) or recrystallization phenomena. To check the quality of dating procedure the 14C content of charcoals, extracted from the analyzed mortars, was measured and taken as reference for comparison with mortar data. Petrographic and mineralogical analysis in thin section by optical microscopy, X-ray diffraction and SEM investigations were carried out for the characterization of mortar samples in order to verify the occurrence of some attributes which can influence the outcome of the dating. The obtained results are in line with what expected, both at methodological and archaeological level: there is a close coherence between mortar and charcoal ages. The application of CryoSoniC procedure, on these archaeological samples revealed an overall good accuracy indicating this protocol as feasible option for the finer characterization of the same site both to extend the chronological attributions of construction phases and to solve possible ambiguities on dating.

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456

S08-P-249

RADIOCARBON DATING PREHISTORIC POTTERY FROM NORTHERN EUROPE

PHILIPPSEN B.(1), cRaIG o.e.(2), HeRon c.P.(3), HaRTZ S.(4), GlYKoU a.(4), HeIneMeIeR J.(1)

(1) aMS 14c Dating centre, aaRHUS, DenMaRK;(2) bioarch, Department of archaeology, University of York, YoRK, UnITeD KInGDoM;(3) archaeological Sciences, University of bradford, bRaDfoRD, UnITeD KInGDoM;(4) Stiftung Schleswig-Holsteinische landesmuseen, Schloss Gottorf, ScHleSWIG, GeRManY

AbstractDirect dating of the pottery is an important goal in archaeological research and many attempts have been made using radiocarbon. One important goal has been to date the earliest pottery in a region to assess the origin and dispersal of ceramic technology. Also with the increasing application of organic residue analysis to study pottery use, it has become important to combine residue data with direct dates on the artefact being investigated. In this study we have radiocarbon dated different organic materials associated with archaeological potsherds from three Ertebølle sites in Northern Germany. These are hunter/fisher/gatherer sites located in coastal or riverine setting and correspond to some of the earliest pottery bearing sites in this region. We have chosen to radiocarbon date different fractions on the pottery including «foodcrusts» (charred deposits from the inner surface of sherds), «soot» (charred deposits from the outer side of sherds), plant remains from inside the clay matrix, and lipids extracted from the ceramic matrix. All of these are potentially problematic media for AMS dating: ‘Foodcrusts’ and absorbed lipids can appear too old because of the marine or freshwater reservoir effect, such as when aquatic products have been prepared in the pottery. Soot can derive from old wood that was used for the hearth fire, or from (potentially aquatic) food that boiled over. Plant remains may have been present in the clay for a long time before manufacture of the pottery. Post-depositional contamination with organic carbon, such as humic acids, may also be problematic. We present these data with radiocarbon datings of contemporaneous terrestrial and aquatic samples to find out the true age of the pottery and estimate the reservoir age. Lipid analysis and bulk carbon and nitrogen stable isotope measurements are used to give additional information about the former contents of the pottery and the risk of reservoir effects.

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457

PRELIMINARY RADIOCARBON ANALYSES ON OSTEOLOGICAL AND PALEOBOTANICAL SAMPLES IN THE ARCHAEOLOGICAL AREA OF MARIGLIANO (NAPLES, ITALY)

PASSARIELLO I.(1)(2), caSTalDo n.(3), MaRZaIolI f.(1)(2), caPano M.(1)(4), bUonInconTRI M.(5), DI PaSQUale G.(5), VeccHIo G.(3), ToRIno M.(6), TeRRaSI f.(1)(2)

(1) cIRce aMS laboratory-InnoVa, caSeRTa, ITalY;(2) Dipartimento di Scienze ambientali, Seconda Università degli Studi di napoli, caSeRTa, ITalY;(3) Soprintendenza Speciale per i beni archeologici di napoli e Pompei, naPolI, ITalY;(4) Dipartimento di Studio delle componenti culturali del Territorio, Seconda Università degli Studi di napoli, SanTa MaRIa caPUa VeTeRe, caSeRTa, ITalY;(5) Dipartimento di arboricoltura, botanica e Patologia vegetale.Università di napoli federico II, naPolI, ITalY;(6) laboratorio di archeoantropologia, Università Suor orsola benincasa, naPolI, ITalY

AbstractWithin the framework of research undertaken on the archaeological site of Marigliano (Naples, Italy) and other sites of the Nola area (Naples, Italy), several radiocarbon measurements of both well-preserved wood and charcoal, coming from agricultural attending areas placed at the edge of «scattered» rural character settlements, and osteological remains, coming from annexed burial contexts, were carried out. The investigated sites (Marigliano-Faibano, San Paolo Belsito, Nola, Palma Campania, Tufino), all sealed by the Pollena eruption of Somma-Vesuvius (end V - early VI AD) and in use in an period of time immediately preceding the eruptive catastrophe, refer to re-attendance or settlement continuity of areas already occupied before the eruption. The study started in the Nola area, through contributions of different applied disciplines, by means of analyses and correlation among the various investigated sites. This approach has highlighted important information about the settlement and economic dynamics that affected the area between the late antique and High Middle Ages (III-VIII AD), allowing the reconstruction of a singolar «picture» about the attendance at these historical phases. The important discovery of the wetland area of Marigliano, in particular, with well-preserved wood, including scraps of lives, opens a window on the paleoenvironmental reconstruction and on the interference and use of natural resources by humans, as well as their adaptation to even less «favorable» environmental conditions.The necessary support of radiocarbon dating, especially in those contexts where there are no other elements useful for a precise chronology, aims to confirm and clarify the various development phases of the site. Radiocarbon measurements on samples coming from above cited archaeological sites, like logs, beams, seeds, charcoals and bones, were performed at CIRCE AMS laboratory in Caserta (Italy). From the first archaeobotanical analyses, the wood has been attributed to the group of deciduous oaks, reinforcing the use of deciduous Quercus in Roman construction. Moreover, the branches, which were attributed to the Vitis Vinifera, represent an exceptional find, both for the very good conditions in which the remains were found and for historical and agricultural information on the typically Roman agricultural-wine landscape. Thanks to the findings in Marigliano, then, today it is also possible to extend this information to Ager nolanus. About radiocarbon analyses, the measurements on the woods of Marigliano confirm and further define the chronology of the site, in particular the lives, while the dating on the beam and the charcoal from Nola, are the oldest. However, all the results, including those from other sites, confirm a re-attendance or a settlement continuity of areas before the Pollena eruption. Work in progress of anthropological analyses on some burials coming from necropolis of Marigliano.

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458

S08-P-251

RADIOCARBON DATING OF THE BEYCESULTAN SITE, TURKEY: NEW 14C DATA AND PROBLEM FOR BRONZE AGE CHRONOLOGY ON WESTERN ANATOLIA

OMORI T.(1), abaY e.(2), naKaMURa T.(3)

(1) The University of Tokyo, KaSHIWa, JaPan;(2) ege Üniversitesi, IZMIl, TURKeY;(3) nagoya University, naGoYa, JaPan

AbstractThe archaeological site of Beycesultan in Turkey is one of the key sites in western Anatolia. The site stratigraphy was occupied from the Chalcolithic period to Bronze age and in the Byzantine period, and especially characterized by a massive settlement with religious buildings in the Late Chalcolithic phase and palace and associated structures in the Late Bronze Age phase. First excavations were performed by the British Institute of Archaeology in Ankara in 1950s, and then radiocarbon dating for two charcoal samples from the Late Chalcolithic phase was carried out (Ralph et al. 1962). The radiocarbon dates from 3710 BCE to 3520 BCE were good agreement with archaeological contexts. On the other hand, an absolute date of the Late Bronze Age phase is quite debatable since index ceramic types are feeble in this period. To reconstruct the cultural chronology, archaeological team of Ege Üniversitesi has excavated the Late Bronze Age phase since 2007. For radiocarbon dating, charred wood and grain samples were sampled from building levels in the Late Bronze Age phase. The obtained radiocarbon dates were calculated with 14C Bayesian analysis to estimate the use of building remains. In this paper, we will present the radiocarbon dates of Beycesultan, and discuss the western Anatolian Chronology.

ReferencesRalph E K, Stuckenrath Jr R. 1962. University of Pennsylvania Radiocarobon Dates V. Radiocarbon 4:144-59.

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S08-P-252

CONTRIBUTION OF NEW RADIOCARBON DATES TO TRACK THE IMPACT OF PAST ANTHROPOGENIC DISTURBANCES ON CURRENT VEGETATION IN CENTRAL AFRICA

MORIN-RIVAT J.(1)(2)(3), GIlleT J.f.(1), boURlanD n.(1), GoURleT-fleURY S.(4), oSlISlY R.(5), beecKMan H.(2), DoUceT J.l.(1)

(1) Univ. liège, Gembloux agro-bio Tech, Unité de Gestion des Ressources forestières et des Milieux naturels, laboratoire de foresterie des Régions tropicales et subtropicales, GeMbloUX, belGIUM;(2) Royal Museum for central africa, laboratory of Wood biology and Xylarium, TeRVURen, belGIUM;(3) fonds pour la formation à la Recherche dans l’Industrie et dans l’agriculture (f.R.S/fnRS), bRUXelleS, belGIUM;(4) Unité de Recherche « biens et Services des Écosystèmes forestiers tropicaux », Département environnements et Sociétés du cIRaD, MonTPellIeR, fRance;(5) Institut de recherche pour le développement, UMR 208-IRD/MnHn, Patrimoines locaux, IRD Yaoundé, YaoUnDÉ, caMeRoon

AbstractUnderstanding current Central Africa vegetation patterns faces the scarcity of data about their past evolution. However, a growing hypothesis suggests that past human activities could have had a substantial influence on vegetation. Indeed, creating large openings, they would have triggered the expansion of light-demanding species currently suffering from a lack of regeneration. One of the main explanations would be the change in land use since colonization with the sedentarization of shifting cultivators.In order to investigate the potential relationship between past anthropogenic disturbances and present vegetation, fieldworks combining anthracological and ecological approaches have been undertaken in Northern Congo and South-Eastern Cameroon. Thirty 150-200 cm deep pits were excavated under different forest covers and vegetation types to identify evidences of past human presence (i.e. potsherds, slags of metallurgy, anthropogenic pieces of charcoals and anthropophilous charred seeds). Charcoals and oil palm seeds (Elaeis guineensis)in combination with artifacts have been dated.A set of 26 new radiocarbon dates ranging from 15,200 cal. BP to present time have been obtained. They confirm the existence of important past fire events in a region where natural ones seldom occur. Together with artifacts, our findings support the few already available dates documenting evidences of past human activities in Central African rainforests. The majority of the dates (70%) belongs to the 2,200-1,400 cal. BP period. The whole semi-deciduous forest zone is concerned by this period of intense disturbances. It follows the last great arid phase ca. 2,500 BP and would be linked to the great Bantu migrations. Another pool of dates between 650 and 250 cal. BP (22%) associated with potsherds would be correlated to a dry phase contemporary to the Little Ice Age in Europe. Those dates point out the potential positive impact of anthropogenic disturbances connected to a dry climatic event on light-demanding species populations.Our multidisciplinary approach allowed new insights into the link between human history and vegetation dynamics in Central Africa. Further investigations should be conducted to go deeper into the understanding of the evolution of Central African rainforests and improve the management of logged light-demanding species.

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460

SESSION 9

RADIOCARBON AND ARCHAEOLOGY OF THE AMERICAS AND OCEANIA: IMPROVING

CHRONOLOGIES AND THEORETICAL INSIGHTS

ConvenersN. Beavan (NZL), T. Dillehay (USA), N. Sanz (UNESCo)

DescriptionThe session calls for papers on radiocarbon applications to improve chronologies or contribute to current theoretical debates. The symposium will focus on several major themes related to the Americas (North America, Mesoamerica, South America, the Caribbean) and to Oceania (Australia, New Zealand, Micronesia, Melanesia, and Polynesia):1) the establishment or re-evaluation of regional chronologies via conventional and/or AMS 14C dating, especially in South America;2) correlating radiocarbon dated archaeological patterns and environmental events;3) recent research on human migrations, dispersal of commensal animals or culturally significant floras, and4) the timing of cross-cultural contacts and cultural transitions.

Keywordscultural history, migration, chronologies, contexts

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S09-P-253

CROSS DATING (TH/U-14C) OF CALCITE COVERING PREHISTORIC PAINTINGS AT SERRA DA CAPIVARA NATIONAL PARK, PIAUI, BRAZIL.

FONTUGNE M.(1), SHao Q.(1)(2), fRanK n.(1), boËDa e.(3)

(1) cea, GIf/YVeTTe, fRance;(2) Dept Préhistoire MnHn, PaRIS, fRance;(3) anTeT cnRS UMR7041 Univ ParisX, nanTeRRe, fRance

AbstractSince at least fifty years,the question of when the first humans arrived in the New World’s has been a bone of contention. Similarly, the oldness of rock painting has been constantly debated. The settlements in the Serra da Capivara National Park in has been dated 5ka to more than 50ka far from older than the Clovis barrier. and calcite formation on a rock-wall painting in rockshelter gave ages TL and EPR ages older than 35ka (Watanabe & al, 2003). Calcite deposits covering prehistoric paintings were sampled in several rockshelters (Toca da Bastiana, Toca do Moendas Serrote de Moendas and Toca da Gameleirinha (Pedra pintada)) and 14 C age were measured and Th/U crossed dated in Toca to Gamelerinha. Ages obtained for these calcites are younger than 12ka and suggest that painting could be more recent than proposed by previous studies.

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462

S09-P-254

NEW RADIOCARBON AGES OF LUZIA WOMAN, LAPA VERMELHA IV SITE, LAGOA SANTA, MINAS GERAIS, BRAZIL

FONTUGNE M.

cea, GIf/YVeTTe, fRance

AbstractLuzia woman was considered, until the recent period, as the oldest paleo-indian skeleton found in the Americas. Luzia was found in Lapa Vermelha IV (Lagoa Santa, Minas Gerais, Brazil) in 1975 by archaeologist Annette Laming-Emperaire (1917-77) who sent immediately to Gif laboratory, charcoals collected in the vicinity of the skeleton for radiocarbon dating. Twenty-nine charcoal samples dated in different level of the stratigraphy of the cave allowed to bracket the age between 10200±220 and 12960±300 14C yr B.P. (Délibrias & al Radiocarbon, 1986). Direct datings on bones were unsuccessful due to the lack of collagen (Neves & al 1999). Thirty five years later, a consultation of A. Emperaire’s correspondence revealed several mail envelopes containing few mg of charcoals certainly ignored due to a quantity far too low for beta counting. These charcoal were dated by Saclay AMS facilities and dates confirm the oldness of Luzia, however ages correspond to the lower part of the interval: charcoals inside Luzia’s skull give an age of 10030±60 14C yrs B.P. [cal BP 11243- 11710].

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463

S09-P-255

RADIOCARBON DATING RESIN INLAYS FROM PRE-HISPANIC CARIBBEAN WOODEN SCULPTURES

BROCK F.(1), oSTaPKoWIcZ J.(2), HIGHaM T.(1), bRonK RaMSeY c.(1), RIbecHInI e.(3), STaceY R.(4)

(1) University of oxford, oXfoRD, UnITeD KInGDoM;(2) national Museums, lIVeRPool, UnITeD KInGDoM;(3) University of Pisa, PISa, ITalY;(4) british Museum, lonDon, UnITeD KInGDoM

AbstractThe ‘Pre-Hispanic caribbean Sculptural arts in Wood’ project studied 66 wooden sculptures made by the pre-colonial indigenous people of the Caribbean. Although over 300 such pieces are now held in museums and private collections around the world, little is known about them, or the corpus as a whole. The pieces are carved from single boles of wood, some of them with inlays of resin, shell or guanin (a copper-gold alloy), in a range of forms including duhos, (ceremonial seats), cemís (representations of spirits), platters and vessels.Radiocarbon dates of the resin from these pieces are of particular interest for two main reasons. Firstly, because the resin was likely to have been applied to the pieces fresh during the final stages of manufacture, they should date the carving’s finishing stages, refining the dates achieved on the wood, and overcoming potential issues of in-built age and re-use. Secondly, when the resin dates were younger than those of the wood from the same piece, they demonstrate the continued use of the carving as it was passed from generation to generation.However, radiocarbon dating of the resins was often not straightforward, due to the small amounts of material available, and the requirement for a sampling and pre-treatment protocol which allowed the effective removal of any potential contamination while still retaining sufficient material after pre-treatment for dating.Here we present radiocarbon dates of resin inlays from 12 of the sculptures from the wider study, alongside the plant species from which they came as identified with GC-MS. We discuss the sampling and pre-treatment protocols applied, and the archaeological significance of the dates.

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S09-P-256

A DEVASTATING PLINIAN ERUPTION AT TUNGURAHUA VOLCANO REVEALS FORMATIVE OCCUPATION AT CA 1100 CAL BC IN CENTRAL ECUADOR

LE PENNEC J.L.(1), De SaUlIeU G.(2), JaYa D.(3), SaManIeGo P.(4)

(1) Institut de Recherche pour le Développement, cleRMonT-feRRanD, fRance;(2) IRD UMR 208 Paloc, IRD-MnHn, PaRIS, fRance;(3) Instituto Geofísico, ePn, QUITo, ecUaDoR;(4) Institut de Recherche pour le Développement, lIMa, PeRU

AbstractBased on archeological and radiometric constraints, previous studies have divided Pre-Columbian times of Ecuador in successive cultural periods: The Paleo-Indian and Pre-ceramic Periods embrace the time from the first Amerindian occupation to about 4000 BP. The Formative Period extends from ca 4000 to ca 300 BC, while the Regional Development (ca 300 BC to 700 AD) and Integration Periods predate the Columbian Period, which starts in AD 1532 in Ecuador. The Formative Cultural Period is poorly known from earlier studies. Here, we bring the first documentation of occupation of Formative age around Tungurahua volcano, 120 km SW of Quito, and we show that local settlements were devastated by an eruption around 1100 cal BC.The past activity of Tungurahua has received attention since its reactivation in 1999. Recent works combining lithostratigraphic, petrologic, and geochronologic analyses reveal that the steep-sloped volcano suffered a major late Holocene flank failure. We show that the debris avalanche results from a major explosive event triggered by massive magma intrusion inside the volcano. Brutal decompression of the magma when flank failure took place resulted in a violent, high-velocity directed blast explosion, which deposited charcoal- and sherd-rich ash layers near the volcano. Our 14 C results range from 2255 ± 30 BP to 5195 ± 45 BP, but most cluster between 2640 ± 45 BP and 3195 ± 45 BP. A calibration analysis indicates that the event took place at ca 1100 cal BC, in the Formative Period. We gathered 38 sherds from three localities. The sherds show a diversity of size, shape, color and ornamentation, and examination of pastes, surface finish, and firing indicates that our material shares many common features from site to site. The material from Tungurahua shows affinities with the Cotocollao tradition, which developed in Quito’s region between 1500 and 500 BC (Villalba, 1988).

i) The use of burnished line and circular punctuates are common in Cotocollao on bowls and jars, notably on those of the first phase Ia, from 1500 to 1300 BC.

ii) One everted rim from a jar is similar to Villalba’s formal class XXVII, which appeared in Quito area in the period Ib, at 1300-1100 BC.

iii) One open recipient, a carinated bowl with circular punctuates exhibits features related to Villalba’s formal class VIII, and aims especially the period IIb, around 800-500 BC.

The material also shares affinities with Machalilla tradition (coastal region of Ecuador), with the occurrence of carinated bowls with punctuate decorations at 1500-1000 BC. In summary, our study reveals that the ca 1100 cal BC Plinian eruption of Tungurahua volcano is among the oldest known volcanic disaster in the Andes.

ReferencesVillalba, M. 1988. Cotocollao: una aldea formativa del valle de Quito, Miscelánea antropológico ecuatoriano, Serie Monográfica 2, Museo del Banco Central del Ecuador, Quito.

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465

S09-P-257

LITTLE SAMBAqUIS AND BIG CHRONOLOGIES: SHELL-MOUND BUILDING AND HUNTER-GATHERERS IN NEOTROPICAL HIGHLANDS.

FIGUTI L.(1), PlenS c.(2), DeblaSIS P.(1)

(1) Universidade de São Paulo, SÃoPaUlo, bRaZIl;(2) UnIfeSP, GUaRUlHoS, bRaZIl

AbstractSambaquis,famous brazilian coastal shellmounds represent a successful archaeological culture, it has a few hundreds sites spread over 2000 km of the Brazilian south-southeast coastline. Those sites have many burial structures, plus a complex mix of faunal remains, charcoal, ashes and sand, resulting in complexes stratigraphic features. Several 14 Csamples exhibits ages from 8,000 y.BP to 1,000 y.BP. In the Brazilian southeast, at the Ribeira de Iguape basin, 40 sites similar to the Sambaquis were found: small mounds composed by a sediment which the major component is land snail shells, followed by animal bones, its industry is represented by lithic and osteodontological artifacs, and more than a few burials. In 2000 just a very few reliable data were available, since then, our archaeological research project has accomplished some excavations, extensive surveys and systematic 14 Csampling. In order to establish the first chronological view of these sites a battery of ages has been obtained from different samples (16 shell, 10 human bones, 6 charcoal) representing 19 sites. These sites show an age range from 10.000 to 1.000 y.Cal BP, pointing out they are contemporary of palaeoindians and older than the coastal shellmounds. The results were very promising, highlighting a 9,000 years of a hunter gatherer cultural continuity. By presenting the 14C distribution associated with the discussion about archaeological assemblages data of these sites, we intend to discuss human dispersion and displacement settlement of early peopling in this portion of Brazil.

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466

SESSION 10

OCEANIC PALAEOCLIMATOLOGY AND PALAEOCEANOGRAPHY

ConvenersN. Frank (FRA), H. Haflidason (NoR), A. Ingalls (USA)

DescriptionThe distribution of 14C both in the ocean and in the atmosphere has fluctuated on decadal to millennial time scales. A better understanding of the behavior, variability, processes and occurrence of 14C in both the present and the past ocean is important for using 14C as an instrument for radiometric dating or as a tracer for reconstructing the past ocean circulation. Over the last decade increasing attention has been drawn to the spatial and temporal variability of marine radiocarbon reservoir ages and their implications for the correction and calibration of marine sediments. The need for new and more accurate estimates of marine radiocarbon reservoir effects and a better understanding of the processes influencing them has been heightened by the increasing number of very high-resolution marine records from various oceanographic regions. Improvements in instrumentation and analytical technique have resulted in an increasing interest in and application of 14C as a circulation tracer. The issues we propose to address in this session include geological- and oceanographic processes related to the exchange of atmospheric radiocarbon with the surface and deep-ocean, application of 14C as a tracer for paleocirculation and the application of 14C in association with trace elements. The session intents to bring together paleoceanographers, oceanographers, atmospheric scientists, physicists and biologists using radiocarbon for a wide range of studies regarding mixing and exchange processes between the atmosphere and ocean and within the ocean.

Keywords14C as a chronometer, 14C tracer of past circulation (more than 1000 yrs), 14C associated with trace elements

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S10-P-258

HOLOCENE CHANGES OF A BRAZILIAN COASTAL ENVIRONMENT: SANTA CATARINA ISLAND

olIVeIRa f.(1), MACARIO K.(1), MaRQUeS a.(1), SIMonaSSI J.c.(2), caRValHo c.R.(1), alVeS e.(1), caRDoZo l.(1), anJoS R.(1), GoMeS P.R.(1), lInaReS R.(1)

(1) Universidade federal fluminense, nITeRoI, bRaZIl;(2) Universidade federal de Santa catarina, floRIanoPolIS, bRaZIl

AbstractIn this work we study a coastal region in the Santa Catarina Island, South of Brazil, with the aim of better understanding environmental processes related to marine productivity and continental erosion. A 51 cm sediment core was collected at 14 meters depth in the Pântano Sul Inlet (27° 51.7” S – 48° 31.6” W) and each 2 cm layer was analyzed. Total organic carbon (TOC), total nitrogen (TN), stable isotopes (δ13C and δ15N), metallic elements and granulometry were evaluated in the core. These parameters were used as proxies to infer about temporal changes in this coastal environment. Fine granulometric fractions account for less than 9% of the core composition. Al, Fe, Mn, Zn and Cu concentrations increase from the base to the surface of the core. Moreover, Zn and Cu present peaks at 20 and 35 cm depth where TOC and TN also increase. The vertical distribution of elements revealed significant changes in the contribution of continental and marine sources along time. For radiocarbon analysis both carbonate and soil organic matter fractions were prepared. Organic matter in the profile ranged from 2.17% to 6.02% and carbonate fraction ranged from 15.54% to 49.23%. Bulk samples were prepared using acid treatment to eliminate the carbonate fraction, and combusted. Individual shells were separated under microscope, etched with hydrochloric acid and hydrolyzed in phosphoric acid. Samples were prepared at the Radiocarbon Laboratory at the Fluminense Federal University (L4C-UFF) in Brazil to be dated by AMS. Graphitization reaction was performed using Zinc and Titanium Hydrate in Pyrex tubes. Measurements are under way in the new 14C AMS facility at UFF (a 250 kV single-stage AMS system) and will be the first radiocarbon AMS study to be performed entirely in Brazil. Moreover, such results will contribute to the understanding of Holocene changes of the Brazilian coastal environment.

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S10-P-259

DATING OF THE BIOGENIC LITTORAL RIMS ON THE ADRIATIC ISLANDS

HORVATINCIC N.(1), faIVRe S.(2), SIRonIc a.(1), baKRan-PeTRIcIolI T.(3), KRaJcaR bRonIc I.(1)

(1) Rudjer boskovic Institute, Zagreb, ZaGReb, cRoaTIa;(2) University of Zagreb, Department of Geography, faculty of Science, ZaGReb, cRoaTIa;(3) University of Zagreb, Department of biology, faculty of Science, ZaGReb, cRoaTIa

AbstractThe biogenic (algal) littoral rims grow at around mean sea-level (MSL) and may be preserved for millennium when growing in rising sea-level environment. In order to reconstruct the relative sea-level change during the Late Holocene, algal littoral rims were collected from three islands in the Adriatic Sea, Croatia. On the particularly exposed sites on rocky coasts of islands Vis, Ravnik and Biševo these littoral rims built by the coralline rhodophyte Lithophyllum byssoidescan be found. The presence of thick and well-developed Lithophyllum rims, considered to be a precise (±10 cm) sea-level indicator, points directly to the rising sea-level environment. Biogenic rims were mapped and sampled for 14C dating during 2008-2010. Two 14C methods, LSC (benzene synthesis) and AMS were used for dating algal samples.14C activity of the calcareous deposit of a recent coralline algae, Vis Island, showed a14C of 103.7 pMC indicating that algae used CO2 from the atmosphere (mean 14C activity of atmospheric CO2 in Zagreb 2010 was 102.0 pMC) and was also close to a14C of recent mollusks from the Adriatic Sea. δ13C values of biogenic rims (2-3 ‰ VPDB) indicated the marine origin, similar values were determined for recent shells and marine biogenic overgrowth on submerged spelothems in the Adriatic Sea (Surić et al, 2005). 14C age of biogenic littoral rims from Vis Island ranged from 260 to 1490 yr BP, from Biševo Island 370 to 1440 yr BP and from Ravnik Island from 510 to 550 yr BP. The age is in concordance with the depth (below MSL) at which the samples of algal rims were taken. If the isostatic-eustatic component is separated, the studied area reveals almost stable tectonic conditions during the past 1500 years. Consequently the phases of sea-level changes seem to be related to the climatic variations during the same time period. The obtained results have been also compared with archaeological markers (Vis Island, Faivre et al, 2010) as well as with geomorphological sea-level markers.

AcknowledgementThis research was supported by the Ministry of Science, Education and Sports of the Republic of Croatia (Projects: 098-0982709-2741, 119-1191309-1305, 119-0362975-1226)

References1. Faivre S, Bakran-Petricioli T, Horvatinčić N. 2010. Relative Sea-Level Change during the Late Holocene on the

Island of Vis (Croatia) - Issa Harbour Archaeological Site. Geodinamica acta 23(5-6): 209-223.2. Surić M, Juračić M, Horvatinčić N, Krajcar Bronić I. 2005. Late Pleistocene - Holocene sea-level rise and the

pattern of coastal karst inundation - records from submerged speleothems along the Eastern Adriatic Coast (Croatia). Marine Geology 214(1-3): 163-175.

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S10-P-261

DETERMINING SURFACE OCEAN CIRCULATION IN THE INDONESIAN THROUGHFLOW USING ∆14C IN CORALLINE SPONGES

ALFORD S., fallon S., KInSleY l.

The australian national University, canbeRRa, aUSTRalIa

AbstractThe Indonesian throughflow is a key component of the global thermohaline circulation, responsible for the mass transfer of waters between the Pacific and Indian Oceans. Here we present results of Δ14C and multiple elemental ratio analyses of coralline sponges, astrosclera willeyana, collected at 10-20 m depth from the Solomon Islands (10°S, 160°E), the Makassar Strait (4°40’S, 118°55’E), the Sulawesi Sea (1°38’N, 124°45’E) and the Banda Sea (5°S, 124°E) to better constrain seasonal-decadal variations in the subsurface flow of waters in this critical region. Independently determined U/Th dates indicate that the analysed sponges are 85-100 years old (Moore et a., 2000). Using Δ14C we will examine water mass movement and mixing in these locations. The long time series available from the sponges allows for an assessment of the variability in this region beyond what is available through direct water measurements. Results are also compared to surface coral Δ14C collected from Bunaken Island and Makassar Strait to further constrain the interpretation of the Δ14C results.

ReferencesMoore, M.D., C.D. Charles, J.L. Rubenstone and R.G. Fairbanks (2000). U/Th-dated sclerosponges from the Indonesian seaway record subsurfacer adjustments to west Pacific winds. Paleoceanography, 15 (4): 404-416.

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S10-P-262

MID- AND LATE HOLOCENE OPEN OCEAN RESERVOIR AGE IN THE NORWEGIAN SEA REFINED USING BOTH A RANGE OF HISTORICAL (THE LAST 1100 YRS) ICELANDIC TEPHRA LAYERS AND THE WELL DATED HEKLA 4 TEPHRA LAYER

HAFLIDASON H.(1), leHMan S.J.(2), SeJRUP H.P.(1)

(1) Department of earth Science, University of bergen, beRGen, noRWaY;(2) Institute of arctic and alpine Research, University of colorado, boUlDeR, UnITeD STaTeS

AbstractThe study and reconstruction of the marine reservoir age has been an important issue in Quaternary and paleoclimate science the last four to five decades. A major effort has been made to radiocarbon date marine shells and whale bones from museum archives, pre-industrially collected along the Norwegian coast and from sites in the Arctic area (Mangerud et al. 2006). Also, recent archeological studies from coastal sites in Ireland and neighboring coastal areas using macro fossils and shells to date the late Holocene marine reservoir age has generally resulted in the same conclusion as found at most Norwegian sites, i.e. a marine reservoir age around 400 yrs with some local variability in the delta R (Ascough et al. 2009). For the first time a high-resolution marine core, located in the E-Norwegian Sea underneath the Norwegian Atlantic current, has been dated with a large number of high precision radiocarbon dates utilizing planktonic foraminifera (Sejrup et al. 2010, 2011). The results of the radiocarbon dating have been used to construct calibrated chronology mainly based on lead and cesium dating in the top, supported by historical tephra layers and through a simple wiggle match with the INTCAL 14C tree-ring for the older record. The results show that for the last 1000 years the delta R for this open ocean site shows delta R values bracketed between 160-190 yrs. This is significantly higher than found at the coastal sites. Similar local delta R deviation of +175 yrs is also determined for the 3826 14C BP dated Hekla 4 regional tephra layer found at the core site. We will present results from the identification of both historical (last 1100 yrs) and some regional late- and mid Holocene tephra layers from Iceland that will contribute to better constraining and independently also refining of the delta R values at this site. The results will also be discussed in terms of other well dated and tephra rich archives from the Norwegian-Greenland Sea region.

References1. Ascough, P.L., Cook, G.T., Dugmore, A.J., 2009. North Atlantic marine 14C reservoir effects: Implications for

late-Holocene chronological studies. Quaternary Geochronology 4(3), 171-180.2. Mangerud, J., Bondevik, S., Gulliksen, S., Hufthammer, A.K., Hoisaeter, T., 2006. Marine C-14 reservoir ages

for 19th century whales and molluscs from the North Atlantic. Quaternary Science Reviews 25, p3228-3245.3. Sejrup, H.P., Lehman, S.J., Haflidason, H., Noone, D., Muscheler, R., Berstad, I.M., Andrews, J.T., 2010.

Response of Norwegian Sea Temperature to Solar Forcing Since 1000 AD. Journal of Geophysical Research 115, C12034, doi:10.1029/2010JC006264

4. Sejrup, H.P., Haflidason, H., Andrews, J.T., 2011. Holocene North Atlantic SSTs and regional climate variability. Quaternary Science Reviews 30, p3181-3195.

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S10-P-263

SIMPLE, RAPID, AND COST EFFECTIVE: AN IMPROVED SCREENING METHOD FOR 14C ANALYSIS OF SMALL CARBONATE SAMPLES

BUSH S., SanToS G., SoUTHon J., XU X.


AbstractPreparation of carbonates for AMS radiocarbon analysis usually involves sample pre-cleaning, hydrolysis with phosphoric acid, and graphitization prior to spectrometer measurement. However, these processes are time consuming and expensive. Here we describe a rapid and relatively inexpensive method of screening a large number of carbonates for their 14C ages with reasonable precision. This method is based on Longworth et al. 20111: pulverized CaCO3 is mixed with Fe powder, and pressed into Al target holders. An optimum beam current of 10% of those produced by ~0.7 mgC graphite targets was obtained for samples of ~0.5 mg of carbonate, and samples as small as 0.3 mg of CaCO3 generate similar beam currents. This method provides similar overall measurement precision to other survey methods2-3. A pooled standard deviation of ±5.1‰ (fm) was estimated based on 19 coral samples ranging in age between 1 ka to 40 ka and analyzed in duplicate. Results on Holocene radiocarbon reference standards have shown that the measured 14C values are consistent with the consensus values within the quoted 1suncertainty. However, results on deglacial standards have sometimes differed from the consensus values by several standard deviations, probably due to the difficulty in establishing a true blank for samples that have not been rigorously cleaned. An average blank (Calcite) of 0.0075 fm (~39,000 Ryr) was achieved. Because of its simplicity, we can process and measure as many as 72 samples in less than 25 hours.

References1. Longworth et al. 2011 Abstract TEC#6, SESSION 3B, AMS12, on March 20-25 of 2011, New Zealand.2. McIntyre et al. 2011 Paleoceanography, 26, PA4212.3. Burke et al. 2010 Deep-Sea Research, 57, 1510-1520 PP.

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S10-P-264

RADIOCARBON RECORD FROM ALOR ISLAND, INDONESIA

BAREšIć J.(1), fallon S.(2), MaZeRaT J.(2)

(1) Ruđer bošković Institute, ZaGReb, cRoaTIa;(2) australian national University, canbeRRa, aUSTRalIa

AbstractTo investigate ocean currents and past climate events affecting the Indonesian throughflow (ITF), a radiocarbon record from a Porties coral from Alor Island, Indonesia, was constructed. Porties are often used in paleoclimate research and water mass circulation studies in Tropics because of their abundance in the region and growth rate of 8 – 20 mm/y. These characteristics allow reconstructions of past environmental changes on weekly to annual time scales. Sampling of coral from Alor has covered approximately 30 years, from 1970 to 2000. An age model was constructed using the sea surface temperatures proxy δ18O. Seasonal variations of a14C are well pronounced (variability from 1 to 4 pMC), and in phase with Langkai and Padang corals (Fallon & Guilderson 2008; Guilderson et al., 2009). El Nino events manifest themselves as lower 14C dips, most likely due to increased upwelling in the Banda Sea area.

AcknowledgmentResearch was supported by the Group of Eight Australian Universities

References1. Fallon, S. J., and T. P. Guilderson (2008), Surface water processes in the Indonesian throughflow as documented

by a highresolution coral Δ14C record, J. Geophys. Res., 113, C09001, doi:10.1029/2008JC004722.2. Guilderson, T. P., S. Fallon, M. D. Moore, D. P. Schrag, and C. D. Charles (2009), Seasonally resolved surface

water Δ14C variability in the Lombok Strait: A coralline perspective, J. Geophys. Res., 114, C07029, doi:10.1029/2008JC004876.

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S10-P-265

RETHINKING RADIOCARBON PRODUCTION TRENDS AND SURFACE OCEAN RESERVOIR AGE VARIABILITY SINCE THE LAST GLACIAL PERIOD: CALIBRATION AND CARBON CYCLE IMPLICATIONS

SKINNER L.

Godwin laboratory for Palaeoclimate Research, University of cambridge, caMbRIDGe, UnITeD KInGDoM

AbstractThe layer-counted chronology for the NGRIP ice-core [Svensson et al., 2008], provides a calendar age-scale for the North Atlantic climatic ‘event stratigraphy’ of the last glacial and deglacial periods that is independent of radiocarbon age constraints. The accuracy of this chronology since ~30kyr BP is attested to by uranium-series dating of speleothems that register the same event stratigraphy [Zhao et al., 2010], as predicted by prevailing climate dynamical theory and numerical model simulations. The NGRIP/speleothem chronology, in combination with the event stratigraphy that it applies to, provides a means of assessing the evolution of past radiocarbon production (e.g. via cosmogenic radionuclides deposited in Greenland ice) and past radiocarbon cycling in the atmosphere-ocean system (e.g. via marine and terrestrial records). Here we update 10Be fluxes that were originally measured in the GRIP and GISP2 ice-cores [Muscheler et al., 2005], based on the new GICC05 NGRIP chronology. We show that taking into account the different accumulation-rate history implied by the GICC05 age-scale for the Greenland ice-cores has a non-negligible impact on 10Be-based trends in past radiocarbon production, in particular across the last deglaciation, with possible implications for the inference of ocean-atmosphere radiocarbon disequilibrium during deglaciation. Indeed, by placing radiocarbon-dated marine records from the Iberian Margin and the Cariaco Basin [Hughen et al., 2006] on the same speleothem/GICC05 calendar age-scale, it can be shown that large reservoir ages appear to have prevailed across the North Atlantic during the last glacial period, and that large and coherent fluctuations in these reservoir ages may have occurred during Heinrich Stadial 1 in particular. If confirmed, these observations would carry major implications for the evolution of the overturning circulation and the carbon cycle across the last deglaciation, as well as our ability to calibrate marine radiocarbon dates during this critical time period in the history of climate and culture.

References1. Hughen, K., et al. (2006), Cariaco Basin 14C calibration and activity record over the past 50,000 years updated

from the Cariaco Basin, Quat. Sci. Rev., 25, 3216-3227.2. Muscheler, R., et al. (2005), Geomagnetic field intensity during the last 60,000 years based on 10Be and 36Cl

from the Summit ice cores and 14C, Quat. Sci. Rev., 24, 1846-1860.3. Svensson, A., et al. (2008), A 60,000 year Greenland stratigraphic ice core chronology, clim. Past, 4, 47-57.4. Zhao, K., et al. (2010), High-resolution stalagmite d18O records of Asian monsoon changes in central and

southern China spanning the MIS 3/2 transition, earth Planet. Sci. lett., 298, 191-198.

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S10-P-266

AGE DIFFERENCES BETWEEN ANORGANIC AND ORGANIC FRACTIONS IN PERUVIAN MARGIN DEEP-SEA SEDIMENTS

DReVeS a.(1), MOLLIER-VOGEL E.(1), bÖScHen T.(2), ScHneIDeR R.R.(1)

(1) University of Kiel, KIel, GeRManY;(2) GeoMaR, KIel, GeRManY

AbstractFor Last Glacial to Holocene deep-sea sediments, core chronologies are generally established by radiocarbon dating of foraminiferal calcite. Yet, sediment cores from high productive upwelling areas characterized by strong oxygen minimum conditions do not provide sufficient amounts of foraminiferal calcite for detailed radiocarbon dating of even laminated sediments. The alternative, dating the organic fraction in the marine sediments, is ambiguous by varying contributions from terrigenous and marine organic matter to the sea floor. As the ages of terrigenous organic matter can be significantly different than that of the marine fraction, due to varying climate-related erosion and transport pathways bringing in older terrigenous material, it is important to identify the age differences between marine calcite and marine and terrigenous organic matter in a given setting. We applied the acid-alkaline-acid procedure to the bulk sediment, resulting in a humin and a humic acid fraction in comparison to the foraminiferal calcite at various depths to check for their differences in age. It turned out that the organic fractions date about 800 to 3,000 years older than the calcitic foraminifera at the same depth horizons. Especially, the humin fraction is remarkably older than the foraminiferal calcite, while most ages of the humic acid fraction reveal ages in between those two. Age differences between foraminiferal calcite and the humin fraction can probably be explained by input of old terrestrial refractory organic matter. The age differences between the humin and humic acid fractions may be interpreted as varying contributions of more ore less soluble terrestrial material or even labile organic matter from marine sources, the latter the most likely possibility in the upwelling zone off Peru. Although the age difference between the calcite and humic acid fraction is not completely understood, it may reflect upwelling of subsurface water containing older carbon dioxide taken up by phytoplankton. This could also explain previous findings that radiocarbon ages of alkenones originating from phytoplankton tend to be significantly older than those of foraminifera in coastal upwelling areas.

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S10-P-267

RECONSTRUCTING THE VERTICAL 14C GRADIENT OF THE BAJA MARGIN DURING THE LAST DEGLACIATION

LINDSAY C.(1), leHMan S.(1), MaRcHITTo T.(1), oRTIZ J.(2), Van Geen a.(3)

(1) University of colorado, boUlDeR, co, UnITeD STaTeS;(2) Kent State University, KenT, oH, UnITeD STaTeS;(3) columbia University, PalISaDeS, nY, UnITeD STaTeS

AbstractThe radiocarbon activity (Δ14C) of the atmosphere decreased in two steps during the last deglaciation, coinciding with the well-known Heinrich 1 (H1) and Younger Dryas (YD) stadials. A leading explanation for these periods of decline involves the release of 14C-depleted carbon from a deep, isolated ocean reservoir, while another involves an input of geologic carbon (Stott & Timmerman, 2011, Geophys. Monogr. Ser.,) both of which could also help explain the deglacial rise in atmospheric CO2. Reconstructions of intermediate water Δ14C near Baja California, Mexico (Marchitto et al., 2007 Science) and in the Arabian Sea (Bryan et al., 2010 Earth Planet. Sci. Lett.) document two intervals of extreme depletion relative to the coeval atmosphere during H1 and the YD that are interpreted as evidence of the return of aged carbon from a deep reservoir to the upper ocean and atmosphere. Here we report on 14C measurements in cores from the Baja California margin that expand the depth range of our observations and enable reconstruction of the vertical Δ14C gradient. Calendar ages were determined by (1) correlation of diffuse spectral reflectance (DSR, a proxy related to local productivity) with the layer-counted age model in the GISP2 ice core and (2) correlation of raw planktic G. ruber 14C ages to new measurements in core PC08 previously studied by Marchitto et al. (2007). Together these provide a common and consistent calendar age model for margin cores PCO8 (depth 705 m), PC10 (430 m) and GC38 (1270 m).In preliminary results, PC08 G. ruber 14C is depleted relative to the contemporary atmosphere during H1 and YD, consistent with upward mixing of the intermediate-depth signal measured in PC08 benthics. GC38 benthic Δ14C closely resembles the nearby, shallower PC08 benthic record during the depleted H1 interval and subsequent recovery, as well as a record of Δ14C from 820 m in the Arabian Sea (Bryan et al., 2010 Earth Planet. Sci. Lett.) GC38 benthic Δ14C diverges from the PC08 record after about 13.6 ka and does not record the extremely depleted values seen in the PC08 benthic data during the late Bølling-Allerød and YD.We interpret these results as evidence for two pulses of 14C-depleted carbon during H1 and YD, the first reaching at least 1270 meters and the second confined to shallower depths, with an intervening period of vertical mixing and re-equilibration. The similarity to the Arabian Sea record during H1, and the restriction to intermediate waters during YD, suggest that the aged carbon was advected laterally to Baja (and the Arabian Sea) from a common source and not vertically from a more local deep source. We speculate that the shift to a more depth-restricted signal reflects a change in the density of 14C-depleted intermediate waters relative to the stratification of the Baja water column.

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S10-P-268

NW PACIFIC MID-DEPTH VENTILATION CHANGES DURING THE HOLOCENE

UCHIDA M., Rella S.

national Institute for environmental Studies, TSUKUba, JaPan

AbstractDuring the last 50 years the oxygen content of North Pacific Intermediate Water primarily originating in the Okhotsk Sea has declined suggesting decreased mid-depth water circulation and possible decrease of CO2 drawdown. It is therefore of high interest to elucidate the climate-oceanic interconnections of the present interglacial period (Holocene), in order to predict possible future climate change that is associated with changes in mid-depth ventilation. However, such efforts have been hampered so far by the lack of appropriate sediment cores with fast sedimentation rates during the Holocene. Core CK05-04 that was recovered in 2005 from off Shimokita peninsula, Japan, at ~1000 m depth shows sedimentation rates of ~80 cm/kyr during the Holocene and therefore presents an ideal opportunity to reconstruct for the first time the Holocene ventilation history of the NW Pacific Ocean. We employ Accelerator Mass Spectroscopy (NIES-TERRA, Tsukuba) radiocarbon analysis of co-existing benthic and planktonic foraminifera to conclude on the ventilation age of the mid-depth water using benthic-planktonic radiocarbon age differences. At the conference we would like to present the results.

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S10-P-269

CHRONO-STRATIGRAPHIES FROM MULTIPLE CORES FROM A SEISMICALLY ACTIVE MUD LENS OFF PERU INDICATE HORIZONTAL EXTENSIONS OF LAMINAE, MISSING SEqUENCES, AND A NEED FOR MULTIPLE CORES FOR HIGH RESOLUTION RECORDS

SALVATTECI R.(1), fIelD D.(2), GUTIeRReZ D.(3), SIfeDDIne a.(4), baUMGaRTneR T.(5), feRReIRa V.(5), VelaZco f.(3), ReYSS J.l.(6), caQUIneaU S.(1), oRTlIeb l.(1)

(1) IRD - france nord, bonDY, fRance;(2) college of natural Sciences, Hawaii Pacific University, HaWaII, UnITeD STaTeS;(3) IMaRPe, callao, PeRU;(4) Departamento de Geoquimica Uff, nITeRoI, bRaZIl;(5) cIceSe, enSenaDa, MeXIco;(6) laboratoire des Sciences de climat et de l’environnement, GIf SUR IVeTTe, fRance

AbstractMarine laminated sediments that accumulate over time in suboxic areas of the ocean floor are an excellent archive to study past climate variability at high temporal resolution. While the existence of discontinuities produced by natural events such as strong bottom currents, bioturbation or lateral depositions are acknowledged, particularly for long records, the extent of their influence on high-resolution sequences has not been carefully examined. In the present work we show widespread evidence for stratigraphic discontinuities from multiple gravity and box-cores retrieved off Pisco (Peru). Chronostratigraphies are largely based on cross-correlation of distinct sedimentary structures (determined by x-ray image analysis). The visual cross-correlations were validated using 210-Pb, 241-Am, and 14-C profiles, as well as proxy records. The 14C dates from bulk organic matter helped to constrain the chronologies to some degree but showed considerable uncertainty for developing a reliable chronological model of high resolution. The cross-correlation of distinct stratigraphic layers clearly shows that some sedimentary sequences are continuous across scales of tens of kilometers, indicating that regional processes often determine laminae formation. However, there are often notable absences of laminated sequences in some cores that are present in other cores. The lack of some laminae may frequently be due to erosion caused by a slump, but erosion by bottom currents, spatial variability in diatom blooms among other factors may account for the differences among core sites. Despite the losses of sedimentary structures a continuous composite record of the last several centuries was assembled from spliced sequences of different cores. This composite record provides a well constrained temporal framework to develop further high resolution proxies in this region of high productivity. However, proxy records developed from single cores will be subject to both temporal gaps and instantaneous deposits. Thus, the results of the present work indicate major problems associated with high resolution reconstructions (e.g. former El Niño events) off Peru that did not take into consideration the sedimentary disturbances.

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S10-P-270

RADIOCARBON VARIABILITY IN NORTHEAST ATLANTIC INTERMEDIATE WATERS

TISNÉRAT-LABORDE N.(1), DoUVIlle e.(1), GonZaleS-RoUbaUD c.(1), SabaTIeR P.(2), MonTaGna P.(1)(3), MonTeRo-SeRRano J.c.(1), fRanK n.(1), Hall-SPenceR J.(4)

(1) laboratoire des Sciences du climat et de l’environnement/IPSl, cea-cnRS-UVSQ, GIf-SUR-YVeTTe, fRance;(2) laboratoire eDYTeM, UMR 5204, cISM, Université de Savoie, le boURGeT DU lac, fRance;(3) Istituto di Scienze Marine, cnR, boloGna, ITalY;(4) Marine biology and ecology Research center, Scholl of Marine Science and engineering, University of Plymouth, PlYMoUTH, UnITeD KInGDoM

AbstractThe radiocarbon content of northeastern Atlantic upper intermediate water is intimately linked to cross thermocline exchange and advection of water masses along the basin scale re-circulation pathways. These water masses result mainly from a mixing of the subpolar and subtropical Atlantic intermediate water masses. Here, we present two 60 years long records of upper intermediate water 14C, one from the Norwegian Sea and one from the Bay of Biscay in order to investigate cross thermocline exchange in these two distinct oceanic regions and changes in the Atlantic mid depth gyre circulations during the last 60 years.Three quasi-annual radiocarbon time series were obtained from 14C measurements of two different species of deep-sea corals, i.e. Madrepora oculata and a lophelia pertusa. The two selected specimens were collected alive at Rost Reef in Norwegian Sea (NwS; 67°N, 9°E) at 350 m of depth in 2007. One deep-sea coral of the species M. oculata were recovered in the Bay of Biscay. The age of Norwegian Sea M. oculata has been estimated to 39 ± 2 years based on 210Pb and radiocarbon dating (Sabatier et al, 2011). The ages of the Norwegian Sea l. pertusia and the M. oculata from the Bay of Biscay have been measured by means of U/Th dating and are estimated to 60 years.The two records cover the pre-bomb and post-bomb period. Before 1963, they reveal a moderate variability of 14C values with a mean value of -52 ± 7‰ and -57 ± 10‰ for NwS and Bay of Biscay, respectively. Then, bomb 14C produced by atmospheric testing of thermonuclear weapons in the 1950s and early 1960s is recorded by all corals at synchronous timing but at variable amplitude. In the records, bomb 14C began to increase around 1963. Both post-bomb 14C records from the NwS are nicely synchronous and reach peak values of +45‰ in the mid-1980s. Thereafter 14C level remains nearly constant with overprinted secular variations of less than 10‰. In contrast, much lower Δ14C values are observed in Bay of Biscay coral. Post-bomb Δ14C values of solely +5‰ were reached in 1985 indicating either a much reduced exchange of water across the thermocline or a more significant advection of 14C depleted mid-depth subtropical gyre water. In addition to the overall trends important secular 14C variations are observed in the Bay of Biscay and NwS, which are most likely reflecting changes in contributions of the subpolar and subtropical Atlantic mid-depth water masses or potentially the Mediterranean outflow water.

ReferencesP. Sabatier0 J.L. Reyss, J.M. Hall-Spencer, C. Colin, N. Frank, N. Tisnérat-Laborde, L. Bordier, E. Douville (2011) 210Pb-226Ra chronology reveals rapid growth rate of Madrepora oculata and lophelia pertusa on world’s largest cold-water coral reef. Biogeosciences Discuss., 8, 12247-12283.

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SESSION 11

CONTINENTAL PALAEOCLIMATOLOGY AND PALAEOHYDROLOGY

ConvenersD. Genty (FRA), L.C.R Pessenda (BRA), H. Wang (USA)

DescriptionThis session addresses multiple issues related to time series for continental palaeoclimatic records and palaeohydrological responses. It focuses on precisely dated continental records that shed light on climatic variability on all continents and its impact on hydrology and vegetation changes. Palaeoclimatic reconstructions from continental carbonates (speleo-thems, travertine, gastropods, ostracods, soils carbonates, calcified roots, etc.), from continental and coastal organic matter (peat, sediment, soil, vegetation, etc.) are welcome. Besides climatic reconstruction, processes involving carbon isotopes (12C, 13C, 14C) and bio indicators (pollen, diatoms, sponge spicules, phytolits, etc.) in above organic archives are welcome.

Keywordsdating, paleoclimatic series, continental carbonates, speleothem, travertine, gastropod, ostracods, calcified roots, rhizoliths, organic matter, soil, vegetation, (paleo) climate, (paleo) hydrology

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S11-P-271

STABLE ISOTOPES FROM RHIZOLITHS PRESERVED IN LAST GLACIAL LOESS RECORDS: ABRUPT CLIMATIC AND HYDROLOGICAL CHANGES IN THE MIDWESTERN USA

WANG H.(1), coUnTS R.(2), WanInGeR S.(2)

(1) Prairie Research Institute, University of Illinois at Urbana-champaign, USa, cHaMPaIGn, UnITeD STaTeS;(2) Kentucky Geological Survey, KY 42420, HenDeRSon, UnITeD STaTeS

AbstractRhizoliths in loess-paleosol successions in the central United States are calcified and encrusted plant roots. Their stable isotopic compositions are sensitive to climate and hydrological changes. In this study, rhizoliths were collected in 5 and 10 cm increments from loess profiles at four locations in the midcontinental USA, two in the Ohio River Valley and two in the Mississippi River Valley. They provided information about paleoclimate and ecosystem changes during transitions from the last glacial maximum to last termination and to Holocene near Laurentide ice margins. Age models using 14C dating on low molecular weight soil organic carbon compounds and rhizolith carbonate carbon along with optically stimulated luminescence (OSL) dating on fine sand indicated that these records covered a time span from 25 to 11 cal. ka BP (before present). Through regional comparisons, these δ13C and δ18O time series suggest that moisture conditions in the Midwest were inversely phased with those in the southwestern USA, which is further confirmed by archived geological records over vast areas of North America. Moreover, regional changes of climate and ecosystems were found in phase with the Greenland ice record since the Bølling/Allerød interstadial, but not in phase during the Heinrich event 1 (H1) interval. Our results suggest that the atmos-pheric circulation over North America responded to hemispheric temperature changes more rapidly than North AtlanticOcean circulation during H1 interval. It also suggests that when deglaciation began, the moisture distribution in North America was controlled by the polar jet stream and rain belt migration, and no longer controlled by the geometry of the Laurentide ice sheet. Together with other proxies, the δ13C and δ18O values of rhizoliths provide insights for studying the evolution of atmospheric circulation associated with the bipolar seesaw hypothesis since the last termination over the North American continent.

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S11-P-272

14C MEASUREMENTS OF ICE SAMPLES FROM “JUVFONNE ICE TUNNEL”, NORWAY – A VALIDATION OF A RADIOCARBON DATING TECHNIqUE FOR GLACIER ICE

ZAPF A.(1)(2), neSJe a.(3), SZIDaT S.(2)(4), WacKeR l.(5), ScHWIKoWSKI M.(1)(2)(4)

(1) Paul Scherrer Institut, VIllIGen PSI, SWITZeRlanD;(2) oeschger centre for climate change Research, beRn, SWITZeRlanD;(3) University of bergen, Department of earth Science and the bjerknes centre for climate Research, beRGen, noRWaY; (4) University of bern, Department of chemistry and biochemistry, beRn, SWITZeRlanD; 5) eTH Zürich, laboratory of Ion beam Physics, ZÜRIcH, SWITZeRlanD

AbstractIn palaeoclimatological investigations of ice cores from high-alpine glaciers dating is a non-trivial task mainly due to the complex impacts of glacier flow, accumulation, ablation etc. resulting in a strongly non-linear depth-age relationship. Particularly in the deepest parts of ice cores, where thinning of the annual layers normally does not allow for conventional dating, other techniques are needed to establish a precise age-depth relationship. A radiocarbon method for dating ice core samples has been developed, utilizing carbonaceous aerosol particles embedded in the ice matrix. Method validation has previously been carried out by comparing ages derived from annual layer counting or volcanic reference horizons with the measured radiocarbon ages (Sigl et al., 2009). Here we present a further validation by for the first time comparing 14C ages determined from carbonaceous particles in glacier ice with 14C ages conventionally obtained from organic remains found in the ice. Two of the analyzed samples (JUV-1 and JUV-2) were collected from an ice tunnel in the inner part of the Juvfonne ice patch in the Jotunheimen Mountains in southern Norway (61.676°N, 8.354°E), whereas one sample (JUV-3) was collected from young ice at the margin of the same ice patch. Several organic rich ice layers have been identified and previously radiocarbon dated by our Norwegian collaborators, yielding ages ranging from 963-1007 yr BP to 3078-3207 yr BP (Nesje et al., 2011). These results were then used as reference values for the validation process of the novel radiocarbon dating technique mentioned above. For that purpose, clear ice samples adjacent to the already dated reference layers were retrieved and analyzed. Based on the ages of the organic detritus layers (Nesje et al., 2011), and their locations with respect to the set of ice samples to be tested with our method, an age range could be estimated. Multiple measurements were performed for each of the three sampling locations. With the exception of one identified outlier, the obtained results could reproduce the expected ages very well. Calibrated 14C ages from one of the sampling locations show a slight scatter that might be due to a complex unconformity in the deeper layers of the ice patch reported elsewhere (Nesje et al., 2011). However, results for all three ice samples are very reasonable with respect to the age estimates given. Thus, a further line of evidence for our method to provide the true age of the ice could be established.

References1. Nesje A, Pilø LH, Finstad E, Solli B, Wangen V, Ødegård RS, Isaksen K, Støren EN, Bakke DI, Andreassen LM:

The climatic significance of artefacts related to prehistoric reindeer hunting exposed at melting ice patches in southern Norway, The Holocene DOI: 10.1177/0959683611425552 (2011).

2. Sigl M, Jenk TM, Kellerhals T, Szidat S, Gäggeler HW, Wacker L, Synal HA, Boutron C, Barbante C, Gabrieli J, Schwikowski M: Towards radiocarbon dating of ice cores, J. Glaciol., 55, 194 (2009).

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S11-P-273

PHYSICAL CHRONOLOGY (14C AND TL), PALEOCLIMATOLOGY AND ARCHAEOLOGY APPLIED TO THE “DECODING” OF A SCENARIO OF ADAPTATION OF ANCIENT CENTRAL SAHARA POPULATIONS TO CLIMATIC CRISIS WHICH HAVE TAKEN PLACE DURING THE LAST TEN MILLENNIUMS (HOLOCENE)

SCHVOERER M.(1), JUnGneR H.(2), aUMaSSIP G.(3), neY c.(4), GUIbeRT P.(4), ollaGnIeR c.(1), MaSSUÉ J.P.(5)

(1) Université de bordeaux 3, bÈGleS, fRance;(2) Helsinki University, HelSInKI, fInlanD;(3) association des amis du Tassili, alGIeRS, alGeRIa;(4) Université de bordeaux 3, PeSSac, fRance;(5) association européenne «Sciences et Patrimoine (PacT), bÈGleS, fRance

AbstractHow the ancient holocene populations of central Sahara reacted when the climate became slowly more and more cold and arid then, rather fast warm and humid?The results acquired at the end of recent researches in paleoclimatology, prehistoric archaeology (which rock art) and physical chronology (14C and Thermoluminescence), allows to offer an answer to the question that was asked.In central Sahara (Tassili-n-Ajjer, Algeria), a scientifically excavated site (Tin-Hanakaten), which exceptional stratigraphy gave rise to several results notably in sedimentary studies and around fourty dates, on one hand with radiocarbon (14C) on plant rests and on the other hand with Thermoluminescence (TL) on ceramics fragments.

They highlight:

- When climate becomes progressively more cold and arid, during an evolution which lasts about 1 300 years, the scarcity of fresh water and vegetation compels men and herds to migrate to regions of Sahara, where remains enough water and humidity, particularly thanks to the porous texture of sandstone of the geological setting.

- When, rather fast (in a few decades it seems), climate becomes distinctly hotter and more humid, vegetation is of course favored once again. Then, analysis shows that some groups migrate the other way round while others, numerous, stay in the zones of altitude, roughly between 1 200 and 1 800 meters, avoiding so – partly at least - flies and mosquitoes, parts of the health problems which affects particularly animals – trypanosomiasis - and human beings – malaria -.

A new question is consequently asked: is this type of adaptation can be transposable in the next decades of the XXIth century?

KeywordsPhysical Chronology – 14C – Thermoluminescence – Climatic Change – Archaeology – Paleoclimatology - Human Adaptation – Central Sahara – Holocene.

* Program « Desert Patina », supported by the European Commission (DG Research) Contract INCO CT FP6 2004-2008 509100 and by the Regional council of Aquitaine (CCRRDT, 2004-2008).

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S11-P-274

DATING RECENT PEAT ACCUMULATION IN EUROPEAN OMBOTHROPHIC BOGS

VAN DER PLICHT J.(1), bRaIn S.(2), cHaMbeRS f.(2), Van Geel b.(3), Van DeR lInDen M.(3), neWbeRRY J.(2), ToMS P.(2), Yeloff D.(3)

(1) University of Groningen, GRonInGen, neTHeRlanDS;(2) University of Gloucestershire, GloUcHeSTeR, UnITeD KInGDoM;(3) University of amsterdam, aMSTeRDaM, neTHeRlanDS

AbstractThis study compares age estimates of recent peat deposits in ten European ombrotrophic bogs produced using the 14C bomb peak, 210Pb, 137Cs, spheroidal carbonaceous particles (SCPs) and pollen. At three sites, the results of the different dating methods agree well. In five cores, there is a clear discrepancy between the 14C bomb peak and 210Pb age estimates. In the upper layers of the profiles, the age estimates of 14C and 210Pb are in agreement. However, with increasing depth, the difference between the age estimates appears to become progressively greater. The evidence from the sites featured in the study suggests the 14C bomb peak is a reliable dating method, and is not significantly affected by the incorporation of old carbon with low 14C content originating from sources including air pollution deposition or methane produced by vegetation decomposition. 210Pb age estimates that are too old may be explained by the enrichment of 210Pb activity in the surface layers of peat resulting from a hypothesised mechanism where rapidly infilling hollows, rich in binding sites, may scavenge 210Pb associated with dissolved organic matter passing through the hollow, as part of the surface drainage network. Until further research identifies and resolves the cause of the inaccuracy in 210Pb dating, age estimates of peat samples based only on 210Pb should be used with caution.

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S11-P-276

GEOCHRONOLOGY, OCCURRENCE OF THE ANCIENT TIMBERS FOUND IN SOUTH CHINA AND ITS IMPLICATIONS FOR PALEOCLIMATE

DING X.(1), SHen c.(2), YI W.(2), DInG P.(2), WanG n.(3), fU D.(1), lIU K.(1)

(1) State Key laboratory of nuclear physics and Technology, Peking University, beIJInG, cHIna;(2) Guangzhou Institute of Geochemistry,chinese academy of Sciences, GUanGZHoU, cHIna;(3) Department of earth Science, Hongkong University, HonGKonG, cHIna

AbstractAncient timbers provide continuous high resolution records for reconstruction of the paleoclimate. According to the AMS 14C data of collected samples, ancient timbers found in South China range from 18700 a B.P. to 500 a B.P., and apparently centralize in several time segments. The first time segment ranges from 18700 a BP to 16400 a BP, several timbers are found lying in the clay of the first terrace of Beijiang River, which is considered to be an important evidence for the existence of Wurm subinterglaciation in South China. The second time segment ranges from 13200 a B.P. to 12600 a B.P., two ldesia polycarpa timbers which commonly seen in temperate area now are found in Moyang River located in Yangchun city, revealing a colder environment with the temperature 3Сto 7Сlower than today. The third time segment ranges from 8300 aB.P. to 6700 a B.P., typically represented by the Sea Bottom Forest in Shenhu Bay’s south coast, Fujian. The Sea Bottom Forest is dominated by Keteleeria and a few of Masson Pine, indicating a cold to warm climate transition during that time. The fourth time segment ranges from 5400 a B.P. to 3300 a B.P. Cellulose from cinnamomum timbers at 5410±100a B.P. shows a more positive δ13C values by 1.7‰ to 3.0‰ than that at present, suggesting warmer climate than today. Ancient forests dominated by Glyptostrobus Pensilis are found in large area in Pearl River Delta during this time segment.Glyptostrobus Pensilis timbers are upright with only stumps or lie in the humic layer. Three or more development stages of ancient forests implicate that the climate fluctuates at millennia and centennial scale. The last time segment ranges from 2200 a B.P. to 1100 a B.P.. Timbers found during this period are generally pinaceae at river bed or low-lying depression, reflecting a relative cold and flooding climate.

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S11-P-277

PALEOCLIMATIC CHANGES IN CARAJáS (PA)

CONCEIÇÃO M.(1), coRDeIRo R.(1), RoDRIGUeS R.(2), SIfeDDIne a.(3), TURcQ b.(3), Seoane J.c.(4), baRboSa M.(4)

(1) Universidade federal fluminense, nITeRÓI, bRaZIl;(2) eMbRaPa agrosilvopastoral, SInoP, MaTo GRoSSo, bRaZIl;(3) Institut de Recherche pour Développement (IRD-lMTG-HYbaM), bonDY, fRance;(4) Universidade federal do Rio de Janeiro, RIo De JaneIRo, bRaZIl

AbstractThe future of global climate becomes of paramount importance to determine the variations of climate over the evolution of the planet. Given that the Amazon region is currently holding the world’s greatest biodiversity, paleoclimate and paleoecological studies in this region are of fundamental importance for the development of policies to mitigate and adapt against global climate change. The objective of this study is to identify the occurrence of paleoenvironmental changes during the Holocene and Pleistocene, through the determination of organic and inorganic parameters and deposition of indicators of burning (charcoal particles). The core has 450 cm and was sliced every two inches, and it was made size analysis, mineralogical, isotopic (δ13C and δ15N) and C / N, microscopic quantification of coal, mercury, dating 14C by AMS and the determination of density and water content of the core. According to data from the core, we can affirm the occurrence of fires in the Serra dos Carajás in the last 26,420 years. Through the interpretation of the results we can determine the occurrence of five distinct phases in the core. The characteristics of Phase I (26,420 cal years BP) as the presence of kaolinite, quartz, silica and gibbsite, low values in the concentration of carbon particles may be indicative of a possible phase more humid, with occurrence of few events of local fire. The occurrence of a phase in the wettest period between 30,000 and 22,000 years BP, by increasing the deposition of clastic material as a result of erosion of the basin during the transition from a humid and dry.Phase II is characterized by increased occurrence of fires more regional events(increased concentration of carbon particles and decreasing particle size), the increase of TOC towards the top of the core, the presence of the minerals gibbsite, quartz, kaolinite and siderite. This increase in the values of TOC, may have been caused by, increased concentration of carbon particles in this phase. Phase III is characterized by a decrease in the occurrence of fires (decrease the concentration of carbon particles), the presence of gibbsite, quartz, kaolinite and siderite, δ13C values become more negative. Phase IV is characterized by an increase of more regional forest fires, the presence of gibbsite, kaolinite and quartz, δ13C values become more positive toward earlier stage. Trend of increased organic matter toward the top of the core. The fifth and final stage (6,650 cal years BP) is characterized by a decrease in the frequency of incendiary, presence of gibbsite, quartz, kaolinite and silica, a large increase in the amount of organic matter. These features are indicative of a possible return of wetter conditions, with low occurrence of fires.

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S11-P-278

THE HOLOCENE ONSET ON THE DJAVAKHETI HIGHLANDS (LESSER CAUCASUS): CHRONOLOGY AND PALAEOENVIRONMENT

MESSAGER E.(1), belMecHeRI S.(2), Von GRafenSTeIn U.(3), noMaDe S.(3), DUMoUlIn J.P.(4), ollIVIeR V.(5), VoIncHeT P.(6), PUaUD S.(6), coURTIn-noMaDe a.(7), GUIlloU H.(3), MGelaDZe a.(8), MaZUY a.(1), loRDKIPanIDZe D.(8)

(1) UMR 7264 cePaM cnRS/Univ nice Sophia antipolis, nIce, fRance;(2) Department of Meteorology Pennsylvania State University, UnIVeRSITY PaRK, Pa 16802, UnITeD STaTeS;(3) UMR 8212 lSce/IPSl, cea-cnRS-UVSQ, GIf SUR YVeTTe, fRance;(4) UMS 2572, laboratoire de Mesure du carbone 14., GIf SUR YVeTTe, fRance;(5) UMR 7192 cnRS collège de france, PaRIS, fRance;(6) UMR 7194 du cnRS Muséum national d’Histoire naturelle, PaRIS, fRance;(7) Université de limoges, GReSe, lIMoGeS, fRance;(8) Georgian national Museum, TbIlISI, GeoRGIa

AbstractIn western Eurasia, the transition from the Late-Glacial to the Holocene represents a key period for the vegetation history. This phase is generally well-characterized by a forest expansion favoured by a rapid warming of the climate.In the Lesser Caucasus highlands, this transition is not easy to identify on the base of the palaeoenvironmental records because of the three following factors:

1. The late glacial ice-retreat on the Djavakheti highlands has affected the timing and chronology of the palaeoecological processes.

2. The exceptional proximity of the glacial tree refugia (located in Colchis Plain, western part of Transcaucasia) generated a singular forest dynamic.

3. The oscillations of glacier systems caused major shifts in lakes sedimentation and therefore in Age-depth model of lake records.

Consequently, the palaeoecological signal recorded in lake sediments is complex to decipher.In the Djavakheti highlands, two lakes were cored respectively in 2009 and 2011: Paravani Lake (2073 m a.s.l, 41°27’N 43°48’E) and Tabatskuri palaeolake (2058 m a.s.l., 41°40’ N 43°40’E). The two sequences cover the chronological interval between 13-8 ka, and were investigated for a multi-proxy analysis including more than 20 radiocarbon dates to improve the age-depth model. The pollen data revealing the environmental changes in both basins will be combined with the new chronologies to characterize the peculiar Holocene onset in this part of Transcaucasia.

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S11-P-279

EVIDENCE FOR EARLY HUMAN PRESENCE AT HIGH ALTITUDES IN THE ÖTZTAL ALPS

KUTSCHERA W.(1), PaTZelT G.(2), WIlD e.M.(1), JeTTMaR b.(1), KofleR W.(2), lIPPeRT a.(1), oeGGl K.(2), PaK e.(1), PRIlleR a.(1), STeIeR P.(1), WaHlMÜlleR-oeGGl n.(2), ZaneSco a.(3)

(1) University of Vienna, VIenna, aUSTRIa;(2) University of Innsbruck, InnSbRUcK, aUSTRIa;(3) burg Hasegg, Hall In TIRol, aUSTRIa

AbstractThe accidental discovery of a frozen human body in 1991 at a glaciated mountain pass located at the north-south water devide of the Central European Alps near the Austrian-Italian border sparked great excitement among archaeologists and the public. Radiocarbon dating revealed that a male human, who was quickly nicknamed “Ötzi” (he was found in the Ötztal Alps), had been locked up in a rocky ice-filled ditch at an altitude of 3210 m a.s.l. for about 5200 years. The well-preserved body is now kept in a room providing glacial conditions in the South Tyrol Museum of Archaeology [1] in Bolzano, Italy. This allows one to perform unprecedented research on a human who had lived in an Alpine environment in the last part of the Neolithic period [2].

In an attempt to trace early human presence in this region on more general grounds, 147 samples (mainly charcoal and peat) were collected along the Ötztal valley to the north, with a few samples collected also south of the Alpine water divide. Radiocarbon dates of these samples from altitudes between 1500 and 2500 m a.s.l. indicate human presence in these high regions of the Alps during the Holocene. Already in the early Neolithic period in the Alps, i.e. since the middle of the 5th millennium B.C., mountain pasturing seem to have evolved at altitudes where natural pastures were found. This suggests that early human activity was concentrated at higher altitudes, which at the time were probably more favourable than the bottom of the valleys where flooding and other hazards existed. It is possible that these early users came from south of the water divide spreading into the northern regions particularly during the summer season.

We also present 88 radiocarbon measurements on equipment and artefacts associated with the Iceman, and on a variety of plant and animal specimens collected at his discovery site. The latter were investigated with the hope to get a hint on the climatic conditions in the Alps 5000 years ago. It was expected that plant life at the great altitude of the Iceman site is very sensitive to climate (temperature) changes. During the lifetime of the Iceman temperatures of the summer months may have been even warmer than today.

Implications of both the Iceman site findings and the other sites along the Ötztal valley on early human activities in this Alpine environment will be discussed.

References[1] Iceman web page at the South Tyrol Museum of Archaeology (http://www.iceman.it/).[2] M. Patalini, The Iceman defrosted, nature 471 (2011) 34.

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S11-P-280

A WET PERIOD AROUND 8.2 ka AS REGISTERED IN TWO BELGIAN SPELEOTHEMS

VERHEYDEN S.(1), KePPenS e.(2), Van STRYDoncK M.(3), QUInIf Y.(4)

(1) Royal belgian Institute of natural sciences, bRUSSelS, belGIUM;(2) Vrije Universiteit brussel, bRUSSelS, belGIUM;(3) Royal Institute for cultural Heritage, bRUSSelS, belGIUM;(4) University of Mons, bRUSSelS, belGIUM

AbstractIntroductionThe coldest Holocene event recorded in Greenland ice cores happened 8200 years ago, lasted approximately 300 years as suggested by changes in δ18O (Alley et al., 1997) and decreased N Atlantic temperatures of up to 7.4°C. The cold event seems to be the consequence of the sudden rupture of an ice dam of the northern American ice-cap releasing important amounts of cold fresh waters in the North-Atlantic ocean (Barber et al., 1999). In Europe, this event decreased the air temperatures of between ~0.5 and ~2°C (Alley and Agustsdottir, 2005) Despite several indications of a possible synchronous cold event around 8.2ka in NW-European terrestrial proxies (Daley et al., 2011), there are strong indications for a longer lasting cold episode (Stager and Mayewski, 1997, Daley et al., 2011). It remains difficult to relate the changes with certainty to the 8.2kyr BP cold event due to a lack of high resolution chronology.Speleothems provide high-resolution proxy tools for paleoclimate reconstruction (Wang et al., 2001; Genty et al., 2003). They can be precisely dated with U-series methods and, provided that a dead-carbon correction is applied, with 14C dating. Several speleothems exhibit a clear anomaly around 8.2ka, while others show a longer lasting anomaly or no significant changes (see Spötl et al., 2010).

A wet period registered in two Belgian stalagmitesTwo Holocene low-Mg calcite stalagmites from the Hotton cave and the Père Noël cave located in southern Belgium, show a sedimentological particularity around 8.2 ka. The U-series dated Père Noël stalagmite presents a particularly dense grey compact calcite between 8.6ka and 8.2ka. The Hotton stalagmite, was 14C-dated. A correction for 12% dead carbon is estimated from former studies (Genty et al., 1999). U-series dating will refine this dead carbon correction. The stalagmite presents a deposition hiatus of ca 1100 years between extrapolated ages of 8700 cal yr Before 2000 AD (B2k) and 7600 cal yr B2k. The hiatus is clearly visible through the presence of a thin clay layer and is the consequence of a flooding period.Combined petrographic, stable isotopic (δ18O and δ13C) and chemical (Mg/Ca and Sr/Ca) analyses give indications for the climatic conditions around 8.2 ka. The stalagmites suggest the occurrence of a wet phase between ca 8.9 and 8.2 ka. Progressive drying is observed until 7.9 ka with a return to fully temperate interglacial conditions at 7.6 ka.

Relation with the 8.2 ka cold eventRegarding the early start of the climate deterioration and its total duration of 1100 years, it is impossible to link the observed wet phase in the Belgian speleothems as directly related to the so-called 8.2 ka event. Moreover, the successive flooding periods recorded in the Hotton stalagmite suggests that the climate deterioration registered in the Belgian stalagmites around 8.2 ka may be one among other deteriorations occurring during the early Holocene.

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S11-P-281

A PALEO-ESTUARY EVOLUTION AT SOUTHEASTERN BRAZIL, DURING HOLOCENE SEA-LEVEL FLUCTUATIONS

BUSO A.A.(1), PeSSenDa l.c.R.(1), De olIVeIRa P.e.(2), VolKMeR-RIbeIRo c.(3), boRoTTI fIlHo M.a.(1), coHen M.c.l.(4), SIQUeIRa G.(5), fRancISQUInI M.I.(1), PaSSaRInI JUnIoR J.R.(1)

(1) c14 laboratory (cena/USP), PIRacIcaba, bRaZIl;(2) São francisco University, bRaGanÇa PaUlISTa, bRaZIl;(3) Zoobotanical foundation of Rio Grande do Sul, PoRTo aleGRe, bRaZIl;(4) laboratory of coastal Dynamics (laDIc/UfPa), belÉM, bRaZIl;(5) Vale nature Reserve, lInHaReS, bRaZIl

AbstractA two meters sediment core revealed the onset and evolution of a paleo-estuary resulted from post-glacial sea-level fluctuations. The core was collected in a freshwater lake placed 23 km from ocean shoreline, at Barra Seca River incised Valley, SE Brazil (19°02.584’S/39°56.695’W). From 7700 to 7100 cal yr BP high influx of mangrove pollen (600 to 1,100 grains per cm² per year) and forest pollen (400 to 750 grains per cm² per year), depleted δ13C, δ15N and high C/N ratios (δ13C ≈ -28‰; δ15N ≈ +2‰; C/N > 30), and fine sand and mud sediment, has been interpreted as a bay-head delta surrounded by mangrove and tropical forest vegetation. The onset of the paleo-estuary at this time may be the result of post-glacial sea-level rise, considering the relative sea-level curves for southeastern Brazil which propose that the present mean sea-level was exceeded at ca. 7800 to 6600 cal yr BP. From 7100 to 2500 cal yr BP the tendency to more enriched δ13C and δ15N and lower C/N ratios (δ13C ≈ -26‰; δ15N ≈ +5‰; C/N ≈ 13 at 2800 cal yr BP), reduced influx of mangrove pollen (11 to 450 grains per cm2 per year), abundance of siliceous spicules from marine Porifera, and silty sediment, suggest higher input of marine organic matter and lower sedimentation energy. This has been interpreted as landward migration of the paleo-estuary and establishment of the central basin of this estuary at the site. Mangrove vegetation followed the displacement of the bay-head delta. The migration of the paleo-estuary may be result of the sea-level fluctuations recorded in the southeastern Brazil. From 2500 cal yr BP to the present, more depleted δ13C and δ15N and higher C/N (δ13C < -27‰; δ15N ≈ +2‰; C/N ≈ 20), higher influx of herbs, aquatic and forest pollen, absence of mangrove pollen, and high percentages of freshwater siliceous sponge spicules, are interpreted as the seaward migration of the paleo-estuary and establishment of modern lake at ca. 1200 cal yr BP. This migration may be the result of relative sea-level fall at southeastern Brazilian coast, as proposed by sea-level curves. Pollen influxes were more suitable (than pollen percentages or concentrations) for the interpretation of mangrove migration in response to sea-level fluctuations and paleo-estuary dynamics.

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S11-P-282

RADIOCARBON DETERMINATION OF PAST GROWTH RATES OF LIVING ACACIA TORTILIS TREES FROM TWO ARID SITES IN EASTERN SAHARA

GOSLAR T.(1)(2), anDeRSen G.(3), KRZYWInSKI K.(4), cZeRnIK J.(2)

(1) adam Mickiewicz University, PoZnan, PolanD;(2) Poznan Radiocarbon laboratory, PoZnan, PolanD;(3) Uni Research aS, beRGen, noRWaY;(4) University of bergen, beRGen, noRWaY

AbstractIn this study we present 14C dates of wood cores, taken from the trunks of Acacia tortilis trees, living in Gebeit (Red Sea State, Sudan), and in Wadi Nuqrus (Eastern Desert, Egypt). From each site, 5 trees were cored, and from these cores (ca. 150-350mm long) altogether 78 samples were forwarded for 14C dating. 14C measurements, performed on alfa-cellulose extracted from wood, revealed post-bomb 14C concentrations in the outer parts of the tree trunks, and for the inner parts, gave almost all 14C dates from the range of the wiggly part of the 14C calibration curve between 1680-1950 AD. Based on sets of 14C dates, calendar chronologies of individual cores were then constructed, using the algorithm of free-shape age-depth modelling (Goslar et al. 2009). These chronologies indicate on differences in growth rates of individual trees (ca. 50-200mm/100yr ), correlating well with differences in sapwood thickness of the tree-trunks.

References Goslar T., van der Knaap W.O., van Leeuwen J., Kamenik Ch. 2009. Free-shape 14C age-depth modelling of an intensively dated modern peat profile, Journal of Quaternary Science, 24, 481-499.

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S11-P-283

INFLUENCE OF PREHISTORIC MEN ACTIVITY ON FACIES OF HOLOCENE TUFA – AN EXAMPLE FROM SOUTHERN POLAND

GRADZINSKI M.(1), HeRcMan H.(2), STWoRZeWIcZ e.(3), SlUSaRZ M.(1), STacHoWIcZ-RYbKa R.(4)

(1) Institute of Geological Sciences, Jagiellonian University, KRaKoW, PolanD;(2) Institute of Geological Sciences, PaS, WaRSZaWa, PolanD;(3) Institute of Systematic and evolution of animals, PaS, KRaKoW, PolanD;(4) Wladyslaw Szafer Institute of botany, PaS, KRaKoW, PolanD

AbstractHolocene tufas are relatively widespread in the Kraków Upland (southern Poland). They fill lowermost parts of narrow valleys entrenched into Jurassic or Palaeozoic carbonate rocks (Pazdur et al., 1988). Tufas comprise barrage and detrital facies; the latter fill the interbarrage ponded areas.The complex of tufas, the thickness of which reaches 5 m, was studied in the lowermost segment of Sąspowska Valley (Ojców National Park). Five tufa barrages have been recognized. They are built of stromatolitic and moss tufa accompanied by oncoidal and phytoclastic onocidal tufa. The detrital facies comprising intraclast and microdetrital tufa formed the filling of the interbarrage ponded areas. The facies is mixed and intertwined with siliciclastic deposits, such as clay, sand and loess as well as peat lenses. This facies was laid down in calm condition within dammed segments of fluvial system.The comparison of tufas from Sąspowska Valley with isochronous tufas from other valleys was possible due to radiocarbon dating. It shows that the main difference between the studied tufas and other Holocene tufas in the Kraków Upland is the amount of non-carbonate fraction in detrital tufa facies. The amount of fraction in question in detrital facies of the studied tufas is locally up to ~60% whereas in other Holocene tufas of the Kraków Upland detrital facies are composed mainly of carbonate fraction. The non-carbonate fraction in fluviatile tufas originated due to erosion of soils and older sediments up the catchment. The main alimentation areas are valley slopes and karst plateaus covered with Pleistocene loess-type deposits. The erosion was possible due to deforestation. It seems very probable that in Sąspowska Valley catchment deforestation started as early as in mid-Holocene, that is earlier than in neighbouring areas, and was connected with exploitation of flints in mid-Holocene time (Lech, 2006). The study was supported by the Ministry of Science and Higher Education grant N° N307 151538.

References1. Lech, J., 2006. The early and middle Neolithic in the Ojców Jura. In: Lech, J. & Partyka, J. (eds), The ojców Jura

in Prehistory and beginnings of the Polish State. Ojcowski Park Narodowy, Ojców, pp. 387-438.2. Pazdur, A., Pazdur, M. F., Starkel, L. & Szulc, J., 1988. Stable isotopes of Holocene calcareous tufa in southern

Poland as palaeoclimatic indicators. Quaternary Research, 30: 177-189.

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RADIOCARBON WIGGLE-MATCHING OF THE HARUNA FUTATSUDAKE PUMICE (HR-FP), CENTRAL JAPAN

OKUNO M.(1), oIKaWa T.(2), GeSHI n.(2), HoSHIno Y.(3), YaTSUZUKa S.(1), naKaMURa T.(4)

(1) fukuoka University, fUKUoKa, JaPan;(2) aIST, Geological Survey of Japan,, TSUKUba, JaPan;(3) botanical Garden, Tohoku University, SenDaI, JaPan;(4) center for chronological Research, nagoya University, naGoYa, JaPan

AbstractThe Haruna volcano, which is located in the central part of Japan, erupted twice in the 6th century (Arai, 1962). The first eruption that occurred in the early part of the century produced a tephra sequence named as the Haruna Futatsudake Ash (Hr-FA). The Haruna Futatsudake Pumice (Hr-FP) is a product of the second eruption that occurred in the middle of the century. Both tephras provide chronological framework to archaeological sites in the Kofun period, which have no historical records of eruptions in Japan. However, the eruptive ages were determined by pottery chronology (Sakaguchi, 1993). Recently, Nakamura et al. (2008) obtained calendar age of cal AD 485 to 504 (2 sigma) for the Hr-FA eruption, using 14C wiggle-matching of three wood trunks.In order to determine the precise age of the Hr-FP eruption by a HVEE Tandetron AMS system at Nagoya University (Nakamura et al., 2000), we sampled five charcoal fragments from a trunk within a pyroclastic flow deposit on the eastern flank of the volcano (Fig. 1: 36º 30’ 30.7”N, 138º 54’ 44.4”E). We obtained a calendar age of cal AD 436 to 450 (2 sigma) for the eruption by 14C wiggle-matching with computer program Calib 5.0 (Stuiver and Reimer, 1993). This result is not consistent with previous chronological studies.Sakaguchi et al. (1982) estimated a time interval between the two eruptions to be 30 years from accumulation rate of peat in Ozegahara (70 km NE from the volcano). The analyzed wood (25.5 cm in diameter) has 29 annual rings and is consistent with the previous estimates. The 14C content of Japanese cedars (Sakamoto et al., 2003) are also compared. Using the Hr-FA age (cal AD 485 to 504) and time interval (30 yrs), the obtained data set has to be moved to 80 years younger than original plotting. This vertical gap may be caused not only by local effect but also by volcanic CO2 emission effect.

References1. Arai, F. (1962) Science Report of Gunma University, 10, 1-79.2. Nakamura, T. et al. (2000) nIMb, 172, 52-57.3. Nakamura, T. et al. (2008) Tree-ring Research, 63, 37-46.4. Sakaguchi, H. (1993) Tephra-archaeology, 151-172.5. Sakaguchi, Y. et al. (1982) ozegahara, 1-29.6. Stuiver, M. and Reimer, J. P. (1993) Radiocarbon, 35, 215-230.7. Sakamoto, M. et al. (2003) Radiocarbon, 45, 81-89.

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S11-P-285

RADIOCARBON CHRONOLOGY OF PALEOENVIRONMENTAL CHANGES OF THE KASHIBARU MARSH, NORTHERN KYUSHU, SW JAPAN

OKUNO M.(1), fUJIKI T.(2), naKaMURa T.(3), MoRI Y.(4), UeDa K.(5), aIZaWa J.(1), KonoMaTSU M.(6), naGaoKa S.(7)

(1) fukuoka University, fUKUoKa, JaPan;(2) International Research center fo Japanese Studies, KYoTo, JaPan;(3) center for chronological Research, nagoya University, naGoYa, JaPan;(4) Kinjo Gakuin University, naGaoYa, JaPan; (5) aichi prefectual Meiwa High School, naGoYa, JaPan;(6) Wakayama University, WaKaYaMa, JaPan;(7) nagasaki University, naGaSaKI, JaPan

AbstractThe Kashibaru Marsh (591 m a.s.l.) is located on the western part of the Sefuri Mountains in northern Kyushu, SW Japan. The mountains consist of Cretaceous plutonic rock with roof pendant of Sangun metamorphic rock (Karakida et al., 1992). In order to reconstruct paleoenvironment of this mountainous area, we collected core samples down to the bottom of the marsh in December 2004. The core samples measure 86 mm in diameter. We performed AMS radiocarbon dating, physical properties measurements and pollen analysis for reconstruction of paleoenvironmental changes in the marsh. The marsh was utilized as rice field around 1200 cal AD with an estimated average sedimentation rate of 4.1 mm/yr. Human cultivation was abandoned by covering of medium to coarse sand layer at 1400 cal AD, and left untouched by any human activity. This result is consistent with insect and diatom assemblages in previous reported core (KS0304) (Okuno et al., 2011).

References1. Karakida, Y. et al. eds. (1992) Regional Geology of Japan, 9 Kyushu,Kyoritsu Shuppan Co., Ltd., 1992, 371p

(in Japanese).2. Okuno, M. et al. (2011) in natural Science on archaeology, Shin-Jinbutsuoraisha Co., Ltd., 79-98 (in Japanese).

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S11-P-286

MYSTERY OF ANCIENT BURIED WOOD IN THE ARNHEIM “SWAMP”, UPPER PENINSULA MICHIGAN, USA

PANYUSHKINA I.(1), leaVITT S.(1), ScHMIeReR J.(2), WIeDenHoefT a.(3)

(1) University of arizona, TUcSon, UnITeD STaTeS;(2) Michigan Technological University, HoUGHTon, MIcHIGan, UnITeD STaTeS;(3) USDa forest Products laboratory, MaDISon, WISconSIn, UnITeD STaTeS

AbstractDuring excavation on a private farm to provide sand for local road construction in 2007, a “jumble” of wood (logs and stumps, some 40 cm in diameter with bark remaining) was discovered ca. 4-5 meters below the surface. The location of this site is ca 100 km northwest of sand plains fringing the southern margin of Lake Superior, which have yielded in situ buried stumps of ca. 10,000 14C BP spruce trees at the Gribben Basin (Lowell et al., 1999), and initial suspicions were that the wood might likewise be of early Holocene age. Fortunately, when the site was open over a dozen logs were collected and preserved, allowing us to identify the wood, to obtain radiocarbon dates, and to conduct dendrochronological analysis.

In contrast to Gribben Basin, no spruce was present at the Arnheim Swamp site, but the majority of samples were hardwoods Ulmus sp. (elm) and betula sp. (birch) with two logs of Thuja (possibly northern whitecedar). Radiocarbon ages ranged from 1408±35 to 1582±36 BP (ca. 408 to 668 A.D), clearly much younger than the Gribben Basin trees. However, in spite of the relatively “young” age, crossdating of ring widths of Arnheim samples provided a floating chronology with potential to match with regional chronologies for absolute dating. Relatively few chronologies in eastern North America extend that far back, but fortuitously we were able to find an exactly dated tree-ring chronology extending back over 2780 years from ancient Thuja occidentalis on an island on Lake Huron.This dating has allowed us to speculate about this wood deposit with respect to the AD 540 global event (Baillie, 2001) and possible origins.

We thank Brendan Buckley, Douglas Larson, Ze’ev Gedalof, and Peter Kelly for providing the Flowerpot Island Thuja occidentalis tree-ring chronology. This work is supported by NSF grant #P2C2-1003483.Author e-mail: [email protected]

References1. Baillie, M.G.L., 2001. The AD 540 event. Current Archaeology 15:266–269.2. Buckley, B.M, R.J.S. Wilson, P.E. Kelly, D.W. Larson and E.R. Cook, 2004. Inferred summer precipitation for

southern Ontario back to AD 610, as reconstructed from rings widths of Thuja occidentalis. Can. J. For. Res. 34:2541-2553.

3. Lowell, T.V., G.J. Larson, J.D. Hughes, G.H. Denton, 1999. Age verification of the Lake Gribben forest bed and the Younger Dryas advance of the Laurentide Ice Sheet. Canadian Journal of Earth Sciences 36(3):383–393.

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S11-P-288

THE RATE OF ACCUMULATION PROCESSES BASED ON DIFFERENT RESEARCH METHODS (A CASE STUDY FROM BRUDZEń REGION, CENTRAL POLAND)

SZWARCZEWSKI P.(1), SMolSKa e.(1), MaZeIKa J.(2)

(1) University of Warsaw, WaRSaW, PolanD;(2) nature Research centre, VIlnIUS, lITHUanIa

AbstractThe palaeogeographic studies carried out in the Skrwa river valley near Brudzen (Masovian Lowland, Central Poland) were focused on the relationship between the human activity, climate change and the sedimentological/geochemical differentiations of the sediments filling the river valley bottom. The area of the study is located in gap part of river valley, next to the steep slopes of glacial plateaus, in the vicinity of settlements developing intensively since the early Middle Ages. The two strongholds of Brudzen Duzy (archaeologically dated for 8th, 10-11th century) and Parzen (archaeologically dated for 12th century) are located at a distance not greater than one kilometer in a straight line from the place where the detailed geological and geomorphological maping were carried out. The region was also affected by human activity during the Neolithic, Bronze Age and Roman times. Authors have recognized palaeochannel, gullies, alluvial fans and a few buried soil horizons. There have been taken sediment samples for interdisciplinary analyzes such as grain size, geochemical or radiocarbon dating. Available archaeological and historical data were studied. The Roman times and medieval land use change (deforestation) and agriculture development resulted in intensification of soil erosion. It is visible both in the facial changes and in geochemical properties of the sediments (increase in the trace elements and especially phosphorus content). The formation of deluvial/colluvial sediments (reaching up to 3 m thick) started in this region nearly 2,000 years ago (1,830-1,620 cal BP, 1,710-1,510 cal BP) and was accelerated during last 800 years (800-690 cal BP, 800-670 cal BP). Geochemical changes of the sediments in this vertical profile allow to assess the intensity of accumulation in the Skrwa valley bottom from 0,1-0,2 mm/year in the Neolith, some 0,5 mm/year in the Roman period, 1-2 mm/year in the early medieval period and even more than 4 mm/year from the industrial revolution. This abstract presents the results of research conducted under a grant from the Ministry of Science and Higher Education N° N305 322135 (2008-2011).

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S11-P-289

RECORDS OF THE MESO– AND NEOHOLOCENE PALEO-ENVIRONMENTAL CHANGES IN WIERCHOMLA LANDSLIDE PEAT BOG (BESKID SąDECKI MTS, POLISH OUTER CARPATHIANS)

MICHCZYNSKI A.(1), MaRGIeleWSKI W.(2), KolacZeK P.(3), MIcHcZYnSKa D.J.(1), obIDoWIcZ a.(4)

(1) Institute of Physics, Silesian University of Technology, GlIWIce, PolanD;(2) Institute of nature conservation, Polish academy of Sciences, KRaKoW, PolanD;(3) faculty of Geographical and Geological Science, adam Mickiewicz University, PoZnan, PolanD;(4) W. Szafer Institute of botany, Polish academy of Sciences, KRaKoW, PolanD

AbstractThe Wierchomla landslide is situated in the eastern part of the Beskid Sądecki Mts., Polish Outer Carpathians. At the foot of landslides’ head scarp, the depression (ca 60 m long and 50 m wide) was formed. This depression, whose maximum depth is ca 4.2 m, is filled with organic-minerogenic deposits of fen type peat bog (minerogenic mire). A few cores were taken from the peat bog using INSTORF sampler (Russian peat sampler). The longest core was studied using loss on ignition analysis of deposits, pollen analysis, lithological analysis and radiocarbon dating. An age-depth model constructed basing on radiocarbon dates allows to establish absolute time scale for the reconstruction of local and regional palaeo-environmental changes. Radiocarbon dating as well as pollen analysis indicate that the landslide came into existence and the beginning of peat accumulation took place at the Atlantic Phase. An interesting fact is that the beginning of spruce (Picea) expansion revealed in the Wierchomla site (GdA-2500: 7010±30 14C BP) started about approx. 1500 years earlier in comparison to the Jesionowa site (GdC-325: 5595±55 14C BP), which is also located in the Beskid Sądecki Mts. (Margielewski et al. 2011). This fact shed new light on the postglacial migration of spruce in the Western Carpathians and indicates that even relatively small mountain systems reflect patterns of nonsynchronous expansion of arboreal taxa.

ReferencesMargielewski W., P. Kołaczek, A. Michczyński, A. Obidowicz, A. Pazdur. 2011. Record of the meso-and neoholocene palaeoenvironmental changes in the Jesionowa landslide peat bog (Beskid Sądecki MTS. Polish Outer Carpathians). Geochronometria 38 (2): 138-154.

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S11-P-291

SELECTED EXAMPLES OF NATURAL AND ANTHROPOGENIC ENVIRON-MENTAL CHANGES IN THE POLISH-LITHUANIAN BORDER IN THE LATE GLACIAL AND HOLOCENE PERIODS

SZWARCZEWSKI P.(1), MaZeIKa J.(2)

(1) University of Warsaw, WaRSaW, PolanD; (2) nature Research centre, VIlnIUS, lITHUanIa

AbstractThe vicinity of present Polish-Lithuanian border is characterized by a distinctly different history of economic development than areas in the central and southern Poland. For quite a long time there dominates the gatherer and hunting economy. The agriculture begins to grow in this region more than 3,000 years later than in the fertile loess plateaus.The study was focused on the analysis of deposits infilling depressions with no outflow and modern sedimentation in lake bottoms. There have been used interdisciplinary methods in the research such as geological mapping, drilling and samples collection with the use of different augers (e.g. piston or hummer type). The collected material was subjected to various physical and chemical analyzes such as loss on ignition, calcium carbonate content and concentrations of selected trace elements. Age of shifts in sedimentation was determined using the radiocarbon dating. The palynological data shows that organic sediments infilling studied depressions represent a complete succession from the end of the last glaciation up to the present day. In the Holocene evolution of the research area, there have been distinguished three main development phases:

1) lacustrine,

2) peat-bog accumulation, and

3) deluvia-colluvia accumulation phase.

The first two were mainly conditioned by the climate changes while the last one is a result of the increasing antropopression. Their ages are:

(1) from 10,600–11,000 14C yr BP to some 4,500-7,000 14C yr BP,

(2) from 4,500-7,000 14C yr BP to 600-1,500 14C yr BP and

(3) from present day to 1,500-600 14C yr BP, respectively.

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S11-P-292

HIGH-RESOLUTION TERRESTRIAL MIS3 ENVIRONMENT FROM TREES RECOVERED FROM LANDSLIDE DEPOSITS IN OREGON, USA

JULL A.J.T.(1), PanYUSHKIna I.P.(1), Van De WaTeR P.(2), leaVITT S.W.(1), SQUIRe J.(3), TeSTa n.(3), WIeDenHoefT a.J.(4), aRMSTRonG a.l.(1), DIaZ-GoMeZ c.I.(1), leonaRD a.G.(1)

(1) University of arizona, TUcSon, aZ, UnITeD STaTeS;(2) california State University, fReSno, ca, UnITeD STaTeS;(3) oregon Department of Transportation, coRVallIS, oR, UnITeD STaTeS;(4) US Department of agriculture, MaDISon, WI, UnITeD STaTeS

AbstractMarine Isotope Stage 3 (MIS3, ca. 60 to 27 ka) was generally cold but interrupted by brief Dansgaard-Oeschger warm excursions. Exploration of terrestrial inter-annual environmental variability within this period by tree rings has been lacking, because only a few occurrences of wood of this age have been reported from Chile and New Zealand. Ancient landslide deposits in Oregon have fortuitously preserved MIS3 wood recently excavated during a highway realignment project in the Oregon Coast Range. Preservation of the wood material and associated macro- and microfossils in organic deposits was facilitated by their entombment by clay sediments. We examined cross-sections of twelve large logs (0.5-1.5 m diameter), which show excellent preservation and in most cases included pith and sapwood. Anatomical examination shows that the wood is exclusively Douglas-fir (Pseudotsuga menziesii (Mirb.) Franco), which currently grows along the Pacific coast from central British Columbia to central California. All specimens were crossdated and overlapped into a 297-year tree-ring width chronology, with no missing rings and a few very narrow pointer-years. The tree-ring width pattern contains several 3-year periods of growth reduction and concentration of resin duct formation in the earlywood. The tree-ring width series are highly variable with first-order autocorrelation up to 0.8 and mean sensitivity of 0.23. Initial radiocarbon dating estimates ages >53ka, but refined radiocarbon analysis will be conducted to establish an absolute age. The ancient trees may come from a moisture-stressed environment, similar to that reported for modern Douglas-fir from the Canadian Cordillera and interior ranges of U.S. Rocky Mountains. Interestingly, the spatial pattern of modern tree-ring widths is consistent with the western dipole of moisture anomaly driven by El Niño.

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S11-P-293

PARIZSKE MOCIARE MIRE: DATING OF HUMAN IMPACT IN VEGETATION CHANGE

JAMRICHOVA E.(1), HaJnaloVa M.(2), baRTa P.(3)

(1) Institute of botany, czech academy of Sciences, bRno, cZecH RePUblIc;(2) Department of archaeology, constantine the Philosopher University, nITRa, SloVaKIa;(3) Department of archaeology, comenius University, bRaTISlaVa, SloVaKIa

AbstractThe poster presents research of mire Parizske mociare, a protected national reserve in SW Slovakia, and its implication on the settlement history of this old loess habitation zone. Five metres deep profile has been investigated by palynology and radiocarbon dating and the results were compared with macroclimate model and known settlement data for the region.According to the pollen spectra and 14C data on plant macro-remains, the mire developed from the early Holocene to mid 4th millennium when sedimentation stopped. From the changes in pollen profile and regional archaeological data, settlement history has been reconstructed. The time span of sedimentation enabled to identify also settlement periods, which have not been attested in archaeological record (Mesolithic).The pollen record has further been used to test the relevance of palaeoclimate model for early and mid Holocene in the region. Bayesian modeling (OxCal) is used to investigate the following:

1) sedimentation rate within undisturbed sequences of pollen profile,

2) identification of outliers or confirmation of redeposition event,

3) absolute dating of periods of regional anthropogenic impacts demonstrated in pollen.

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S11-P-294

LITTLE ICE AGE DRYNESS IN NORTHEAST BRAZIL RECORDED BY LACUSTRINE SEDIMENTS OF LAKE BOqUEIRãO EXPLAINS DISCREPANCIES BETWEEN 14C AND 210Pb MEASUREMENTS

TURCQ B.(1), ZocaTellI R.(2), coSTa R.l.(3), coRDeIRo R.c.(3), albUQUeRQUe a.l.S.(3), ManDenG-YoGo M.(1)

(1) IRD, bonDY, fRance;(2) ISTo, oRleanS, fRance;(3) GeoQUIMIca-Uff, nITeRoI, bRaZIl

AbstractLake Boqueirão is located at 5°S latitude, on the Brazilian Atlantic coast, a region where the climate is directly influenced by the Intertropical Convergence Zone (ITCZ) displacements.Two cores were collected at different water depths based on a seismic survey. 210Pb were measured in the top 20 cm and 14C all along the profiles. The two methods indicated very different results concerning ages and sedimentation rates of the sediment.Lake level changes has been reconstructed using granulometry, Total Organic Carbon, C/N, 13C, 15N and Rock Eval (Hydrogen Index (HI), Oxygen Index (OI)). These proxies indicate large variations of the lake levels during the last 3000 cal yrs BP. Moreover, a prolonged dryness occurred in Lake Boqueirão since 570 cal yrs BP, till the last decades. This event provoked a drying of the lake at the two sampling sites. This drying can explains why the 210Pb method did not work in this lake probably due to an enrichment phenomenon of bare surfaces called « meteoric cap ».This dry phase corresponds to the Little Ice Age characterized by a cooler North Atlantic Ocean. These data indicate that the teleconnection pattern between tropical Atlantic, ENSO and Northeast Brazil rainfalls has changed in the past 3000 years.

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VEGETATION CHANGE IN CENTRAL CAMEROON DURING THE LATE HOLOCENE ENVIRONMENTAL CRISIS (3000 YRS B.P.)

MANDENG-YOGO M.(1), DeSJaRDInS T.(2), TURcQ b.(1), nGUeTnKaM J.P.(3), acHoUnDonG G.(4), leZIne a.M.(5)

(1) IRD/locean, bonDY, fRance;(2) IRD/bIoeMco, bonDY, fRance;(3) Université de ngaoundéré, faculté des Sciences, Département des Sciences de la Terre., nGaoUnDeRe, caMeRoon; (4) Herbier national du cameroun, YaoUnDe, caMeRoon;(5) locean (UPMc/cnRS/IRD/MnHn), PaRIS, fRance

AbstractA major environmental crisis occured during the Late Holocene in equatorial Africa (3000 yrs B.P.) (Lezine, 2007). This crisis modified the geographic distribution of ecosystems which led to a destruction and fragmentation of the rainforest. Human populations were also impacted especially the central Cameroon pygmies who lived solely in forest areas (Verdu et al., 2009). As a consequence, they were probably separated and isolated in different forest fragments. Originally, our objective was to study what were the ecosystems like, in these areas, before the crisis .We made a sampling mission in Central Cameroon in november 2010. We collected 22 soil profiles from different types of vegetation. Representative samples have been collected from Abong Mbang, west of Yaoundé (3°50’N 13°20’E), to the Northern forest remnant at Ngambé Tikar (5°40’N, 11°30’E).Fortunately we manage to get some profiles of almost 4meters deep, which exceeded the time span of our original purpose and reach a maximum of 7000 yrs B.P. at the bottom of the profiles. So we used Radiocarbon techniques and 13C analyses to reconstruct the changes in paleoclimate and vegetation types in the continental interiors where Pigmy populations are living.This method had already been used to trace the savannah-forest boundary fluctuations in Congo (Schwartz et al., 1992) and for very recent changes in Cameroon (Guillet et al., 2000.

References1. LezineA.-M. 2007. Postglacial Pollen Records of Africa. In Encyclopaedia of Quaternary Sciences, Scott A Elias

ed., Elsevier. Vol.4, 2682-2698.2. Guillet, B., Achoundong, G., Youta Happi, J., Kamgang Kabeyene Beyala, V., Bonvallot, J., Riera, B., Mariotti,

A., Schwartz, D . 2001. Agreement between floristic and soil organic carbon isotope (I3C/12C, 14C) indicators of forest invasion of savannas during the last century in Cameroon. Journal of Tropical Ecology, 17:809-832.

3. Schwartz, D., Mariotti, A., Trouve, C.; Klaas Van Den B., Guillet, B., 1992. Étude des profils isotopiques 13C et 14C d’un sol ferrallitique sableux du littoral congolais. Implications sur ladynamique de la matière organique et l’histoire de la végétation. C. R. Acad. Sci. Paris, t. 315, Série II, p. 1411-1417.

4. Verdu P., Austerlitz F., Estoup A., Vitalis R., Georges M., Théry S., Froment A., Le Bomin S., Gessain A., Hombert J.-M. et al., 2009. Origins and genetic diversity of pygmy hunter-gatherers from Western Central Africa. Current Biology 19, 4:312-318

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S11-P-296

THE WIGGLE MATCHING METHOD AT DATING OF HOLOCENE HUMID PHASES IN THE POLISH CARPATHIANS (PEATBOG PUśCIZNA WIELKA)

KRAPIEC M.(1), SZYcHoWSKa-KRaPIec e.(2)

(1) aGH University of Science and Technology, KRaKoW, PolanD;(2) aGH?University of Science and Technology, KRaKoW, PolanD

Abstract

The high peatbog Puścizna Wielka (near Nowy Targ, S Poland) is one of the largest in the Carpathians, as well as the only one, in which the peat is still exploited economically. This allows for access to unique research materials in form of trunks of subfossil trees occurring in the peat bog in distinct levels. The peatbog sediments record two stages of its development; the low peatbog stage, developed on a mineral background, and the high peatbog, in form of a dome. Advancing of trees and bushes into the bog area, and occasional peatbog fires, marked as charcoal levels, are connected with drying climate. On the other hand, increasing humidity resulted in recession of trees from high peats and their mass felling.Dendrochronological analysis has been hitherto made for over 200 samples of subfossil wood of pine (Pinus sylvestris L.) representing trees reaching individual ages up to 200-250 years. Correlation of dendrochronological sequences resulted in construction of three floating chronologies of respective lengths: 200 years (2NTT_A1), 250 years (2NTT_B1), and 330 years (2NTT_C1). For the absolute dating, 10 samples, each encompassing five subsequent tree-rings, were taken from each chronology for radiocarbon analyses. The wiggle matching method, applied with the program Ocal v 4.1, allowed to date the floating chronologies: 2NTT_A1 to ca. 970-770 cal BC, 2NTT_B1 to ca. 2500-2300 cal BC, and 2NTT_C1 to 3230-2900 cal BC. Also the beginnings of humid periods (at first marked with decreasing tree-ring widths and subsequent dying and felling the trees in the peatbog) were recognized and dated, with relatively high accuracy, to ca. 870-770 cal BC, 2370-2300 cal BC, and 2950-2900 cal BC.

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SESSION 12

INSIGHTS INTO THE OCEAN CARBON CYCLE FROM RADIOCARBON MEASUREMENTS

ConvenersE. Druffel (USA), A. mcNichol (USA) , K. Tedesco (UNESCo), N. Tisnérat-Laborde (FRA)

DescriptionRadiocarbon measurements on carbon isolated from all of the reservoirs in the ocean-from bulk pools such as dissolved inorganic (DIC) and dissolved organic (DOC) carbon to individual biomarkers isolated from complex matrices-adds important time and source information to studies of the carbon cycle in the natural environment. The addition of radiocarbon measurements to carbon cycle studies brings critical information for understanding and quantifying the impact of human activity and climate change on the environment. Sensitive environments such as coastal and high latitude regions have complex carbon cycle processes with organic matter inputs from a variety of sources and ages-direct input from primary production, modern and pre-aged terrestrial matter, as well as ancient material. The combination of bulk and compound specific measurements can help sort out the history of carbon deposition in these environments and permit us to make insightful predictions for the future. In the open ocean, tracing the bomb pulse in specific compounds can help to understand the synthesis, degradation and reactivity of complex materials such as DOC. We invite contributions describing studies using radiocarbon to investigate the modern carbon cycle.

Keywordsocean carbon cycle, dissolved inorganic carbon cycling, dissolved organic carbon cycling, compound specific radiocarbon analyses, coastal ocean carbon cycling, pre-aged terrestrial carbon

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S12-P-297

RADIOCARBON IN PALAU CORAL REVEALS EARLY BOMB FALLOUT TO THE WESTERN PACIFIC DURING THE EARLY 1950S

GLYNN D.(1), DRUffel e.(1), DUnbaR R.(2), oSboRne M.(2)

(1) University of california, Irvine, IRVIne, UnITeD STaTeS;(2) Stanford University, STanfoRD, UnITeD STaTeS

AbstractThere are three main processes controlling radiocarbon (Δ14C) in the surface ocean; air-sea CO2 exchange, vertical mixing of subsurface waters, and lateral advection by ocean currents. In order to evaluate the variability in surface water masses of the tropical Pacific near Indonesia, we made high-precision radiocarbon measurements of annual and seasonal bands from Porites lutea corals collected from the Palau Islands (7°17.153” N, 134°15.016” E). The Δ14C values trace the bomb radiocarbon signal originating from the Marshall Islands nuclear testing of 1954. This research examined the close-in fallout of bomb 14C that was observed by Fallon and Guilderson (2008) in an Indonesian coral. Palau is located approximately 3,425 km west of the Bikini Atoll and 3,080 km west of the Enewetak Atoll where the large bombs were detonated. This site had the unique opportunity to record a very concentrated signal of these bomb products. Annual bands of coral that grew from 1945 to 2008 were analyzed for Δ14C. Seasonal samples, sub-sampled every 1 mm, were analyzed from 1953 to 1957 in order to capture the detail of the early input of bomb 14C from the weapons testing. Results from radiocarbon analyses show a Δ14C pre-bomb average of -54.5‰ between 1945 and 1954. Beginning early in 1954 there is a rapid increase to a bomb peak high of -23‰ at the start of 1955. The large rise in 14C cannot be fully accounted for by the relatively slow air-sea CO2 exchange that has a turnover rate of ~10 years. We therefore suggest that the primary cause of this increase is due to water containing nuclear fallout being transported by lateral advection via the North Equatorial Current to our site.

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505

S12-P-298

14C DISTRIBUTION OF SEDIMENTARY ORGANIC CARBON IN YELLOW SEA AND NORTHERN EAST CHINA SEA

SHIN K.H.(1), Yoon S.H.(1), YI H.I.(2)

(1) Hanyang University, anSan, SoUTH KoRea;(2) Korean ocean Reaserch and Development Institute, anSan, SoUTH KoRea

AbstractRadiocarbon (14C) has been applied to investigate the source and fluxes and age of carbon in the ocean. In particular, 14C values of organic carbon have been useful information to understand origin and sink of organic matter in the ocean. In this study, we have collected surface sediment from more than 300 sampling sites, and have measured stable carbon and nitrogen isotopes. A map of organic carbon and nitrogen isotopes ratios was described on the entire Yellow Sea and northern East China Sea, indicating apparently lighter carbon isotope ratios at the sites near Sangdong Peninsular. In addition, 14C values of organic carbon in surface sediment were also determined at the same sites. 14C values of organic carbon ranged from 10930±80 to modern. In the near Shangdong Peninsular, the oldest 14C age of organic carbon corresponds to the lighter stable carbon isotopes ratios, reflecting large contribution of terrestrial organic carbon. However, 14C value of organic carbon in the central basin of Yellow Sea is close to modern, which is mainly contributed by marine organic carbon. Other sites in the shelf regions show around 2000 of 14C age. Some sedimentary organic carbon was younger than 2000 14C age in the northern East China Sea where is the area affected by Tsushima Current. In the current study, the 14C values of organic carbon in the surface sediment of Yellow Sea and northern East China Sea seems to be strongly influenced by terrestrial organic carbon or petroleum derived organic carbon from the coastal regions.

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S12-P-299

IMPACT ON SOIL ORGANIC CARBON STORAGE, TURNOVER IN MANGROVE ECOSYSTEM FROM SEA LEVEL RISING IN SOUTHERN CHINA

YI W.(1), SHen c.(1), DInG P.(2), WanG n.(3), DInG X.(4), fU D.(4), lIU K.(4), Wen W.(1)

(1) Guangzhou Institute of Geochemistry,chinese academy of Sciences, GUanGZHoU, cHIna; (2) Guangzhou Institute of Geochemistry,chinese academy of Sciences, beIJInG, cHIna; (3) Department of earth Science, Hongkong University, HonGKonG, cHIna; (4) State Key laboratory of nuclear physics and Technology, Peking University, beIJInG, cHIna

AbstractMangrove ecosystems play an important role in global coastal carbon (C) budgets. However, the impact on sediment organic carbon (SOC) storage and turnover in mangrove forests from sea level rising resulted from global warming are still poorly understood. In this paper, two natural mangrove forests in Southern Chinadominated at high tidal flat (site 1, a Aegiceras corniculatum) and at middle tidal flat (site 2, a bruguiera gymnorrhiza + Kandelia candel), were selected to evaluate the influence of mangrove ecosystems by measuring the organic carbon content and organic carbon isotopic composition (14C and 13C). The results show that SOC density for site 1 is about 674.4 Mg ha-1 and is about 372.8 Mg ha-1 for site 2 in both upper 100 cm. In site 1, SOC δ13C values throughout the soil core ranges from -29.36 to -25.92‰, showing a similar trends of SOC decomposition in terrestrial ecosystems. While in site 2, SOC δ13C value throughout the soil core fluctuates between -26.04‰ and -26.77‰, reflecting an oceanic sedimentary environment. Bomb-14C contained in SOC in different depth in both soil cores are investigated. In site 1, the first Bomb-14C section appears at 2-12 cm in depth with pMC ranging between 100.13 and 101.51 and the second Bomb-14C section at 25 – 60 cm with pMC ranging between 107.58 and 116.29, respectively. And it appears at 2 – 4 cm in depth with pMC varying between 101.30 and 101.95 and 12 – 50 cm with pMC varying between 105.78 and 118.21, respectively in site 2. Based on a Bomb-14C model, SOC decomposes at a rate about 0.004 a-1 and 0.005 a-1 have been estimated in the first Bomb-14C section in site 1 and 2, while, it has a turnover rate between 0.02 a-1 and 0.08 a-1 at the second Bomb-14C section where the most mangrove roots distribute in both sites. Since the sea level changes has little influence on SOC turnover rates, the great difference in SOC density would be attributed to the significant decrease of the litter input from mangrove forest in site 2 where experiences frequent tidal flushing. Therefore, given the sea level rising at 2 mm per year, SOC density in the upper 100 cm in mangrove forest site 1 would decline by 45% in about 50 years.

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S12-P-300

RECENT INTERTIDAL MICROBIAL MATS DATED BY RADIOCARBON

TRICHET J.(1), HaTTÉ c.(2), fonTUGne M.(2)

(1) olIVeT, fRance;(2) lSce, cea-cnRS-UVSQ, GIf-SUR-YVeTTe, fRance

AbstractMicrobial mats (kopara in Polynesian language) that develop in shallow brackish to hypersaline ponds on the rims of atolls were intensively investigated under a microbiological point of view 1 but few is known on their accumulation process and rate. They are a few millimeters to several tens of centimeters deep.Whatever the type of salinity where kopara is found its structure is made of vertically-laminated microbial mats of different colors. Like most of other microbial mats it is dominated by some microorganisms characterized by their functional groups: photosyntetic cyanobacteria, sulfur-photosynthetic bacteria, non-sulfurous red bacteria, sulfate reducers and, deeply, methane producers and oxidizers. These layers are generally the seat of intense high-Mg calcite authigenic minerals precipitation, leading to their possible fossilization under stromatolitic facies 2.Here two sequences of ca. 30 cm deep kopara, out of the Tetiaroa atoll, are investigated. Sampling was performed in 1996. TI and TII sections are respectively composed of seven and five layers distinct by their colors and sedimentological facies. Interest was brought to three points regarding the age of the components of these layers:1) does the kopara sequence accumulate continuously?2) what is the age of bottom kopara layers3) what is the age of carbonate authigenic minerals in each layer, with regards to that of their surrounding organic matter?

Combination of 14C activity measurement on both layer organic and mineral constituents, reservoir age estimation and comparison with Southern Hemisphere atmospheric bomb peak 14C record 3 allowed us to establish a fine chronology of the layer successions.Comparative assessment of both kopara successions shows remarkable similarities in their accumulation process. It shows that1) their succession is not continuous and consists of packages of layers whose ages are continuous,2) accumulation was still active the sampling year (1996),3) oldest age was, in TI section, of year 1958,4) the carbonate minerals are definitely authigenic, precipitating during the year following the deposition of their host-organic matter. As a whole, these dating show that accumulation rate can reach 1cm/year.

The lack of layers whose ages would have been intermediate between the measured ones coincide with those of heavy storms, hurricanes, and cyclones having hit Polynesia between 1958 and 1996. These heavy events however kept in place the deepest layers of such fragile deposit (dated between 1958 and 1992). Such global results are interesting for reconstructing the sedimentological and petrographical history of microbially-derived sedimentary deposits and, presently, for the use of organic, fast growing and renewable, resources.

References1. e.g. Mao-Che et al. (2001) Can. J. Microbio.; Richert et al. (2006) Eur. J. Phycol.; Guézennec et al. (2011)

Process Biochemistry2. Défarge Ch. et al. (1994) Sed. Geol.3. Hua et al. (2004) Radiocarbon

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S12-P-301

SPATIAL DISTRIBUTION OF RADIOCARBON IN THE SOUTHWESTERN JAPAN/EAST SEA RIGHT AFTER THE BOTTOM WATER RENEWAL

ARAMAKI T.(1), TanaKa S.S.(1), KUSHIbaSHI S.(1), KIM Y.I.(2), HonG G.H.(2)

(1) national Institute for environmental Studies, Japan, TSUKUba, JaPan;(2) Korea ocean Research and Development Institute, anSan, SoUTH KoRea

AbstractThe Japan/East Sea, which has a maximum depth of more than 3700 m, is a marginal sea separated from the western North Pacific by the Japanese Islands and Sakhalin. Because of its shallow sill depths (<140 m), the deep water in the Japan/East Sea, which is called the Japan Sea Proper Water (JSPW), is formed within the Sea itself. JSPW consists of two waters of the bottom water (lower layer of JSPW) and the deep water (above the bottom water). The bottom water is characterized by extremely homogeneous in the vertical distribution of temperature and chemical variables of seawater such as dissolved oxygen. The origin of the water is the surface water in the northern Japan/East Sea, because the surface water in winter due to evaporation and/or freezing at the sea surface is dense enough to sink toward the bottom. Therefore, the bottom water is colder and richer in dissolved oxygen than the deep water in the North Pacific. The dissolved oxygen in the bottom water, however, has been decreasing since the 1960’s or earlier to the present, probably due to the reduced deep convection in the sea during the recent global warming. On the other hand, newly formed bottom water was found in the northwestern Japan/East Sea in the summer of 2001 after the severe winter 2000–2001. The new bottom water showed low temperature, high salinity and high dissolved oxygen compared to the old bottom water. The hydrographical analysis indicated that the bottom water was formed in the south off Vladivostok, Russia and the formation event occurred in the late January-early February 2001.Generically, the radiocarbon of dissolved inorganic carbon (DIC) in the ocean is higher in the surface layer and decreases with water depth, because radiocarbon enters the ocean through air-sea CO2 gas exchange only and then decreases with the progress time from which it enters the ocean due to its radioactive decay and mixing with “old” radiocarbon deficient seawater. Therefore when the bottom water renewal in the Japan/East Sea occurrs, the radiocarbon of DIC in the bottom water would increase like dissolved oxygen concentration. In April 2001 right after the bottom water renewal, a hydrographic survey of the Korea Ocean Research and Development Institute carried out in the southwestern Japan/East Sea south of the bottom water formation area. Seven vertical profiles of radiocarbon were obtained from the area including the Japan Basin and the Ulleung Basin. In the station at south edge of the Japan Basin, higher radiocarbon than those in other statons were observed in JSPW below 1000 m depth to bottom. It suggests that the newly formed bottom water had flowed southward at the Japan Basin just within 2 months. However, the water had not reached at the Ulleung Basin which is separated from the Japan Basin by a sill around the Ulleung Island. Detailed analisis of the radiocarbon results yields valuable information in study on the bottom water circulation in the Japan/East Sea.

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509

S12-P-302

POC PROVENANCE INSIGHTS FROM RAMPED THERMAL DEGRADATION AND 14C ANALYSES

BEAUPRE S.(1), eGlInTon T.(2)

(1) Woods Hole oceanographic Institution, WooDS Hole, UnITeD STaTeS;(2) eTH, ZURIcH, SWITZeRlanD

AbstractVertical transit times of sinking particulate organic carbon (POC) in the open ocean based on decreasing Δ14C values with depth significantly exceed estimates based on particle sinking velocities. Neither radioactive decay nor isotopic fractionation can account for this discrepancy. Rather, it has been hypothesized to arise from incorporation of constituents at depth from the comparatively Δ14C-depleted pools of dissolved organic carbon (DOC), dissolved inorganic carbon (DIC), and laterally transported resuspended sediments. To constrain this provenance, Δ14C values were measured on CO2 generated from the oxidation of sinking POC during a 5°C/min ramp from room temperature to 1000°C. This method produces coarse spectra of concentrations and Δ14C values as functions of temperature that i) are representative of bulk POC based on mass balance and ii) reveal the abundance of underlying populations of carbon and their estimated Δ14C values. The utility of this method as applied to POC and potential constraints on Δ14C-depleted carbon sources are discussed.

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510

S12-P-303

TEMPORAL VARIATIONS IN THE OCEANIC PROPERTIES OF THE NORTHERN INDIAN OCEAN SINCE GEOSECS

BHUSHAN R.(1), DUTTa K.(2), aGnIHoTRI R.(3), RenGaRaJan R.(1)

(1) Physical Research laboratory, aHMeDabaD, InDIa;(2) large lakes observatory, University of Minnesotta, DUlUTH, UnITeD STaTeS;(3) national Physical laboratory, DelHI, InDIa

AbstractReoccupation of several stations occupied in the northern Indian Ocean during 1997-99 nearly two decades after GEOSECS (1977-78) provides temporal changes of oceanic properties. These changes are manifestations of the environmental/climatic changes caused due to natural or anthropogenic processes. Several stations in the Arabian Sea, the equatorial Indian Ocean and the Bay of Bengal were reoccupied during various cruises during the period 1997-1999. Vertical profiles of seawater samples were collected from various depths to ascertain decadal changes in salinity, temperature, dissolved O2, ΣCO2, pH, Nutrients and radiocarbon. Marginal changes in the silicate, phosphate and oxygen was observed with nitrate and nitrite showing significant decrease. Noticeable variation in the radiocarbon concentrations in the top 1000m were observed in all the station. Significant changes in the radiocarbon content of the upper 1000m is due to the introduction of bomb radiocarbon introduced in the atmosphere during early 1950’s caused by nuclear testing conducted in the stratosphere. Decadal changes in seawater properties and its implications would be discussed.

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S12-P-304

FIRST HIGH-RESOLUTION TIME SERIES OF PRE AND POST-RADIO-CARBON CONCENTRATION IN THE NW MEDITERRANEAN SEA (LIGURIAN SEA) DERIVED FROM THE CORAL CLADOCORA CAESPITOSA

TISNÉRAT-LABORDE N.(1), MonTaGna P.(1)(2), DUMoUlIn J.P.(3), SIanI G.(4), SIlenZI S.(5), PaTeRne M.(1)

(1) laboratoire des Sciences du climat et de l’environnement/IPSl, cea-cnRS-UVSQ, GIf-SUR-YVeTTe, fRance;(2) Istituto di Scienze Marine, cnR, boloGna, ITalY;(3) laboratoire de Mesure du carbone 14, UMS 2572, cea Saclay, GIf-SUR-YVeTTe, fRance;(4) laboratoire Interactions et Dynamique des environnements de Surface IDeS, UMR 8148 cnRS-Université Paris-Sud 11,

oRSaY, fRance;(5) Istituto Superiore per la Protezione e la Ricerca ambientale, RoMe, ITalY

AbstractWith the introduction of bomb 14C produced by atmospheric testing of thermonuclear weapons in the 1950s and early 1960s, radiocarbon time series in surface ocean provide information about air-sea 14CO2 exchanges and variations in ocean circulation. Continuous 14C records have been mainly obtained from annually-banded tropical corals and provide direct integrated measures of 14C of the dissolved inorganic carbon from the surrounding ambient seawater (Druffel and Linick 1978; Druffel, 1986). Until now, 14C time series exist in the Atlantic, Pacific and Indian Oceans, but not in Mediterranean Sea, which is expected to have a rapid response to the global warming and sea water acidification.Here, we present the first annually-resolved time series of 14C for the surface Western Mediterranean Sea obtained from a long-lived specimen of the zooxanthellate coral Cladocora caespitosa. A 14.5 cm long corallite was collected alive by SCUBA diving in 1998 at 28 m water depth in Bonassola (Northern Tyrrhenian Sea). C. caespitosa has a rectilinear continuous growth and deposits two density bands per year; one high-density band in winter and one low-density band in summer (Peirano et al., 1999). The size of the coral corresponds to an age of 56 years considering a mean annual linear growth rate of 2.58 mm/yr for the colony in Bonassola (Peirano et al., 1999) and high-resolution trace element variations derived by laser ablation ICP-MS (Montagna et al. unpublished data).The Δ14C average of the pre-bomb surface waters is -55 ± 3‰ corresponding to a reservoir age of 269 ± 35 years between 1942 and 1950. The uptake of 14C bomb is revealed by a steady increase after 1950, with an initial leveling off in 1956-1957. Between 1957 and 1963, Δ14C values rise quickly until 1963, similarly to the trend recorded in the North-Eastern Atlantic (NEA) surface ocean. While NEA Δ14C values still increase until 1967, the Mediterranean record shows a slower rise to a maximum value of 90 ± 5‰ in 1972. A steady decrease with temporal variability of about 10‰ is recorded by the coral after 1972. Based on these new results, we will discuss the efficiency of radiocarbon uptake in surface Mediterranean Sea water compared to NEA and its 14C variability in terms of changes in oceanic circulation.

References1. E.R.M. Druffel, T.W. Linick (1978) Radiocarbon in annual coral rings of Florida. Geophysical Research Letters

5:913–916.2. E.R.M. Druffel (1996) Post-bomb radiocarbon records of surface corals from the tropical Atlantic Ocean.

Radiocarbon 38:563–572.3. A. Peirano, C. Morri, C.N. Bianchi (1999) Skeleton growth and density pattern of the temperate, zooxanthellate

scleractinian cladocora caespitosa from the Ligurian Sea (NW Mediterranean). Marine Ecology Progress Series 185:195-201.

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S12-P-305

AUTOMATED qUANTITATIVE EXTRACTION OF CO2 FROM (SEA-) WATER SAMPLES

VAN HEUVEN S., SIePMan D., HoGeVeen P., JonKeR W., MeIJeR H.

University of Groningen, GRonInGen, neTHeRlanDS

AbstractWe are in an advanced state of development and testing of an instrument for the automated, quantitative extraction and subsequent storage (in duplicate) of CO2 from water samples. The finished instrument will facilitate the analysis of large amounts of such samples for Δ14C and δ13C. The instrument additionally determines the amount of CO2 extracted from samples (nCO2) with sufficient accuracy and precision to be of value to the ocean carbon chemistry community (when expressed as DIC: circa ±2 μmol kgSW-1).Design goals for the instrument included

a) fully automatic operation, except for connection and removal of samples and storage tubes;b) the ability to sequentially process up to 8 samples in a single run;c) high throughput (>4 samples per hour);d) extraction efficiency of >99.99% and (thereby) very low fractionation in order to allow analysis of δ13C;e) precise and accurate quantification of nCO2;f) safe operation irrespective of the unknown and potentially large amount of CO2 contained by, for instance, groundwater.

The developed instrument extracts CO2 by means of (non-recirculating) sparging of acidified sample with N2 at near-atmospheric pressure, followed by trapping (with LN2) of CO2 at reduced pressure (circa 10 mbar). This method allows for high sparging rates without risking loss of CO2 from the single cold finger. The extraction process can be monitored in real time through a CO2 sensor upstream of the cold finger. A dedicated IRGA CO2-sensor located at the end of the extraction line verifies the full upstream retention of CO2. Throughput is optimized by performing quantification and storage of a sample concurrently with the extraction of CO2 from the next sample. Measurements of pressure and temperature of the extracted gas (requisite for determination of nCO2) are performed after automated drying and temperature equilibration of the containing glassware. The LabView-controlled system continuously monitors and logs flows, pressures, concentrations et cetera in order to ascertain rapid and demonstrably quantitative extraction.Early application suggests the feasibility of processing 8 samples in 2 hours. We will present an estimate of the spread in δ13C in replicate samples (an important metric for the reproducibility of the extraction) and first results of the measurements of standard material. Additionally, we will report accuracy and reproducibility of the determination of nCO2.

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S12-P-306

EXTRANEOUS CARBON CORRECTIONS FOR Δ14C MEASUREMENTS IN BLACK CARBON SEDIMENTS USING THE BENZENE POLYCARBOXYLIC ACID METHOD

COPPOLA A.(1), ZIolKoWSKI l.a.(2), ZHenG D.(1), XU X.(1), DRUffel e.R.(1)

(1) University of california Irvine, IRVIne, UnITeD STaTeS;(2) McMaster University, HaMIlTon, canaDa

AbstractExtraneous, or blank carbon added during chemical processing and isolation of Black Carbon (BC) in sedimentary organic carbon was studied for its impact on radiocarbon (Δ14C) measurements. The addition of extraneous carbon (Cex) to samples is inevitable during the extensive pre-treatment and extraction of BC from sediments using the Benzene Polycarboxylic Acid Method. The isolation and collection of resulting BC molecular markers by preparative capillary gas chromatography (PCGC) is another source of Cex to the samples. Extraneous carbon is introduced during many steps, including incomplete removal of solvents, and bleed from the gas chromatograph and cation-exchange resin columns. The isotopic signature and mass of Cex significantly affects the radiocarbon value of the sample if uncorrected.There are two approaches to correct Δ14C values for additions of Cex to BC samples. In the direct approach, a process blank evaluates the Cex directly by processing initially empty containers with the absence of a sample through the entire method, identically to the treatment of an actual sediment sample. To obtain enough carbon for AMS measurement, the process blank was injected into the PCGC three hundred times, and then normalized per number of injections for comparison to BC sediment samples. We found that direct corrections using process blanks did not correct the BC standards to reach their known consensus Δ14C values. Alternatively, an indirect approach quantifies Cex as the difference between processed and unprocessed Δ14C values in BC standards. The standards we used to evaluate Cex were Risotto grass char, Chestnut wood char, and SRM 1649a aerosols. In this study, the indirect method was best suited to correct standards for the presence of Cex, because it accounted for matrix effects, which is not represented by a direct blank. Corrections applied to the BC standards were then applied to BC samples to correct Δ14C values for the influence of Cex. As with any AMS reported Δ14C values, we highly advocate the use of the multiple approaches to investigate extraneous C corrections throughout sample processing.

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S12-P-307

INITIATION OF A RADIOCARBON DATABASE FOR ORGANIC CARBON IN MARINE SURFACE SEDIMENTS

EGLINTON T.(1), TaVaGna M.l.(1), blaTTMann T.(1), GRIffITH D.(2)

(1) eTH Zurich, ZURIcH, SWITZeRlanD;(2) Woods Hole oceanographic Institution, WooDS Hole, UnITeD STaTeS

AbstractRadiocarbon has proven to be a powerful tool for assessing the sources and pre-depositional history of organic components accumulating in aquatic sediments, yielding complementary information to that derived from other geochemical approaches. In particular, 14C provides a means to trace and quantify organic carbon (OC) derived from recent biological productivity, and to distinguish it from more slowly cycling carbon pools. We have compiled available core-top 14C data for bulk OC in surface (upper few cm) marine sediments in order to examine the spatial variability in 14C contents and to relate this variability to organic matter source and composition, as well as sedimentological factors. Emphasis is placed on continental margin environments because of their global importance as sites of OC burial. Measured OC 14C contents are compared with predicted estimates for the surface sediment mixed layer based on a simple model that incorporates information on sediment accumulation rate and mixed layer depth, and which assumes sedimentary organic matter is exclusively derived from surface ocean primary productivity (Griffith et al., 2010). Discrepancies between measured and modeled 14C contents provide a framework for considering other factors (e.g., terrestrial OC inputs, sediment redistribution processes) that influence OC accumulation in the marine environment. Additional parameters are being incorporated into the core-top database in order to examine 14C contents in the context of the depositional setting and organic matter characteristics, as well as to utilize 14C to constrain biospheric carbon burial. We are presently seeking to expand the spatial coverage of the existing 14C dataset for core-top marine sediments (~1000 measurements) to cover a broader range of oceanographic provinces and depositional environments in order to develop a global perspective on the overarching controls on sedimentary organic matter abundance, age and composition. This presentation will describe the database and model, and highlight examples of the types of information that are emerging from the database.

References Griffith D.R., Martin W.R. and Eglinton T.I. (2010) The radiocarbon age of organic carbon in marine surface sediments. Geochim. cosmochim. acta. 74, 6788-6800

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S12-P-308

RADIOCARBON AND NEODYMIUM: COMPLEMENTARY (SEDIMENT) BEDFELLOWS?

EGLINTON T.(1)(2), HWanG J.(3)(2), blUSZTaJn J.(2), ManGanInI S.(2), GIoSan l.(2)

(1) eTH Zurich, ZURIcH, SWITZeRlanD;(2) Woods Hole oceanographic Institution, WooDS Hole, UnITeD STaTeS;(3) Pohang University of Science and Technology, PoHanG, SoUTH KoRea

AbstractThere is growing evidence that particle remobilization and lateral transport can disperse sediments and associated organic matter over continental margins and the ocean’s interior basins. In some cases, organic materials come to rest on the sea floor hundreds to thousands of kilometers away from their site of formation. These processes have significant implications for our understanding of the cycling of organic matter delivered to, and produced in the ocean, as well as for the interpretation of sediment records as archives of paleoclimate and paleoceanographic information.One of the key observations indicating redistribution of organic matter is the presence of old particulate organic carbon, which may reflect aging during temporary storage prior to dispersal, or during transport. This carbon is likely carried with fine-grained detrital mineral host materials that are susceptible to resuspension and dispersal as nepheloid layers. Establishing the provenance of the sediments that entrain this carbon represents an important challenge in reconstructing the sources and trajectories of materials laterally transported in the ocean.Neodymium concentrated in fine-grained detrital sediments provides a powerful tool to establish sediment provenance for systems where strong contrasts exist in the geologic age of terrigenous sediments supplied to ocean basins due. We provide examples from the northwest Atlantic margin and the Arctic Ocean (Canada Basin) to illustrate the complementary information that can be derived from coupled radiocarbon and neodymium isotopic studies of water column particles and seafloor sediments. These studies reveal both the strong influence of lateral transport on particle and organic carbon dynamics as provide important constraints on the sources of advected materials.

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S12-P-309

DO RADIOCARBON SIGNATURES OF SURFACE OCEAN DISSOLVED INORGANIC CARBON AND PLANKTON CARBON AGREE?

BERTRAND C., GRIffIn S., DRUffel e.


AbstractIt is usually assumed that Δ14C of dissolved inorganic carbon (DIC) and plankton in surface seawater are similar, but very little research has been conducted to answer this question. We report radiocarbon measurements of DIC (Druffel, et al., 2010, Hwang, et al., 2004) and plankton samples collected from the same surface water samples during 10 cruises from 1995-2004. The majority of the samples are collected from “Station M” in the northeast Pacific, 220 km off Point Conception, California (34° 50’N, 123° 00’W). The Δ14C values decrease with time, reflecting the decrease in bomb carbon, with most values ranging from 20-60‰. We will show that the trend does display seasonal variability; however it is not consistent from year to year. In general, the DIC Δ14C values are equal to or are higher than the plankton Δ14C values. This trend may indicate that plankton can take up older carbon from deeper in the water column. The presence of very old carbon was observed for two of our plankton samples. We believe that these results indicate contamination by plastic material, which have been shown to be present in convergent zones of the open ocean.

References1. Druffel, et al., 20102. Hwang, et al., 2004

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S12-P-310

EVIDENCE FOR THE SIZE-AGE-COMPOSITION CONTINUUM OF MARINE ORGANIC MATTER: IMPLICATIONS FOR CARBON CYCLING IN THE COASTAL AND OPEN OCEAN

WALKER B.(1), MccaRTHY M.(2), beaUPRe S.(3), DRUffel e.(1), GUIlDeRSon T.(4)

(1) University of california Irvine, IRVIne, UnITeD STaTeS;(2) University of california, SanTa cRUZ, UnITeD STaTeS;(3) Woods Hole oceanographic Institution, WooDS Hole, UnITeD STaTeS;(4) lawrence livermore national laboratory, center for accelerator Mass Spectrometry, lIVeRMoRe, UnITeD STaTeS

AbstractWater column organic matter (OM) size class is strongly linked to bioavailability, an idea typically referred to as the “size-reactivity continuum” hypothesis. As a result, relative physical size is thought to be a key factor for predicting the relative fate and lability of detrital OM (i.e. containing the lowest C:N ratios, abundance of “fresh” biomolecules and high Δ14C signatures). However, bioavailability is not always synonymous with 14C-content, and to what degree organic matter physical size may correlate with 14C-age is far less certain. Recently, Walker and coauthors (2011) showed that within the oligotrophic open ocean dissolved OM (DOM) pool, relative molecular size and Δ14C are strongly linked. While a few qualitative observations of a size-age relationship have included particulate OM (POM) samples, to date the potential relationship between OM size, composition and Δ14C has never been directly tested for any ocean region. Here we present a compilation of new and previously published Δ14C and C:N data comparing a wide range of organic size-classes (including size-fractionated suspended POM, total DOM, and high molecular weight DOM), from the coastal and oligotrophic Pacific ocean. These results suggest a robust size-age-composition continuum exists between all OM size-classes, from particulate to dissolved OM. To our knowledge, this is the first time that bulk chemical composition, Δ14C values, and OM size have been shown to be quantitatively linked in the ocean. We will discuss these results and their implications for ocean carbon cycling within the context of size-reactivity ideas, and in particular for modes of POM/DOM transformation mechanisms.

ReferencesWalker, B.D., Beaupre, S.R., Guilderson, T.P., Druffel, E.R.M., McCarthy, M.D., 2011. Large-volume ultrafiltration for the study of radiocarbon signatures and size vs. age relationships in marine dissolved organic matter. Geochimica Cosmochimica Acta 75, 5187-5202.

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S12-P-311

THE WOCE/CLIVAR RADIOCARBON PROGRAMS: WHAT DI14C REVEALS ABOUT OCEAN PROCESSES

McNICHOL A.(1), KeY R.(2), JenKInS W.(1), elDeR K.(1), Von ReDen K.(1), GaGnon a.(1), bURTon J.(1)

(1) noSaMS/WHoI, WooDS Hole, UnITeD STaTeS;(2) Princeton University, PRInceTon, UnITeD STaTeS

AbstractAn important goal of the National Ocean Sciences Accelerator Mass Spectrometry Facility (NOSAMS) has been to measure the radiocarbon content of dissolved inorganic carbon (DI14C) samples collected during the global survey programs of WOCE and CLIVAR. As an ocean tracer, radiocarbon is unique and important for a number of reasons. It has both natural and anthropogenic components that, combined, make it an important diagnostic of global ocean circulation models on time scales ranging from decades to millenia. It participates in the global carbon cycle and is a key tracer of material transport by biogeochemical cycling. Its atmospheric history is exceptionally well known from air samples and measurement of tree rings. The known history coupled with its huge “isotopic inertia” makes it a tracer of air-sea exchange on decadal timescales. In addition, coral records (both near surface and benthic) provide a detailed time series of DI14C changes over decades and centuries that give us insight into past variations in ventilation, circulation, and carbon cycle. Finally, the time history of its delivery is unique among other transient tracers (e.g., CFCs, SF6,

3H) so that it provides valuable additional information about ocean ventilation and circulation.We have analyzed over 21,000 individual samples; data from these analyses are available at unrestricted web sites. WOCE results provide a global snapshot of the radiocarbon distribution in all oceans. Reoccupations of WOCE lines during CLIVAR permit a study of the migration of the bomb-produced DI14C spike through the global thermocline and abyssal oceans. Central to these studies is the comparability of measurements made over decades. We demonstrate this by analyzing splits of gas stored from our original preparation of the WOCE and CLIVAR samples. Repartitioning of bomb radiocarbon between oceanic regions is an important signature of ocean circulation. In the Pacific Ocean, significant changes are observed over 15 years. Jenkins et al. (2010) calculated both increases and decreases of up to 70 ‰ in the surface 1500 m of 150°W in the southern hemisphere. Not only is the bomb signal penetrating deeper, it is also moving laterally away from the central gyres. Three cruises along 32°S coupled with limited data from the 1970’s GEOSECS Program document a relatively constant decrease of 2.6 ‰/yr in the surface water across the entire basin. A Southern Atlantic transect along the prime meridian shows the transport of the bomb signal into this region from the western basin. Here we present more results from the Pacific, Atlantic and Indian Oceans as well as discuss their implications for our understanding of carbon cycling, physical transport processes (e.g. wind-induced gas exchange), and ocean general circulation models.

References Jenkins W.J., K.L. Elder, A.P. McNichol and K. von Reden (2010) The passage of the bomb radiocarbon pulse into the Pacific Ocean. Radiocarbon 52, p1182-1190.

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S12-P-312

INSIGHTS OF CARBON CYCLING IN ARCTIC OCEAN BY USING DUAL CARBON ISOTOPE PROFILES OF DIC, DOC AND POC

XU L.(1), McnIcHol a.(1), GRIffITH D.(1), MclaUGHlIn f.(2), MacDonalD R.(2), bRoWn K.(3), eGlInTon T.(4)

(1) Woods Hole oceanographic Institution, WooDS Hole, UnITeD STaTeS;(2) Institute of ocean Sciences, fisheries and oceans canada, SIDneY, canaDa;(3) Dept. of earth and ocean Sciences, University of british columbia, VancoUVeR, canaDa;(4) Geological Institute, Swiss federal Institute of Technology, ZÜRIcH, SWITZeRlanD

AbstractThe recent warming in the Arctic is affecting broad systems in this region. Some of the changes may be irreversible on century time scale and may cause rapid changes in the earth system. A good understanding of the carbon cycle is very import to predict the regional even global climate change. Here we present the first set of concurrent, full-depth, dual-isotope (14C and 13C) profiles for dissolved inorganic carbon (DIC), dissolved organic carbon (DOC), and suspended particulate organic carbon (POCsusp) at two sites in the Canada Basin of the Arctic Ocean. One site is seasonally ice-covered (CB-4) and the other is permanently ice-covered (CB-9). Relatively stronger biological pump is indicated as younger DOC at the ice-covered location (CB9). The 14C composition of sinking and suspended particle is unique compare to that at open Atlantic and Pacific sites. Mass balance calculation shows that surface derived organic carbon is a major source of POCsusp and OC derived from in situ DIC fixation contributes up to 22% POCsusp. Small vertical POC fluxes in the Canada Basin make it possible to see evidence of DIC fixation even at the bulk isotope level.

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SESSION 14

CONTINENTAL CARBON CYCLE

ConvenersT. Chiti (ITA), P. moreira-Turcq (FRA), J. Rethenmeyer (DEU)

DescriptionThe investigation of organic carbon dynamics in continental carbon reservoirs is complicated by the highly heterogeneous composition and relatively rapid turnover of organic matter in soils and continental aquatic sediments. 14C has proven to be a useful indicator for different carbon sources and tracer for organic matter degradation and transport processes. In this session we would like to bring together scientists using 14C analysis to determine residence times and stable/labile carbon pools, identify microbial degradation of organic matter, the loss of gaseous and dissolved carbon from terrestrial systems, and transport of plant and soil derived carbon into rivers, lake and coastal sediments. Contributions using or further developing methodical approaches such as fractionation methods and compound-specific 14C analysis are also welcome.

Keywordssoil carbon cycling, turnover times, carbon transport, compound-specific 14C

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S14-P-313

COMPOUND-SPECIFIC 13C & 14C ANALYSIS OF SOIL LIPIDS ALONG A SAVANNA (C4)/EUCALYPTUS (C3) CHRONOSEqUENCE (POINTE-NOIRE, CONGO): NEW INSIGHTS TO RESOLVE SOIL ORGANIC CARBON DYNAMICS (DYNAMOS ANR-PROJECT)

MenDeZ-MIllan M.(1), nGUYen TU T.T.(2)(3), ÉGaSSe c.(2), DeRenne S.(3), DeRRIen D.(4), ZelleR b.(4), baleSDenT J.(5), HATTÉ C.(1)(5)

(1) lSce, cea-cnRS-UVSQ, GIf-SUR-YVeTTe, fRance;(2) cR2P, MnHn-cnRS-UPMc, PaRIS, fRance;(3) bioeMco, cnRS-UPMc, PaRIS, fRance;(4) bef, InRa, cHaMPenoUX, fRance;(5) GSe, InRa, aIX-en-PRoVence, fRance

AbstractThe world experiences an important afforestation which strongly affects the global carbon cycle and primarily one of its key compartments, the soil organic carbon (SOC). One way to understand the fundamental processes that take place during such a land use change is to focus on lipids, important contributors to SOC since they influence soil physical and chemical properties.The sylviculture located at the Republic of Congo, area of Pointe-Noire, is a C4/C3 chronosequence, were native savanna (C4) was replaced with eucalyptus (C3). Molecular composition of the apolar lipid fractions were determined in plants and soils (0-20cm) cropped with eucalyptus for 0, 7.5, 17 and 30 years. 13C isotopic signature and 14C measurement were achieved for relevant plant markers to assess SOC dynamics: three major pentacyclic triterpene methyl ethers (PTMEs), crusgallin, isosawamilletin and milliacin,which were specifics for savanna vegetation and three odd n-alkanes n-C25, n-C27 and n-C29 common to both vegetations.PTMEs, remained abundant in soils after 30 years of eucalyptus coverage and 13C analyses displayed constant δ13C over the trial, close to the δ13C measured in savanna vegetation. Nevertheless, their 14C content increased along the eucalyptus crop pointing to the mineralisation of more stabilized PTMEs. Compound-specific 13C analyses of soil n-C25 and n-C27 showed typical trend of a C4/C3 vegetation shift. Surprisingly, the n-C29 13C content is of -30,5‰ for all stands. Compound-specific 14C analyses displayed that under savanna soil the n-C29 was older than the n-C25 and n-C27. A part of the n-C29 alkanes comprised a significant amount of n-C29 from the past C3 vegetation. With afforestation, 14C content decreased for intermediate stands, and increased for 30 years of eucalyptus coverage. High level of mineralisation of younger n-alkane pool occurred within the first years of the trial. Afterwards, 14C content reflected the contribution of new n-alkanes from the eucalyptus vegetation.At molecular level, dynamics is compound specific andisclearly affected by molecular composition of new vegetation inputs. 13C isotopic analysis allowed for dynamics of recently OC inputs, whereas 14C measurements assessed the dynamics of the entire OC pool. The use of both 13C and 14C isotopes analyses improved dynamics understanding and allowed for a better parametrisation of models developed to determine SOC dynamics. The afforestation involved a new equilibrium between the proportion of “old” compounds previously stabilized, and “recent” compounds incorporated, pointing to dramatic changes in soil lipids composition that will probably affect soil chemical and physical properties.

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S14-P-314

DISTRIBUTION OF RADIOCARBON AGES IN SOIL ORGANIC MATTER BY THERMAL FRACTIONATION

PLANTE A.F.(1), beaUPRe S.R.(2), RobeRTS M.(2), baISDen T.(3)

(1) University of pennsylvania, PHIlaDelPHIa, UnITeD STaTeS;(2) Woods Hole oceanographic Institution, WooDS Hole, UnITeD STaTeS;(3) national Isotope centre, GnS Science, GRacefIelD, neW ZealanD

AbstractRadiocarbon analysis is an important tool in quantifying soil organic matter dynamics within the terrestrial carbon cycle (Trumbore 2009). Measuring radiocarbon concentrations in bulk soil samples provides the mean age or residence time of the associated organic matter. However, it is well known that soil organic matter consists of a heterogeneous spectrum of materials, and that representing it as a single, homogeneous pool with a single, mean radiocarbon concentration is inadequate. Significant effort has gone into separating soil organic matter into pools with different intrinsic radiocarbon concentrations, but the success of these methods has been mixed. We ask:do the differing patterns in CO2 release during thermal analysis reflect organic matter of different ages, and hypothesize that thermally labile soil organic matter (combusting at low temperatures) consists of younger carbon than thermally resistant organic matter. Using thermal analysis techniques to fractionate soil organic matter is rooted in the hypothesized link between the thermal and biogeochemical stability of the organic matter (Plante et al. 2011).Grassland topsoil samples under contrasting land uses (native vegetation and long-term cultivation) were selected for radiocarbon analysis. Results of bulk 14C analyses showed a significant shift in radiocarbon age from 94 PMC under native vegetation to 79 PMC under cultivation, which is attributed to depletion of labile organic matter during long-term cultivation. Thermogravimetry and evolved gas analysis also showed distinct patterns in mass loss and CO2 release during heating, suggesting significant changes in organic matter composition due to land use. Four to five thermal “fractions” associated with different CO2-evolution regions were identified and analyzed for radiocarbon via NOSAMS’ established “dirt burner” method (Rosenheim et al. 2008), consisting of a recently developed discrete CO2 fraction collector interface between NOSAMS’ dirt burner and microwave gas ion source (GIS) continuous flow AMS system (CFAMS).Results showed that thermally stable soil organic matter fractions appear older (i.e., smaller fraction modern), and that differences were greater in the cultivated soil compared to native vegetation soil. However, results are confounded by overlap of thermal reactions, and planned regression analyses will more accurately identify the radiocarbon ages of each deconvoluted peak.

References1. Plante, A. F., J. M. Fernandez, M. L. Haddix, and R. T. Conant. 2011. Biological, chemical and thermal indices

of soil organic matter stability in four grassland soils. Soil Biol. Biochem. 43: 1051-1058.2. Rosenheim, B. E., M. B. Day, E. Domack, H. Schrum, A. Benthien, and J. M. Hayes. 2008. Antarctic sediment

chronology by programmed-temperature pyrolysis: Methodology and data treatment. Geochemistry Geophysics Geosystems 9: 1-16.

3. Trumbore, S. 2009. Radiocarbon and soil carbon dynamics. Annu Rev Earth Pl Sc 37: 47-66.

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S14-P-315

CARBON ALLOCATION IN GRASSLAND COMMUNITIES UNDER DROUGHT STRESS FOLLOWED BY 14C PULSE LABELLING

SANAULLAH M.(1)(2), cHabbI a.(1)(3), RUMPel c.(1), KUZYaKoV Y.(4)

(1) bIoeMco, cnRS-InRa-Université Paris VI, THIVeRVal-GRIGnon, fRance;(2) Institute of Soil and environmental Sciences, University of agriculture, faISalabaD, PaKISTan;(3) Uefe, InRa Poitou-charentes,, lUSIGnan, fRance;(4) Department of agroecosystem Research, University of bayreuth, baYReUTH, GeRManY

AbstractAlthough extreme climatic events such as drought may have important consequences for belowground carbon (C) cycling but their impact on the plant-soil system is poorly understood. Our objective was to study the effect of drought on C allocation and rhizosphere-mediated CO2 fluxes under three plant species: lolium perenne, festuca arundinacea and Medicago sativa grown in monocultures or mixture. The conceptual approach included 14CO2 pulse labeling of plants grown under drought and optimum water conditions in order to follow above- and belowground C allocation. After six days of incubation, we traced 14C partitioning in plant biomass, soil and rhizospheric CO2, dissolved organic carbon (DOC) and in microbial biomass. Drought and plant community composition significantly affected assimilate allocation in the plant-soil system. Drought conditions changed the source sink relationship of monocultures, which transferred a relatively larger portion of assimilates to their roots compared to water sufficient plants. In contrast, plant mixtures additionally increased 14C allocation to shoots. Under drought stress, root respiration was reduced for all monocultures except under legume species. Microbial respiration remained similar in all cases showing that microbial activity was less affected by drought than root activity. This may be explained by strongly increased assimilate allocation to easily available DOC under drought. In conclusion, plant community composition may modify the impact of climatic changes on carbon allocation and belowground carbon fluxes which were determined through 14C pulse labelling. The presence of legume species may attenuate drought effects on rhizosphere processes.

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S14-P-316

FACTORS CONTROLLING LATE HOLOCENE ORGANIC MATTER SEDIMEN-TATION IN AN AMAZON FLOODPLAIN LAKE, MARACA LAKE, BRAZIL

MOREIRA L.(1), MoReIRa-TURcQ P.(2), TURcQ b.(2), coRDeIRo R.c.(1), KIM J.H.(3), caQUIneaU S.(2), SInnInGHe DaMSTÉ J.(3)

(1) Universidade federal fluminense, nITeRÓI, bRaZIl;(2) Institut de recherche pour le développement, bonDY, fRance;(3) Royal netherlands Institute for Sea Research (nIoZ), Den bURG, TeXel, neTHeRlanDS

AbstractIn order to understand the impact of the Amazon River hydrological changes on the source of the organic matter in Amazonian floodplain lakes, three sedimentary cores were collected from Maracá Lake (Eastern Amazonia) along a transect from the Amazon River main channel to the catchment area. The cores were dated with 14C Accelerator Mass Spectrometry, X-rayed and analyzed for total organic carbon, nitrogen content (TN), stable isotopes (δ13CTOC and δ15N) and mineralogical composition. The results acquired enabled to reconstruct the variations in Maracá Lake during the transition between the Middle to Late Holocene. Between 3600 and 2700 cal years BP the low δ15N, low values of δ13CTOC and higher C:N ratios and high TOC suggesting an environment dominated by C3 land plants. The higher concentration of kaolinite in this period suggests the presence of a semi-isolated lake with a reduced influence of the Amazon River. Since 2700 cal years BP, the high levels of smectite and low concentrations of carbon and C:N ratios, are interpreted as larger inputs of the Amazon River. These characteristics indicate a higher water level of the Amazon River since 2700 cal years BP that has a direct influence on the floodplain lake and consequently impacts in its ecology and sedimentology.

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S14-P-317

ENVIRONMENTAL CHANGES DURING THE HOLOCENE FROM THE SACI LAKE RECORD, PARá STATE - SOUTHEASTERN AMAZON BASIN

MARTINS G.S.(1), fonTeS D.(1), coRDeIRo R.c.(1), TURcQ b.(2), MoReIRa l.S.(1), RoDRIGUeS R.a.(3), GUIlleS M.c.c.(1), SanToS a.b.(4), anIceTo K.c.P.(1), SIfeDDIne a.(2), Seoane J.c.S.(5), baRRoS M.(5), baRTH M.o.(5)

(1) Universidade federal fluminense, nITeRoI, bRaZIl;(2) Institut de Recherche pour Développement, bonDY, fRance;(3) embrapa agrossilvopastoral, SInoP, bRaZIl; (4) UnIcaMP, caMPInaS, bRaZIl;(5) Universidade federal do Rio de Janeiro, RIo De JaneIRo, bRaZIl

AbstractThe Holocene environmental history of the Saci Lake was reconstructed by multiproxy analysis that includes Total Organic Carbon (TOC) and Nitrogen content (N), isotopic composition and Black Carbon and pollen analysis of a 131 cm core. The 14C dating showed a basal age of 9200 cal years BP and four sedimentary units were identified. Between 131-112 cm a transition from a wetter to a drier climate was characterized by the occurrence of run-off events. Between 112 -81 cm a depositional environment of low hydrodynamic energy was established (Behling & Costa, 2000). In this phase the high values of Black Carbon (BC) and high concentration of pollen type characteristic of grass savannas support the evidence of a dry climate during the mid-Holocene with the lowest average values of total organic carbon, suggesting low lake levels and low values of chlorophyll derivatives indicate a low productivity environment (Einsele et al., 2001; Turcq et al., 2002; Cordeiro et al., 2008). The transition to late-Holocene was marked by wetter conditions with decrease of Black Carbon concentration. The presence of Mauritia-type taxa is probably due to much flooding around the Saci Lake. The values of δ13C and lowest values of δ15N suggest the development of forest cover around the lake in the mid-late-Holocene transition (Meyers, 1997). The transition to the late-Holocene was marked by wetter conditions, marked by the decrease of Black carbon concentration. In this phase the maintenance of the forest cover a slight increase in the Black Carbon accumulation rate was observed, probably due to anthropic activities in the region (Bush et al, 2008). There were variations of the occurrences of run-off and watershed erosion events marked by the presence of sands in the sediment. The cause of this kind of extreme events seems to be linked to changes in climate variability during the Holocene which needed further investigations.

References1. Behling, H., Costa, L.D., 2000. Holocene Environmental Changes from the Rio Curuá Record in the Caxiuana

Region, Eastern Amazon Basin. Quat Res 53: 369-3772. Bush, M.B., Silman, M.R.,. McMichael, C and Saatchi. S. 2008. Fire, climate change and biodiversity in

Amazonia: a Late-Holocene perspective Phil. Trans. R. Soc. B, 363: 1795-18023. Cordeiro, R.C., Turcq, B., Suguio, K., Silva, A.O., Sifeddine, A., Volkmer-Ribeiro, C., 2008. Holocene fires in

east Amazonia (Carajás), new evidences, chronology and relation with paleoclimate. Global and Planetary Change 61: 49-62

4. Einsele G, Yan J, Hinderer M. 2001. Atmospheric carbon burial in modern lake basins and its significance for the global carbon budget. Global and Planetary Change, 30: 167-195,

5. Turcq B, Albuquerque ALS, Cordeiro RC, Sifeddine A, Simoes Filho FFL, Souza AG, Abrao JJ, Oliveira FBL, Silva AO, Capitaneo J (2002) Accumulation of organic carbon in five Brazilian lakes during the Holocene. Sedimentary Geology: 148:319-342

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S14-P-318

COMPOUND-SPECIFIC RADIOCARBON ANALYSIS OF LAKE SEDIMENTS: WHAT CAN THEY TELL US?

BIRKHOLZ A.(1), HaJDaS I.(2), SMITTenbeRG R.H.(3), WacKeR l.(2), baKKe J.(4)(5), beRnaSconI S.M.(1)

(1) Geological Institute, eTH Zürich, 8092 ZÜRIcH, SWITZeRlanD;(2) laboratory of Ion beam Physics, eTH Zürich, 8093 ZÜRIcH, SWITZeRlanD;(3) Department of Geological Sciences, Stockholm University, 10691 STocKHolM, SWeDen;(4) bjerknes centre for climate Research, 5007 beRGen, noRWaY;(5) Department of earth Sciences, University of bergen, 5007 beRGen, noRWaY

AbstractWe present an extensive radiocarbon dataset of macrofossils, Bulk total organic carbon, leaf-wax derived n-alkanes, and soil bacteria-dervied branched glycerol-dialkyl-glycerol-tetraethers (brGDGTs) from lake Lusvatnet sediments and its catchment soils. The lake is located on Andoya, Lofoten, Norway (69°N). This area was deglaciated shortly after the last glacial maximum, a unique feature for Scandinavia.In order to separate molecular organic fossils with an unequivocal terrigenous source from aquatic – derived compounds, a separation scheme of the total lipid extract of the lake sediments was designed. From the soils only GDGTs were isolated. For the isolation and purification of these compounds semi-preparative High-Performance Liquid Chromatography - Mass Spectrometry and preparative capillary Gas Chromatography were used. Radiocarbon dating was performed using an Accelerator Mass Spectrometer interfaced with a gas source, allowing the analysis of very small samples[1].Our age model is based on 14C ages of terrestrial macrofossils and TOC, which were combusted and graphitized for AMS analysis. This model shows that the sediment core dates back to ca. 15 ka cal. BP. Bulk TOC and brGDGTs show slightly older ages than the macrofossils whereas the n-alkanes match the macrofossil ages very well. We will discuss the data in relation to the lake sediment age-depth model, the use of compound-specific radiocarbon analysis (CSRA) for dating purposes and to study the build-up and evolution of soil organic carbon (SOC).

References[1] M. Ruff, et al., Radiocarbon 49 (2007) 307.

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S14-P-319

THE AGE OF PARTICULATE ORGANIC MATTER TRANSPORTED BY RIVERS: INSIGHTS IN THE AMAZON RIVER SYSTEM

MOREIRA-TURCQ P.(1), PeReZ M.(2), abRIl G.(3), beRnaRDeS M.(2), ManDenGo YoGo M.(4)

(1) Institut de Recherche pour le Developpement IRD-GeT, bonDY, fRance;(2) Universidade federal fluminense, nITeRoI, bRaZIl;(3) Université de bordeaux I - ePoc, Talence, fRance;(4) Institut de Recherche pour le Developpement IRD-locean, bonDY, fRance

AbstractRiver and other inland waters constitute an important component of the global carbon cycle and influence the transport and processing of carbon from continents to the oceans and the atmosphere. Several studies show that particulate organic matter (POM) transported by the Amazon River is old because soils are the main source of riverine organic matter. Amazon riverine POM contains a significant quantity of old, non-hydrolyzable, recalcitrant soil organic matter originating from soil transported to rivers via erosion. This suggests that the bulk of the POM transported by the Amazon River was fixed by terrestrial photosynthesis hundreds to thousands of years ago. Most studies point out significant differences in source, composition, and age of organic matter fractions: particulate (coarse and fine) and dissolved. The dissolved fraction seems to be richer in C, more degraded and more recent than the particulate fraction. The coarse particulate organic fraction is mainly composed of tree leaves and vascular plants detritus while the fine particulate organic matter seems to be an association of mineral particles and organic molecules. More recent studies in the Amazon River (e.g., Mayorga et al., 2005) have shown that respiration of contemporary (i.e., less than five-year-old) organic matter is the dominant source of the excess carbon dioxide that drives outgassing in medium to large Amazonian rivers. This discrepancy in the ages of POM and CO2 suggests the occurrence of two superimposed carbon cycles in the system: (i) the transport of an old refractory POM from land to ocean with little or no degradation and (ii) the transport and mineralization in the river of a young and labile POM. We show here, based on 14C data, that the age of particulate organic matter transported in Amazonian waters show temporal and spatial variations at long an annual hydrological cycle. POM from Amazonian Peru rivers is older than those transported in the lower Amazonian basin. During rising water periods the POM transported by the Rivers is older than during falling water periods when the rivers received the fresh and young POM produced in floodplains lakes. These lateral inputs seem to be responsible for a younger age of Amazon organic matter during the falling period. Generally, during this falling period, the corse (>63µm) fraction is younger than the fine (<63µm) fraction.

ReferencesMayorga, E., Aufdenkampe, A.K., Masiello, C. A., Krushe, A.V., Hedges, J.I., Quay, P.D., Richey, J.E. and T.A. Brown (2005), Young organic matter as a source of carbon doixide outgassing from Amazonian rivers, Nature 436, 538-541.

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S14-P-320

SEARCHING OLD CARBON IN PERMAFROST SOILS: IDENTIFYING PROTECTION MECHANISMS

RETHEMEYER J.(1), HÖfle S.(1), MÜlleR c.(2), JoHn S.(1), HeInZe S.(1)

(1) University of cologne, coloGne, GeRManY;(2) Technical University Munich, MUnIcH, GeRManY

AbstractUnderstanding the controlling factors of organic matter storage is critical for the quantification and prediction of carbon fluxes in response to climatic changes. Physical protection of organic matter (OM) such as interaction with mineral particles and aggregate formation is an important mechanism in preventing or reducing the oxidative and microbial decomposition of OM in soils and sediments (Hedges and Oades 1997, Marschner et al. 2008). A variety of physical fractionation methods have been used to study these protection mechanisms mainly in arable and forest soils (v. Lützow et al., 2006). No study has been conducted so far to determine how OM is protected against degradation in Arctic permafrost soils storing vast amounts of organic carbon and being most strongly affected by rising global temperatures. Thawing of permafrost exposes ‘old’, previously frozen organic carbon to microbial decomposition resulting in a significant reduction of this carbon pool (Schuur et al., 2010).We used 14C analysis of OM separated into different density and particle size fractions to identify ‘old’ carbon pools in the active layer thawing during summer and in the uppermost permafrost in the Siberian tundra. The ‘oldest’ OM was found in the still frozen soil layer (bulk soil: 68 pMC) in silt-sized particles (24 pMC, 25-30cm depth), which was the largest fraction but had the lowest organic carbon content. ‘Old’ carbon was also preserved inside soil aggregates (occluded particulate OM, oPOM<20µm: 69 pMC) from the same depth interval. Generally, lower 14C values were determined for size and density fractions from the frozen soil beneath the permafrost table compared to the active layer soil above. OM ‘younger’ than the bulk soil value was stored in the clay fraction containing most of the organic carbon.To gain information on compositional changes in the various density and size fractions separated from differentdepth intervals, we applied elemental and lipid analysis as well as 13C-CPMAS NMR spectroscopy. Preliminary results indicate that OM in the clay and in the oPOM<20µm fraction is most strongly degraded, while oPOM>20 µm and not occluded in aggregates was little transformed.

References1. Hedges, J.I. and Oades, J.M., 1997. Comparative organic geochemistries of soils and marine sediments,

Organic Geochemistry 27, 319–361.2. Marschner, B. et al., 2010. How relevant is recalcitrance for the stabilization of organic matter in soils? Journal

of Plant Nutrition and Soil Science 171, 91–110.3. Schuur, E.A.G. et al., 2009. The effect of permafrost thaw on old carbon release and net carbon exchange

from tundra. Nature 459, 556-559.4. v. Lützow, M. et al., 2006. Stabilization of organic matter in temperate soils: Mechanisms and their relevance

under different soil conditions - a review. European Journal of Soil Science 57, 426-445.

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S14-P-321

SYNCHRONICITY AMAZONIAN DROUGHTS DURING THE HOLOCENE IN RELATION TO CHANGES OF THE GLOBAL CARBON CYCLE

CORDEIRO R.C.(1), TURcQ b.(2), RoDRIGUeS R.(3), SIfeDDIne a.(2), Seoane J.(4), SIMÔeS-fIlHo f.(5), conceIÇÃo M.(1), MoReIRa l.(1), MoReIRa-TURcQ P.(2), MaRTInS G.(1)

(1) Universidade federal fluminense, nITeRÓI, bRaZIl;(2) Institut de recherche pour le développement, bonDY, fRance;(3) embrapa solos, SInoP, bRaZIl;(4) Universidade federal do Rio de Janeiro, RIo De JaneIRo, bRaZIl;(5) conselho nacional de energia nuclear, RIo De JaneIRo, bRaZIl

AbstractSeveral studies have shown that the Amazonia region has recorded intense and prolonged drought events during the middle Holocene and less intense and shorter during the upper Holocene when lake levels and forest biomass increased. Records of these events have been observed at various locations in soils and lake sediments. In other hand from 8000 cal BP until 4000 cal BP, Taylor Dome ice core (Antartica) record showed an increase around 25 ppm of CO2 concentration. This concordance between fire occurrence during the middle Holocene and the increase in CO2 concentration show that the large biomass burning is probably the most effective mechanism explaining the CO2 concentration increase in the atmosphere. Results of charcoal accumulation from lacustrine records and charcoal datations in soils of Amazonia region suggest that fire occurrence during upper Holocene (~1300 cal BP until ~600 cal BP) can explain the 5 ppm anomalies of CO2 increase in the atmosphere. The most effective indicator of the possible connections between the paleoclimatic and changes in the is the quantification of the deposition of charcoal particles and interpretation of lake level. This subject will be. In this study, paleofires records were obtained through the charcoal particle fluxes analysis and the interpretation of the lake level were obtained trough the organic and mineralogical indicators in sediments of lakes surrounded by different vegetation. Analyses in lacustrine sediments cores were made at the following locations in Brazilian Amazon: Lagoa da Pata (AM); Humaitá (AM), Lago do Saci (PA), Carajás N4, (PA); and Caracarana (RO) and reservoirs sediments in an intense land use change region (Alta Floresta, MT). Fires occurrences during the middle Holocene are synchronous with the increment of CO2 detected by ice core study Taylor Dome record. Anomalies in the global carbon cycle (fluctuation between 5 ppm of CO2 demonstrated by Taylor Dome record in the upper Holocene can be related to fire records in many sites. Discrepancy in the chronologies in different sites could be attributed to imprecision in the chronologic models of the records.

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S14-P-322

ORIGINS OF SUBSOIL CARBON

BRÄUER T., GRooTeS P.M., naDeaU M.J., anDeRSen n.

leibniz-laboratory for Radiometric Dating and Isotope Research, KIel, GeRManY

AbstractA 2,000-year chronosequence of soils, developed on estuarine sediments of the Yangtze River around Cixi, China, provided a unique opportunity to compare the effects of paddy management, characterized by alternating flooded and dry phases that create anoxic and oxic conditions in the soil, with those of normal, non-paddy soil development. The rapidly accumulating sediments consist mainly of erosion material of the Yangtze and, initially, are vertically homogeneous with ca. 0.4% organic carbon (OC) and 50 pMC 14C. OC input and turnover under cultivation can thus be followed via its modern, atmospheric 14C signature.Topsoils are well mixed and show a replacement of the original OC on a time scale of decades with simultaneous increases in OC content up to 3.5% in paddy and 1.1% in non-paddy soils. A compacted layer of low permeability under the paddy topsoil, the plough pan, limits export to the paddy subsoil.14C as a tracer for the origin of different types of OC in the subsoil reveals a complex mixture. Fractionation of OC with the standard acid-alkali-acid pre-treatment yields approximately 50% acid soluble fulvic acids, 10 to 20% alkali soluble humic acids, and around 30% insoluble humin. 14C concentrations of the humin fraction are always well below those of OC, while the mobile humic and fulvic acid fractions contain significantly more 14C. This fits with original sediment containing old reworked OC plus fresh material from the time of deposition, and subsequent water transport of fresh OC from the surface. This results in the build up over time of a 14C concentration gradient, decreasing from (near) atmospheric values in the topsoil to values close to those of the original sediment at depth. Reduced OC transport, caused by the plough pan of paddy soils, delays the development of the gradient. Yet, after ca. 300 years also paddy subsoil OC and 14C gradients change only little. Decreasing OC concentrations, accompanying the 14C build-up, document that the observed subsoil OC and 14C values represent a dynamic equilibrium between import, export, and mineralization of recent OC. Fine rootlets and plant remains with 14C concentrations up to 128% of the modern standard, found till far below the plough pan, indicate plant roots and root exudates, as well as downward transport due to animal activity or via soil cracks, as direct sources of subsoil OC and further complicate the dynamic picture of carbon cycling in the subsoil.

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S14-P-323

DETERMINING SOIL ORGANIC CARBON MEAN RESIDENCE TIMES IN TWO STUDY SITES ALONG A LATITUDINAL TRANSECT IN ITALY.

MARZAIOLI F.(1)(2), alDaneSe R.(3), TanDoH J.b.(4)(2), PaSSaRIello I.(2)(4), caPano M.(5)(2), PaPa S.(3), fIoReTTo a.(3), TeRRaSI f.(4)(2)

(1) Second University of naples, caSeRTa, ITalY;(2) InnoVa, centre for Isotopic Research on cultural and environmental Heritage, caSeRTa, ITalY;(3) Dipartimento di Scienze della Vita, Seconda Universita degli Studi di napoli, caSeRTa, ITalY;(4) Dipartimento di Scienze ambientali, Seconda Universita degli Studi di napoli, caSeRTa, ITalY;(5) Dipartimento di Studio delle componenti culturali del Territorio, Seconda Universita degli Studi di napoli, caSeRTa,

ITalY

AbstractSoil Organic Carbon (SOC) represents the most important and long-lived C reservoir for the terrestrial ecosystems. The study of SOC dynamics represents one of the most important issues regarding the evaluation of CO2 raise related climate changes effects and their mitigation strategies. In this framework there are two main points still unsolved:

i) the future role of SOC in terms of source or sink of C under the future climate conditions;ii) the possibility to manage these systems in order to increase the average C sequestering times.

The possible development of CO2 mitigation strategies by means of soil managements requires the acquisition of a deep knowledge about SOC stabilization mechanisms (in Sollins, 1996 sensu), their effects in terms of C mean residence times and their feedbacks with climate. In order to study SOC dynamics (e.g. mean residence times, MRT) avoiding misleading interpretations SOC should be studied as a complex compartment (a cohort of different turnover times C pools) by means of ultrasensitive methodologies capable to detect small changes of the reservoir over relatively short observation periods (if compared to the expected SOC dynamics). Accelerator Mass Spectrometry (AMS), radiocarbon bomb pulse and modeling represent a valid tool to assess directly SOC MRTs attaining high sensitivities. More over it is important to underline how either if SOC MRT should strongly increase with depth and deep soils (>0.2 m) preserve the majority of soil C buffer little is known about the factors controlling the stability of carbon in deep soil layers.

This study examines two beechwood forest sites in Italy over a latitudinal gradient along the Apennines:

i) the Pradaccio site (nearby Parma northern Italy) about 1600 m above mean sea level (msl) with a Mean Annual Precipitation (MAP) of 2600 mm and a Mean Annual Temperature (MAT) of 6°C.

ii) the Laceno site (nearby Avellino southern Italy) about 1600 m above msl with a MAP of 1600 mm and a MAT of 10°C.

Soils (comprised of litter layer) were cored in variable depth intervals, in replicates and pooled together to smooth site dependent variability. Samples underwent a physical/chemical fractionation procedure in order to separate different MRT fractions and analyzed for radiocarbon concentrations by means of the CIRCE AMS system.Radiocarbon data were converted in MRT by means of ad hoc numerical modeling. Observed results were used to:

i) quantify the relative contribution of each C pool and its MRT; ii) evidence site related soil processes;iii) study climate related dependencies of MRTs.

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S14-P-324

A RADIOCARBON DATABASE FOR IMPROVING UNDERSTANDING OF GLOBAL SOIL CARBON DYNAMICS

TORN M.(1), SMITH l.(1), TRUMboRe S.(2), SWanSTon c.(3), naVe l.(4), aGaRWal D.(5), HaRDen J.(6)

(1) berkeley lab and Uc berkeley, beRKeleY, UnITeD STaTeS;(2) Max Planck biogeochemistry, Jena, GeRManY;(3) U.S. forest Service and national Soil carbon network, HoUGHTon, UnITeD STaTeS;(4) University of Michigan biological Station and national Soil carbon network, PellSTon, UnITeD STaTeS;(5) berkeley lab, beRKeleY, UnITeD STaTeS;(6) U.S. Geological Survey, Menlo PaRK, UnITeD STaTeS

AbstractWe report on progress towards the development of a global terrestrial radiocarbon database that will1) compile existing radiocarbon measurements and provide a continuing common repository for new analyses;2) supply ancillary information and simple modeling frameworks for interpreting radiocarbon data;and 3) facilitate or generate synthesis products that provide insight into the dynamic nature of soil carbon under global change. The database will offer query capabilities and the ability to combine data with gridded global attributes, such as local temperature and precipitation, NPP and GPP, and a climate-based decomposition index.Radiocarbon provides critical information for understanding carbon exchanges between soils, the atmosphere, and the hydrosphere. Radiocarbon has been used to demonstrate the importance of short range order minerals in stabilizing organic carbon on millennial timescales. Infiltration of ‘bomb’ radiocarbon indicates the magnitude and nature of the soil carbon response to human impacts on decadal to centennial timescales. Radiocarbon signatures of chemically or physically fractionated soil, or even of specific organic compounds, offer one of the only ways to infer terrestrial carbon turnover times or test ecosystem carbon models. Radiocarbon in microbial biomass or respiration can be a sensitive indicator of relationships between decomposition and vegetation, nutrient availability, or temperature change. Taken together, such measurements can be used to test and parameterize models of soil carbon dynamics at a broad range of spatial scales. Although a wealth of terrestrial radiocarbon observations exists, they are scattered in small data sets held by individual researchers, and have not been compiled in a form easy to use for multi-site analysis, global assessments, or model testing. By synthesizing these datasets, this global database will facilitate research on a number of questions, including:1) What are current patterns of soil carbon dynamics, and what factors influence these patterns?2) What is the sequestration capacity of different soils?3) What are likely impacts of climate change and human land use activities on the soil resource?4) How well do models represent important carbon cycle processes, and how can they be improved? and5) How important are soil minerals as controls of carbon cycling on a range of timescales? This presentation will focus on how synthesis might address these questions and show preliminary patterns.More than 18 data holders have already committed to contributing data, with 14C measurements from six continents that represent nine soil orders, plant and microbial tissues, and respiration fluxes. Our intention is to grow the database, linking with the National Soil Carbon Network and other groups, and to make the database available to a wide community of scientists, thus increasing the global understanding of carbon cycling in soils and terrestrial ecosystems.

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533

S14-P-325

CHARACTERIZING FOSSIL CARBON IN AND EXPORT FROM PERMA-FROST SOILS OF SPITSBERGEN USING COMPOUND-SPECIFIC RADIOCARBON DATING

MOLLENHAUER G.(1), ReTHeMeYeR J.(2), KUScH S.(3)

(1) alfred-Wegener-Institute, bReMeRHaVen, GeRManY;(2) University of cologne, coloGne, GeRManY;(3) Harvard University, caMbRIDGe, UnITeD STaTeS

AbstractPermafrost soils in the circumpolar Arctic regions contain vast amounts of carbon stored as organic matter, which could potentially be mobilized during the climate warming followed by transport and respiration. We studied a small catchment area covered by permafrost soils on the island of Spitsbergen. Total organic carbon (TOC) conventional radiocarbon years (14C yrs BP) in a soil profile of the annually thawed active layer increase with depth from 5800 14C yrs BP in 0 to 30 cm depth to 26000 14C yrs BP at 60-85 cm. However, in this region known for its occurrence of fossil coals, these ages are likely biased by variable relative contributions of fossil coal particles. Compound-specific radiocarbon (CSRA) ages of short-chain (C16) and long-chain (C26 and C28) fatty acids, which are derived mainly from bacteria and recent tundra vegetation, respectively, are substantially younger than TOC, but still reach values between 2280 14C yrs BP for C16 in the uppermost 0-30 cm and 8350 14C yrs BP for C26 fatty acids in the 30-60 cm soil depth interval. Obviously, several different carbon pools contribute to TOC in the soil profile, and carbon turnover is slow. Radiocarbon dating of long-chain (C26-C28) fatty acids recovered from core-top sediments of the river draining the catchment and from shallow water fjord sediments directly off the river mouth yields 14C ages of 10800 and 7900 yrs BP, respectively. As the C16 fatty acids in marine sediments are primarily attributed to marine phytoplankton, its modern age in the marine sediment clearly identifies it as recent sediment, in which old terrestrial plant material is deposited. Apparently, this terrigenous material is buried near shore, as 14C ages of long-chain fatty acids from three core-top sediments recovered from deeper settings in the fjords contain long-chain fatty acids of 2850 to 3700 14C yr co-occurring with modern or very recent short-chain fatty acids. At each location, substantial amounts of older, likely fossil carbon contributes to TOC as attested by bulk sediment radiocarbon ages of 3800 to 7900 yrs BP. Overall our data imply that export of fossil terrigenous organic carbon derived from permafrost soils occurs and is likely to integrate over the annually thawed depth. However, the average age of exported soil-derived organic matter seems to vary between locations, and the oldest age of exported material is observed in a shallow water setting with very high sedimentation rates. This may imply that in recent times covered by the uppermost centimeters of the shallow water sediment, mobilization of older material has already started compared to the time intervals represented by the core-tops of deeper water fjord sediments, which likely accumulate at lower rates. Alternatively, differences in the oxygenation of waters overlying the respective sediments or the length of transport of particles toward the location of sediment deposition may lead to preservation of different signals.

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534

S14-P-326

RADIOCARBON BASED ORGANIC CARBON SOURCE IDENTIFICATION OF SOIL CO2 UNDER SOIL WARMING IN A CULTIVATED ANDISOL

KONDO M.(1), UcHIDa M.(1), KISHIMoTo a.(2), YoneMURa S.(2), WaGaI R.(2), JoMURa M.(3), SHIRaTo Y.(2), SHIbaTa Y.(1)

(1) national Institute of environmental Sciences, TSUKUba, JaPan;(2) national Institute for agro-environmental Sciences, TSUKUba, JaPan;(3) nihon University, ToKYo, JaPan

AbstractUnderstanding the response of soil organic carbon (SOC) to environmental factors is necessary for estimating the potential of soils to sequester atmospheric carbon. The temperature sensitivity of decomposition of the SOC has recently received considerable interest because of its importance in the global carbon cycle and potential feedbacks to climate change. Despite much research, a consensus has not yet emerged on the temperature sensitivity of soil carbon decomposition, because of uncertainty about the complex biological and ecological processes involved in soil organic carbon dynamics, especially the sensitivities of labile and recalcitrant carbon to rising temperature. In order to study the effects of warming on soil carbon dynamics under Asia monsoon climate and soil properties, we designed a field soil warming experiment for an Andisol, the dominant soil type of agricultural lands in Japan. The aim of this study was to assess the sensitivities of recalcitrant carbon to rising temperature using the soil warming experiment. For the heated plots we used two infrared lamps to warm the soil from 150 cm above the ground, and established a feedback ON/OFF control system to keep the soil temperature at 5 cm depth in the heated plots 2 degrees C higher than the non-heated control plot. We measured Δ14C of soil CO2 inthe heated and non-heated plots, which established in a wheat-soybean double cropping field. We also conduct physical and chemical separation of soil samples, and measured Δ14C of bulk soil and isolated factions. In this conference, we will compare respiration Δ14C with Δ14C of isolated SOC factions and discuss the sources of soil respiration.

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535

SESSION 15

ATMOSPHERIC CARBON CYCLE

ConvenersJL Jaffrezo (FRA), I. Levin (DEU)

DescriptionThis session is devoted to the applications of radiocarbon measurements for the understanding of the atmospheric carbon cycles of gases and aerosols. This potentially includes a wide range of applications, from global to regional scale carbon fluxes fingerprinting to process level investigations. The important aspects of sampling and analysis of minute amounts of carbon for radiocarbon measurements as well as measurements with separation techniques between different fractions (e.g. Elemental Carbon, EC and Organic Carbon, OC or gaseous compounds) are also welcome.

Keywordsatmospheric carbon cycle, source apportionment, flux measurements, sampling, separation, and analysis

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536

S15-P-327

LONG-TERM CHANGES OF Δ14CO2 IN THE GLOBAL ATMOSPHERE

LEVIN I.(1), KRoMeR b.(1)(2)

(1) Institut für Umweltphysik, University of Heidelberg, HeIDelbeRG, GeRManY;(2) Heidelberger akademie des Wissenschaften c/o Institut für Umweltphysik, HeIDelbeRG, GeRManY

AbstractMeasurements of the distribution and long-term trends of radiocarbon in atmospheric carbon dioxide have provided invaluable insight into global and regional fluxes within the carbon cycle. While Δ14CO2 has been decreasing almost exponentially in the decades following the 1960s’ atmospheric bomb testing, due to uptake of bomb-produced 14C by the ocean and the terrestrial biosphere, the currently observed Δ14CO2 decrease of about 4‰ per year is almost solely caused by the input of fossil fuel CO2 into the atmosphere. This 14C-free anthropogenic CO2 flux has increased globally by almost 50% compared to 1990, thus raising the atmospheric CO2 burden by more than 4 PgC (1PgC = 1015 gC) or 0.5% per year in the last decade. As the largest share of fossil fuel CO2 is released in the Northern Hemisphere, the north-south CO2 concentration difference also showed a steady increase. However, until recently this increase was not accompanied by a change in the north-south difference of Δ14CO2. This can be partly explained by the fact that in the early 1980s the terrestrial biosphere changed from a net sink of bomb 14C into a net source1, thus compensating the ongoing 14C-depletion by fossil fuel CO2 emissions in the Northern Hemisphere. Only since about 2005 we observe a significantly faster Δ14C decrease in the Northern than in the Southern Hemisphere, and Δ14CO2 is now about 5‰ lower in the Northern Hemisphere than in the South. This coincides with a steep increase of fossil fuel CO2 emissions which changed from about 1% per year growth rate in the 1990s to more than 3% per year in the last decade. The latest Δ14CO2 measurements from the High-Alpine Observatory Jungfraujoch in the Swiss Alps and from Neumayer station at the Antarctic coast will be presented and the feasibility to use recent Δ14CO2 trends as quantitative constraint of fossil fuel CO2 emissions on the global and hemispheric scale will be discussed.

ReferencesNaegler and Levin, J. Geophys. Res. 114, 2009

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537

S15-P-328

RADIOCARBON DETERMINATION OF CARBONACEOUS PARTICLES (ORGANIC CARBON AND ELEMENTAL CARBON) IN PRECIPITATION

ZHANG Y.L.(1)(2)(3), PRÉVÕT a.S.H.(2), WacKeR l.(4), SZIDaT S.(1)(3)

(1) Department of chemistry and biochemistry, University of bern, beRne, SWITZeRlanD;(2) Paul Scherrer Institut (PSI), VIllIGen, SWITZeRlanD;(3) oeschger centre for climate change Research, University of bern, beRne, SWITZeRlanD;(4) laboratory of Ion beam Physics, eTH Hönggerberg, ZURIcH, SWITZeRlanD

AbstractCarbonaceous particles (CP), which comprise the large fractions of elemental carbon (EC) (also called black carbon; BC) and organic carbon (OC), badly affect climate and human health. The concentration and sources of CP in precipitation are important parameters for understanding of the detailed processes of wet deposition which is known to be a key scavenging (removing) process of OC and EC. Radiocarbon (14C) measurements of both EC and OC allow an improvement in carbonaceous aerosol source apportionment, leading to a full and unambiguous distinction and quantification of the contributions from non-fossil and fossil sources. However, such a method has not been applied to the precipitation samples. Here we develop a thermal-optical method with a commercial OC/EC analyzer to isolate water insoluble OC (WISOC) and EC of the filtered precipitation samples. The temperature protocol is optimized to separate OC and EC without interfering fractions with the best possible recovery. For their 14C determinations, CO2 resulting from the sample analysis is transferred to the gas ion source of the accelerator mass spectrometer MICADAS. The concentrations of WISOC and EC as well as their corresponding fraction of modern (fM) in rain/snow samples collected in Bern, Switzerland in 2012 will be measured. And the distinction and qualification of the biogenic and anthropogenic sources of particles in precipitation will be discussed. The techniques described in this study may also be applied to measure CP in surface snow and ice core samples.

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538

S15-P-329

RADIOCARBON DETERMINATION OF DIFFERENT CARBON FRACTIONS IN PM10 AND PM1

ZHANG Y.L.(1)(2)(3), ZoTTeR P.(2), PRÉVÕT a.S.H.(2), WacKeR l.(4), SZIDaT S.(1)(3)

(1) Department of chemistry and biochemistry, University of bern, beRne, SWITZeRlanD;(2) Paul Scherrer Institut (PSI), VIllIGen, SWITZeRlanD;(3) oeschger centre for climate change Research, University of bern, beRne, SWITZeRlanD;(4) laboratory of Ion beam Physics, eTH Hönggerberg, ZURIcH, SWITZeRlanD

AbstractRadiocarbon (14C) offers a unique possibility for unambiguous source apportionment of carbonaceous aerosol particles due to a direct distinction of contemporary and fossil carbon. Various studies have been carried out to characterize the sources of carbonaceous aerosol by 14C analysis. However, much less data have been available in size-segregated particles from the same locationalthough their sources may vary with particle size. In this study, we investigate the fossil and non-fossil contribution to both coarse and fine particles with the thermal-optical analysis (TOA) method which has been recently developed to isolate different carbon fractions of the carbonaceous aerosol for their individual 14C determinations. 14C data in both PM10 and PM1 aerosols collected in Zurich, Switzerland, are presented for the two sub-fractions of TC, organic carbon (OC) and elemental carbon (EC). Furthermore, water-soluble OC (WSOC) and water-soluble OC (WINSOC) are separated from OC to comprehensively investigate the sources of secondary OC (SOA) since WSOC is often considered a proxy for SOA due to the oxidized nature of these species as compared to other organics.

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S15-P-330

RADIOCARBON MEASUREMENT ON TC/OC/EC CARBONACEOUS FRACTIONS OF ATMOSPHERIC AEROSOL AT LABEC

CALZOLAI G.(1)(2), beRnaRDonI V.(3)(4), cHIaRI M.(2), feDI M.(2), lUcaRellI f.(1)(2), naVa S.(2), TacceTTI f.(2), VallI G.(3)(4), VeccHI R.(3)(4)

(1) University of florence, SeSTo fIoRenTIno (fI), ITalY;(2) Infn, floRence, ITalY;(3) University of Milan, MIlan, ITalY;(4) Infn, MIlan, ITalY

AbstractCarbonaceous particles are among the main components of the atmospheric aerosol; they are estimated to have important effects on both human health and environment. The identification of natural, biomass burning and fossil fuel combustion contributions is mandatory for the development of efficient pollution abatement strategies and for the correct assessment of global radiative aerosol effects.14C analysis on the total carbon fraction (TC) of the atmospheric aerosol by accelerator mass spectrometry (AMS) was demonstrated as an effective tool for the evaluation of the contributions from either fossil fuel combustion or modern sources (wood burning, biogenic activity). Anyway, in order to separate the anthropogenic contributions from the natural ones, further analyses are needed, since wood burning is generally anthropogenic.Carbonaceous aerosols consist of soot (elemental carbon, EC) and of a variety of organic compounds (organic carbon, OC), which have different thermal and optical properties. EC is produced only during combustion processes, while OC can be related to combustion processes or to biogenic activity. The use of 14C measurements on the separate OC and EC fractions was proposed as a tool to separate natural and anthropogenic contributions [1]. A key point in the 14C measurements on aerosols is sample preparation, since the separation of the carbonaceous fractions demands special requirements for the sample preparation line and the assessment of proper sample pre-treatment and combustion protocols.At the INFN-LABEC laboratory of Florence (Italy), a new sample preparation line was designed and realized to fulfil all the procedures for the TC, EC and OC separation and sample graphitization. The line was successfully tested for TC by reproducibility, accuracy and background measurements [2].Suitable sample pre-treatment procedures (i.e. filters washing) and thermal protocols were set up for a correct separation of the EC and OC. As concerns EC, it is usually isolated using an oxygen step only. We have proposed a new thermal protocol that includes also an in-He step at high temperature: in our work, this treatment was demonstrated to be more effective in the OC removal. Furthermore, two approaches for the determination of the fraction of modern carbon of OC (fm(OC)) were tested. They are based on the measurement of either fm(TC) and fm(EC) or of the fraction of modern carbon of water soluble (fm(WSOC)) and water insoluble (fm(WINSOC)) organic carbon.Our tests were carried out on samples collected in a heavily polluted area (Milan, Italy) during wintertime. Results obtained in our tests were also used to attempt a preliminary source apportionment in the area using 14C measurements [3].

References[1] Szidat et al. (2006), J. Geophys. Res., 111 D07206[2] Calzolai et al. (2011), Nucl. Instr. Meth. B 260, 203[3] Bernardoni et al., J. Aer. Sc., submitted

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S15-P-331

INPUT OF STABLE ISOTOPE CARBON MEASUREMENTS IN THE SOURCE APPORTIONMENT OF AEROSOLS

PIOT C.(1), el HaDDaD I.(2), beSoMbeS J.l.(3), coZIc J.(1), MaRcHanD n.(4), JaffReZo J.l.(1)

(1) lGGe, SaInT-MaRTIn D’HeReS, fRance;(2) Paul Scherrer Institut - laboratory of atmospheric chemistry, VIllIGen PSI, SWITZeRlanD;(3) lcMe, le boURGeT DU lac, fRance;(4) lcP, MaRSeIlle, fRance

AbstractMore stringent European Union regulations of the fine aerosol mass (PM2.5) will require a better knowledge of emission sources. Carbonaceous matter (organic and elemental carbon), emitted from several primary sources (e.g. biomass burning, fossil-fuel combustion, cooking …) or formed in-situ in the atmosphere (secondary organic carbon; SOC), represents the major fraction of PM. An accurate knowledge of the relative contribution of these different sources to carbonaceous matter is required in order to reduce PM2.5 concentrations. Source apportionment can be addressed using different approaches; in particular the isotopic carbon signature allows a direct and quantitative discrimination between fossil and non-fossil sources of the carbonaceous matter.In this context, chemical characterizations including isotopic measurements of biomass burning emissions from aged and recent biomass and vehicular emissions in tunnel were performed to determine the non-fossil fraction of total carbon in emissions. Notably, modern fraction in emissions of recent biomass is about 105%, confirming the enrichment in 14C of recent biomass emissions and allows correcting ambient measurements.Isotopic measurements were also used in combination with Chemical Mass Balance (CMB) to apportion the sources of carbonaceous matter in two French urban sites: Grenoble in both winter and summer and Marseille in summer. While CMB modeling provides estimates of the contributions from the major primary sources, isotopic measurements allow validating CMB results and distinguishing the origins of the precursors of SOC, the un-apportioned fraction by the CMB. This fraction was found to represent a large part of carbonaceous matter. For example, in Grenoble, in the summer, 83% of organic carbon (OC) mass cannot be attributed to the major primary sources and remains un-apportioned. Radiocarbon measurements suggest that nearly 80% of this fraction is of non-fossil origin, assigned most probably to biogenic secondary organic carbon (BSOC). More examples spanning different types of sites and seasonality will be discussed.

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S15-P-332

OBSERVATIONS OF ATMOSPHERIC RADIOCARBON IN CARBON DIOXIDE AT HATERUMA ISLAND, JAPAN

TERAO Y.(1), MUKaI H.(1), ToHJIMa Y.(1), MaKSYUToV S.(1), UcHIDa M.(2), KonDo M.(2), SHIbaTa Y.(2)

(1) center for Global environmental Research, national Institute for environmental Studies, TSUKUba, JaPan;(2) center for environmental Measurement and analysis, national Institute for environmental Studies, TSUKUba, JaPan

AbstractWe have been conducted monthly air samplings for measurements of atmospheric radiocarbon in carbon dioxide (14CO2) at Hateruma Island (HAT, 24.05ºN, 123.80ºE, 47 m a.s.l.), Japan since 2004. We collected whole air samples using 2.5L glass flasks pressurized to 2.3 atm, and 5L air was used for radiocarbon analysis. The values of Δ14C were measured using Compact Accelerator Mass Spectrometry (CAMS, NEC 1.5SDH) and National Institute for Environmental Studies’ Tandem Accelerator for Environmental Research and Radiocarbon Analysis (NIES-TERRA). Uncertainty in Δ14C measured by CAMS is less than 2‰, which is based on the number of 14C counts and the scatter of 14C/12C ratios during measurements. The reproducibility of CAMS measurements is ±1.4‰ (standard deviation of Δ14C values in a reference air cylinder). The Δ14C values of background maritime air observed at HAT clearly show the seasonal cycle (minimum in March and October and maximum in August) with amplitude of 10‰. The simulation using atmospheric transport model (NIES TM) indicates that fossil fuel CO2 causes seasonal cycle of Δ14C.In HAT we can measure polluted continental air from the East Asia in winter. To capture the high CO2 events of Asian outflow, we installed remote-controlled autosampling system at HAT in 2010. For example, between March 7 and 11, 2010, we observed two events of CO2 enhancement. The Δ14C values in the high CO2 samples were significantly lower than the background level. The Δ14C observations indicate that fossil fuel CO2 contributes 73-83% of CO2 enhancement in the first event and 47-72% in the second event. The simulation suggests that biospheric emissions cause the other part of CO2 enhances. The keeling plot of Δ14C shows the difference between two events clearly rather than that of Δ13C, implying advantage of high precision Δ14C measurements for CO2 source appointment.

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S15-P-333

RADIOCARBON IN ATMOSPHERIC AND SOIL CARBON DIOXIDE IN BRATISLAVA

HolY K., MUlleRoVa M., POVINEC P., RIcHTaRIKoVa M., SIVo a.

comenius University, bRaTISlaVa, SloVaKIa

AbstractCarbon dioxide is produced in soil by the microbial decomposition of the soil organic matter and by the root respiration. Part of carbon dioxide produced in soil is exhaled into the atmosphere and influences, especially in ground-level air, atmospheric CO2 concentrations, as well as 14C levels in CO2. The 14C content in the soil CO2 can be different from the 14C content in the atmospheric CO2 during the year. The results indicate that 14CO2 exhalations from the soil into the atmosphere should be taken into account when precised results of the 14C content in the atmosphere are required. The CO2 exhalation rates from the soil can be derived from the 222Rn and CO2 depth profile measurements, and simultaneously from 222Rn exhalation rate measurements (the CO2 exhalation rates calibrated by 222Rn measurements). This method has some advantages in comparison with the direct CO2 exhalation rate measurement as the disturbance of the 222Rn concentration gradient during the exhalation rate measurement can be practically neglected due to the comparatively large 222Rn relaxation depth, and the direct 222Rn exhalation rate measurement is not disturbed by the above-ground vegetation. It is possible to realize the 222Rn activity measurements with a high precision, and the result of the determination of the CO2 exhalation rate by this method is not influenced by the soil state. In this contribution the results of radiocarbon measurements in the atmospheric CO2 at the Bratislava (Slovakia) station are compared with the measurements of carbon isotopes in the soil CO2. The results of testing of the 222Rn method as a tool for the determination of the CO2 fluxes from the soil are presented as well. We placed accent on the simultaneous measurements of the 222Rn and CO2 depth profiles, as well as on the simultaneous analysis 14C and 13C in collected CO2 samples.

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S15-P-334

LATEST 14C CONCENTRATIONS OF ROCK PLANT LEAF AT THE ALTITUDE OF 5200 M OF MT. CHACALTAYA LOCATED IN LOW LATITUDES AT THE SOUTHERN HEMISPHERE

SAKURAI H.(1)(2), ToKanaI f.(1)(3)(2), KaTo K.(3), TaKaHaSHI Y.(2), SaTo T.(2), TaVeRa W.(4)

(1) Dept. of Physics, Yamagata University, YaMaGaTa, JaPan;(2) Graduate School of Science and engineering, Yamagata University, YaMaGaTa, JaPan;(3) faculty of Science, Yamagata University, YaMaGaTa, JaPan;(4) IIf, Universidad Mayor De San andres, la PaZ, bolIVIa

AbstractThe atmospheric 14C concentrations of 800‰ due to the atmospheric nuclear detonation in 1960s are reducing to less than 80‰ at 2003. The profiles were reported by both the observations of CO2 and the tree rings (Levin and Kromer (2004), Radiocarbon 46(3), 1261-1272, Rakowski et al. (2008), J. environmental radioactivity 99, 1558-1565). Also, Hua and Barbetti indicated that the seasonal positions of Intertropical Convergence Zone (ITCZ) affected on the difference of 14C concentrations for the bomb peak period between the Northern and Southern hemispheres (JGR vol.112, D19120) using tree-ring data. At moment, the 14C concentrations are showing similar value between both the hemispheres implying well mixing globally in the atmosphere for both the stratosphere and the troposphere.Although, however, we have the 14C concentrations at high altitude in the Northern hemisphere by Jungfraujoch station (3450 m asl), there is no data at high altitude in the Southern hemisphere. First of all, hence, we have measured the 14C concentrations of rock plant leaf growing at Mt. Chacaltaya (16.34° S, 68.12° W, 5200 m). Since the sampling site is located in top of mountain with very high altitude and near to tropical region in the Southern hemisphere, we might be able to look at influence of the seasonal positions of Hadley cell and ITCZ in the 14C concentrations. The plant samples were picked at three altitudes 4000 m, 4800 m, 5200 m, respectively, on November 2011. To compare the 14C concentrations with those at middle latitude in the Northern hemisphere, we picked Japanese plant at Yamagata (38.25° N, 140.35° E, 1300 m) by same month.The plant leafs were treated by AAA after rinse by acetone. The 14C concentrations were measured with the new Compact AMS at Yamagata University (Tokanai et al. (2011), AIP conf. Proc. 1336, 70-74 ). The 14C concentrations were 45.1‰ and 44.1‰ with the error of 2.8‰ at Chacaltaya and Yamagata, respectively.We will describe comparison between the 14C concentrations and the published data sets of Bomb profiles for the CO2 and the tree rings at 2011. Moreover, we will discuss the altitude dependence of the 14C concentrations, considering the production due to cosmic rays and urban effects.

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S15-P-335

MEASUREMENT OF FOSSIL FUEL CARBON DIOXIDE AND OTHER ANTHROPOGENIC TRACE GASES FROM MEGAPOLI INTENSIVE CAMPAIGN IN PARIS DURING WINTER 2010

LOPEZ M.(1), ScHMIDT M.(1), DelMoTTe M.(1), GRoS V.(1), MonDelaIn D.(2), leHMan S.J.(3), RaMoneT M.(1), VUIlleMIn c.(1), XUeRef-ReMY I.(1)

(1) lSce, cea-cnRS-UVSQ, GIf-SUR-YVeTTe, fRance;(2) lPMaa, cnRS, PaRIS, fRance;(3) InSTaaR, University of colorado, boUlDeR, UnITeD STaTeS

AbstractThe Paris agglomeration is the third biggest megacity in Europe (12 million inhabitants) and according to national emission inventories, is responsible for 15 % of the French anthropogenic CO2 emissions mainly originating from road transport, and residential and industrial energy consumption. The objective of our feasibility study was to design an efficient monitoring strategy in order to quantify future trends in anthropogenic CO2 emission in Paris area. During the winter campaign of the European project MEGAPOLI and French project CO2-MEGAPARIS, we performed measurements of CO2 and related trace gases from January to February 2010. The RAMCES (Atmospheric Network for Greenhouse Gases Monitoring) team at LSCE monitored CO2 and CO mixing ratio with high temporal resolution using instruments based on Cavity Ring Down Spectroscopy (CRDS) in the thirteenth arrondissement of Paris (south). We also sampled air in more than fifty flasks covering three full days at the same place. Flask were analysed in the RAMCES central laboratory with a Gas Chromatograph system for CO2, CO, CH4, N2O, SF6 and H2 mixing ratios and also by Mass Spectroscopy for CO2 isotopic ratios (δ13C and δ18O). In order to quantify the fossil fuel CO2 (CO2ff) most flasks were analysed at INSTAAR for Δ14C in CO2. In addition, 13CO2 isotopic ratio and total CO2 concentration were measured at high temporal resolution (< 1 min) over three days at Paris with the SIMCO instrument developed at LPMAA. In parallel with the Paris measurements, in-situ CO2, CO and other trace gases were monitored at Gif-sur-Yvette, a semi urban station 20km south west of Paris and also at the Trainou tower, 100 km south of Paris. Similar synoptic variations of CO2 and CO mixing ratios were found in Paris and Gif with maximum mixing ratio up to 495 ppm CO2 and 1000 ppb CO downtown Paris. The mean diurnal variation during this winter period shows a peak to peak amplitude of 15 ppm CO2 and 150 ppb CO at Paris and 10 ppm CO2 and 40 CO ppb at Gif station. Using the MEGAPOLI database we will test different tracers (CO, VOCs, NOx) as possible candidate to quantify CO2ff (fossil fuel) based on calibration of these tracers against CO2ff estimates based on Δ14C. These results from the campaign will be compared to the emission inventories from EDGAR 4.2 (global inventories) and the national ones from CITEPA and AirParif.

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S15-P-336

INTERCOMPARISON OF 14C ANALYSIS OF CARBONACEOUS AEROSOLS

SZIDAT S.(1)(2), bencH G.(3), beRnaRDonI V.(4), calZolaI G.(5), cHIaRI M.(5), cZIMcZIK c.(6), DeRenDoRP l.(7), DUSeK U.(7), elDeR K.l.(8), feDI M.e.(5), GenbeRG J.(9), GUSTafSSon Ö.(10), KIRIlloVa e.(10), McnIcHol a.P.(8), PeRRon n.(11)(9), SanToS G.M.(6), STenSTRÖM K.(9), SWIeTlIcKI e.(9), USHIDa M.(12), WacKeR l.(13), ZHanG Y.(1)(2)(11), PReVoT a.S.H.(11)

(1) Department of chemistry and biochemistry, University of bern, beRn, SWITZeRlanD;(2) oeschger centre for climate change Research, University of bern, beRn, SWITZeRlanD;(3) center for accelerator Mass Spectrometry, lawrence livermore national laboratory, lIVeRMoRe, ca, UnITeD STaTeS; (4) Department of Physics, Università degli Studi di Milano and Infn (Istituto nazionale di fisica nucleare), MIlan, ITalY; (5) Infn, floRence, ITalY;(6) earth System Science Department, University of california, IRVIne, ca, UnITeD STaTeS;(7) IMaU (Institute for Marine and atmospheric Research Utrecht), Utrecht University, UTRecHT, neTHeRlanDS;(8) noSaMS/Department of Geology and Geophysics, Woods Hole oceanographic Institution, WooDS Hole, Ma, UnITeD STaTeS;(9) Department of Physics, lund University, lUnD, SWeDen;(10) Department of applied environmental Science, Stockholm University, STocKHolM, SWeDen;(11) Paul Scherrer Institut, VIllIGen-PSI, SWITZeRlanD;(12) environmental chemistry Division, national Institute for environmental Studies (nIeS), TSUKUba, JaPan;(13) laboratory of Ion beam Physics, eTH Hoenggerberg, ZURIcH, SWITZeRlanD

AbstractThe carbonaceous aerosol (total carbon, TC) as a major fraction or air-borne particulate matter (PM) adversely influences human health and the climate system. It consists of organic carbon (OC), i.e. colorless and non-refractory substances of low molecular mass, and elemental carbon (EC; also denoted as black carbon, BC), i.e. optically absorptive and recalcitrant polymers [1]. In spite of its general environmental importance, the understanding on sources and formation processes of the carbonaceous aerosol is still low. Here, 14C analysis provides a powerful distinction of fossil from non-fossil emissions, as the former is extinct in radiocarbon whereas the latter shows a 14C/12C signal slightly above the contemporary level [2].In this work, we present results from an intercomparison of 8 laboratories for 14C analysis of carbonaceous aerosol samples on quartz fiber filters. Two ambient samples were collected at an urban and a rural station in Northern Italy and provided with a representative filter blank. Furthermore, NIST RMs 8785 (air particulate matter on filter media) and 8786 (filter blank for RM 8785) were chosen aiming at the assessment of isotopic information values for these reference materials. All 8 laboratories performed 14C determinations of TC and, moreover, a subset isolated EC for isotopic measurement. Applied sample masses ranged from small (<20 µgC) to large (>500 µgC) sizes. In general, 14C measurements of TC agreed reasonably well between the laboratories, whereas the analysis of EC revealed a major deviation as a consequence of different separation techniques.We are grateful to J.-P. Putaud (JRC Ispra) for collection of ambient aerosol samples and G.A. Klouda (NIST) for providing SRM 8785 and 8786.

References[1] U. Pöschl, Angew. Chem. Int. Ed., 7520-7540 (2005).[2] L.A. Currie, Radiocarbon, 42, 115-126 (2000).

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S15-P-337

RADIOCARBON CONCENTRATION IN ANNUAL TREE RINGS FROM SALAMANCA REGION, CENTRAL SPAIN

RAKOWSKI A.(1), naKaMURa T.(2), PaZDUR a.(3)

(1) leibniz-laboratory for Radiometric Dating and Isotope Research, KIel, GeRManY;(2) center for chronological Research, nagoya University, naGoYa, JaPan;(3) Institute of Physics, Silesian University of Technology, GlIWIce, PolanD

AbstractNew results of carbon isotopic composition from tree rings have been analyzed. Δ14C and δ13C data, representing isotopic composition of carbon in “clean air”, were obtained from annual rings of a pine tree (Pinus pinea) taken in Salamanca region in central Spain.α-cellulose was extracted from all samples. Radiocarbon concentration in each annual ring was measured using AMS at the University of Nagoya and stable isotopic composition of carbon was determined using IRMS. The dataset cover a growth period between 1985 and 2007.Those results were use to calculate cfoss component in the city center of Valladolid. By fitting exponential and linear functions to the experimental data, the exchange time was calculated, and the expected future 14C concentration in the atmosphere was estimated.

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S15-P-338

ATMOSPHERIC MEASUREMENTS OF RADIOCARBON IN CO2 FROM THE SCRIPPS CO2 PROGRAM’S GLOBAL NETWORK

GRAVEN H.(1), GUIlDeRSon T.(2)(3), KeelInG R.(1)

(1) University of california - San Diego, la Jolla, UnITeD STaTeS;(2) lawrence livermore national laboratory, lIVeRMoRe, UnITeD STaTeS;(3) University of california - Santa cruz, SanTa cRUZ, UnITeD STaTeS

AbstractSamples of atmospheric CO2 collected by the Scripps CO2 Program at seven global sites were measured for Δ14C with high precision at the Lawrence Livermore National Laboratory. The observations, which span 2- to 16-year periods ending in 2007, contribute significantly to the amount and spatial coverage of atmospheric data that is available for the recent period. Decreasing trends of roughly 5‰ yr-1 in Δ14C are observed, consistent with simple models of the influence on atmospheric Δ14C from exchanges with the ocean, terrestrial biosphere and stratosphere, from natural and anthropogenic 14C production and from 14C-free fossil fuel CO2 emissions. Comparison to previous measurements (Meijer et al. 2006; Levin et al. 2010) reveals a shift in the interhemispheric gradient of Δ14C since the 1980s, similar to the shift observed by Levin et al. (2010). The main cause of the shifting interhemispheric gradient is likely to be a weakening in Southern Ocean uptake of 14C over this period. The 16-year record at La Jolla also exhibits significant interannual variability in the trend and seasonal cycle of Δ14C. This presentation will summarize the work of Graven et al. (2012ab), highlighting the new atmospheric data that is available to the community.

References1. H. Graven, T. Guilderson and R. Keeling 2012a, Observations of radiocarbon in CO2 at La Jolla, California,

1992-2007: Analysis of the long-term trend, J. Geophys. Res.,117, D02302, doi:10.1029/2011JD016533.2. H. Graven, T. Guilderson and R. Keeling 2012b, Observations of radiocarbon in CO2 at seven global sampling

sites in the Scripps flask network: Analysis of spatial gradients and seasonal cycles, J. Geophys. Res.,117, D02303, doi:10.1029/2011JD016535.

3. I. Levin et al. 2010, Observations and modeling of the global distribution and long-term trend of atmospheric 14CO2, Tellus, 62B, 26-46, doi: 10.1111/j.1600-0889.2009.00446.x.

4. H. A. J. Meijer, M. H. Pertuisot, and J. van der Plicht 2006, High accuracy 14C measurements for atmospheric CO2 samples by AMS, Radiocarbon, 48(3), 355–372.

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S15-P-339

FOSSIL FUEL CO2 ESTIMATIONS AT A RURAL STATION IN NORTHERN FRANCE (TRAINOU TOWER, ORLEANS FOREST) BASED ON INTEGRATED 14CO2 MEASUREMENTS AND HOURLY CO AND CO2 OBSERVATIONS

SCHMIDT M.(1), loPeZ M.(1), RaMoneT M.(1), leVIn I.(2)

(1) lSce, GIf-SUR-YVeTTe, fRance;(2) Institut für Umweltphysik, HeIDelbeRG, GeRManY

AbstractAtmospheric CO2 measurements at rural and urban stations are influenced by anthropogenic fossil fuel as well as biogenic CO2 emissions. To quantify both, the anthropogenic fossil fuel and the biogenic CO2 fluxes at a measurement station it is necessary to separate both signals. High precision atmospheric 14CO2 measurements allow to quantifying the CO2 emitted by fossil fuel combustions, as oil, natural gas and coal do not contain 14CO2.Here we will present three years of integrated 14CO2 measurements at a rural station, Trainou Tower (47°58’N, 02°06’E, 131 m asl ) in the forest of Orleans, about 100 km south of Paris. The 14CO2 samples are collected from the 180m air inlet line integrated over 14 days. Parallel, high frequency mole fractions of CO2 and CO are analyzed at the station as it was shown that CO is a good (alternative) tracer for fossil fuel CO2, when calibrated against 14CO2 measurements. Here, we use the biweekly integrated 14C-based fossil fuel CO2 (CO2FF) and the corresponding CO offsets from clean background air to calculate seasonal ratios of CO/CO2(FF). These ratios can then be applied to the high frequency CO measurements to derive hourly CO2(FF) time series. The resulting time series will be compared to CO2 (FF) determined with the chemistry-transport model CHIMERE and to ratios of CO/CO2 (FF) estimated from emission inventories.

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S15-P-340

OBSERVATIONS OF ATMOSPHERIC 14CO2 AT THREE TALL TOWERS IN THE CONTINENTAL UNITED STATES

LAFRANCHI B.W.(1), MIlleR J.b.(2)(3), leHMan S.J.(4), anDReWS a.e.(2), DlUGoKencKY e.J.(2), MIlleR b.R.(2)(3), MonTZKa S.a.(2), PeTRon G.(2)(3), TURnbUll J.c.(5), TanS P.P.(2), GUIlDeRSon T.P.(1)

(1) lawrence livermore national lab, lIVeRMoRe, UnITeD STaTeS;(2) noaa/eSRl, boUlDeR, UnITeD STaTeS;(3) cIReS, boUlDeR, UnITeD STaTeS;(4) InSTaaR, University of colorado, boUlDeR, UnITeD STaTeS;(5) GnS Science, loWeR HUT, neW ZealanD

AbstractAtmospheric radiocarbon in CO2 (

14CO2) represents an important observational constraint on emissions of fossil-fuel derived carbon into the atmosphere, facilitating carbon cycle studies and the validation of fossil fuel emissions inventories. For these purposes, sampling of whole air for 14CO2 is underway at 8 tall towers in the continental United States, part of the NOAA/ESRL Global Monitoring Division tall tower network. Here we present an overview of 14CO2 observations across 1.5-2 years, from 3 of these towers: one outside of Denver, Colorado (BAO; 40.05°N, 105.01°W), one in northern Wisconsin (LEF; 45.94°N, 90.27°W), and a third in northern Maine (AMT; 45.03°N, 68.68°W). Whole air samples were collected at each site 2-3 times per week and analyzed for 14C by accelerator mass spectrometry (AMS). The 3 sites each have distinguishing features providing a unique case study for testing the utility of 14CO2 observations across different continental regions experiencing a range of anthropogenic vs biogenic and near-field vs far-field factors, thus representing a large spectrum of conditions under which 14CO2 observations are expected to be used to infer surface fluxes.In this study we will explore a range of issues related to the use of 14CO2 observations to partition variability of CO2 mixing ratios into its biogenic and fossil components for better understanding surface-atmosphere exchange of CO2 and other trace gases important to air quality and climate change, including CH4, N2O, C2H2, CO, a suite of halo-carbons, and SF6. We will focus our analysis on understanding the regional differences of emissions and surface exchange in relation to those predicted by bottom-up inventories such as Vulcan, Edgar, US NEI, and Carbon Tracker. We will also explore a number of ancillary issues related to understanding the geographical differences in surface fluxes through 14CO2 observations, such as: selection of background reference sites, the influence of photochemistry, and the influence of CO2 respiration from older soil carbon pools.

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S15-P-341

RESULTS OF AN INTER-COMPARISON OF AMS-BASED ATMOSPHERIC 14CO2 MEASUREMENTS

MILLER J.(1), leHMan S.(2), WolaK c.(2), DUnn G.(3), GRaVen H.(4), KeelInG R.(4), MeIJeR H.(5), SMITH a.(6), allISon c.(7), SoUTHon J.(8), XU X.(8), naKaZaWa T.(9), naKaMURa T.(10), GUIlDeRSon T.(11), lafRancHI b.(11), MUKaI H.(12)

(1) noaa earth System Research laboratory, boUlDeR, UnITeD STaTeS;(2) University of colorado, boUlDeR, UnITeD STaTeS;(3) Palo alTo, UnITeD STaTeS;(4) Scripps Institution of oceanography, la Jolla, UnITeD STaTeS;(5) Univeristy of Groningen, GRonInGen, neTHeRlanDS;(6) anSTo, lUcaS HeIGHTS, aUSTRalIa;(7) cSIRo, aSPenDale, aUSTRalIa;(8) University of california, IRVIne, UnITeD STaTeS;(9) Tohuku University, SenDaI, JaPan;(10) nagoya University, naGoYa, JaPan;(11) lawrence livermore national laboratory, lIVeRMoRe, UnITeD STaTeS;(12) national institute for environmental Studies, TSUKUba, JaPan

AbstractWe present results from three rounds of an international inter-comparison of atmospheric 14CO2 measurements. Seven pairings of radiocarbon preparation and AMS laboratories measured the radiocarbon content of CO2 in whole air that was transferred from high pressure cylinders into duplicate, triplicate or quadruplicate air sampling flasks typically employed by the participating groups. One cylinder (FARI-A) had near ambient concentrations of CO2 and 14C of ~380 ppm and 50 per mil, respectively, while the second cylinder (FARI-B) was spiked with fossil CO2 to create a cylinder with CO2 and 14C of ~420 ppm and -30 per mil. The construction of the inter-comparison (which we expect to be ongoing) allows us to test the measurement accuracy of each group; their measurement precision (as defined by the reproducibility from the multiple flasks); and the longterm stability of measurements based on consistency of results between inter-comparison rounds. The large scope of atmospheric observing programs, combined with the relatively high cost and labor-intensiveness of 14CO2 measurements calls for data from different laboratories that can be combined with substantial assurance that spatial and temporal gradients are geophysical and not the result of inter-laboratory measurement artifacts. This laboratory inter-comparison is a first, critical step on that quality assurance path.

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SESSION 18

COSMOGENIC NUCLIDES

ConvenersD. Fink (AUS), S. Ivy-ochs (CHE), A.J.T. Jull (USA), W. Zhou (CHN)

DescriptionThis session will highlight new developments and improvements to cosmogenic radionuclide measurements (14C, 10Be, 26Al, 36Cl, etc). In the last 25 years, the development of measurements of cosmogenic nuclides produced in situ has gone from a simple idea to a wide variety of applications. The development of in-situ 14C is an excellent example. There are also related studies such as atmospheric 10Be in marine and non-marine sediments. In parallel, there has been a development of long-lived nuclear tracers, such as 129I for a rather different application of oceanic tracer studies.Themes:• Advances in in situ 14C techniques; • Applications of in situ 14C produced in terrestrial, extraterrestrial and ice samples • Improved chemical procedures in sample preparation and AMS measurements related to cosmogenic-nuclide studies. • Exposure dating of rock surfaces and sediment using cosmogenic nuclides; • Dating of soil and loess deposits using atmospheric 10Be • New applications including basin-wide erosion rate determinations, weathering and soil burial ages. • Archaeological applications of in situ cosmogenic nuclides. • Marine tracers

Keywordscosmogenic 14C, cosmogenic radionuclides, surface exposure dating, erosion, burial

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S18-P-342

14C, 13C AND 10Be IN FALLING DUST ON APRIL 16 ~ 17, 2006 IN BEIJING

SHEN C.(1), YI W.(1), DInG P.(1), WanG n.(2), DInG X.(3), fU D.(3), lIU K.(3), Wen W.(1)

(1) Guangzhou Institute of Geochemistry,chinese academy of Sciences, GUanGZHoU, cHIna;(2) Department of earth Science, Hongkong University, HonGKonG, cHIna;(3) State Key laboratory of nuclear physics and Technology, Peking University, beIJInG, cHIna

Abstract10Be,14C and δ13C in the dust fall samples collected on April 16 ~ 17, 2006 in Beijing are analyzed. Results show that the content of 10Be in the falling dust ranges from 1.69 atoms / g to 2.07×108 atoms / g, δ13C value of black carbon varies between -23.15‰ and -23.80‰, and δ13C value of total inorganic carbon (TIC) fluctuates between -5.40‰ and -6.00‰. All these values are close to that of the corresponding components in loess. The dust fall in Beijing this time likely originate from loess. Different 14C ages of black carbon in the dust fall, which can represent the real 14C ages of the loess strata the dust fall originated, could be divided into two intervals: 4200-5200yr BP and 3000-4000yr BP, reflecting two different sources of the dust fall or the same source but from various depth. 14C ages of TIC are obviously older than that of black carbon, because 14C ages of TIC are determined by the mixture of primary and secondary carbonates in dust fall. A 14C-Secondary Carbonate model has been built to calculate the ratio of the secondary carbonate to total carbon in dust fall which could be used as an indicator of soil moisture of the dust fall sources. The ratio ranges from 50% to 64% for the dust fall investigated in this paper.

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S18-P-343

EVALUATING STORAGE OF COLLUVIUM IN ALPINE HEADWATERS WITH COSMOGENIC IN SITU 10BE AND IN SITU 14C

KOBER F.(1), HIPPe K.(2), SalcHeR b.(1), IVY-ocHS S.(3), KUbIK P.W.(3), cHRISTl M.(3), WacKeR l.(3)

(1) Institute of Geology, ZÜRIcH, SWITZeRlanD;(2) Institute of Geochemistry and Petrology, eTH Zürich, ZÜRIcH, SWITZeRlanD;(3) Institute of Ion beam Physics, eTH Zürich, ZÜRIcH, SWITZeRlanD

AbstractCosmogenic nuclides (e.g.,10Be) are widely used to obtain catchment wide denudation rates in alpine settings using quartz from modern stream samples. While a single nuclide requires the assumption of steady state and thus infinite time to calculate denudation rates, using a second nuclide will supply this information, which then allows to check steadiness of exposure and erosional processes. Commonly 10Be has been applied along with 26Al, however, both have long half-lives and are therefore insensitive to short-term processes (sediment storage, climate fluctuations) that occur in Alpine settings. We applied 10Be in concert with in situ 14C, to take advantage of the short half-life of 14C (see method and analytical details in Hippe et al., this conference). Preliminary data from an Alpine catchment in Central Switzerland that is dominated by episodic processes (debris flows) indicate, that in situ 10Be and in situ 14C concentrations do not match a similar isotopic steady state history. Due to the fact that several in situ 14C concentrations are lower compared to the 10Be concentrations, we argue that this has been caused by intermittent storage of sediment (and thus decay of 14C). Such storage units are talus and debris flow cones, colluvial slopes and glacial deposits. The material of these deposits was first exposed on hillslopes and cliffs prior to storage, and were then mobilized with this inherited concentration by the debris flows. Therefore, 14C concentrations cannot be unambiguously interpreted as denudation rates. In contrast 10Be concentrations do reflect the denudation rate signal, a rather paleodenudation rate signal. In combination in situ 10Be and 14C yield burial times, that can be interpreted as sediment storage times of at most a few thousand years. This highlights the fact that the in situ 10Be and 14C pair is a powerful tool for analyzing storage segments and times.Stored sediment places a significant natural hazard in alpine settings that is commonly mobilized during thunderstorms in landslide or debris flow events causing flooding and ponding in major valleys. Furthermore, release and mobilization of stored colluvial sediment will be enhanced by the postulated climate change and global warming trends. These trends affect alpine landscapes heavily by permafrost thawing. The magnitude and frequency of debris flow and landslide hazard occurrences are crucial to know for the prediction of future hazards.

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S18-P-344

DIP DIRECTION CONTROLS OF BEDROCK ON CHANNEL MORPHOLOGIES AND DENUDATION RATES IN THE EASTERN SWISS ALPS

BEKADDOUR T.

bern University, beRn, SWITZeRlanD

AbstractThe bedding orientation of bedrock exerts a prime control on the nature and the rates of sediment transfer on mountainous landscapes. Here, we address one particular situation, landsliding, in which the dip angle of the bedrock is subparallel to the topographic slope. Hillslopes with the opposite situation have no such preconditioning, and will denude through standard mechanisms. The dip slope case is transport limited, with deep-seated landslides of up to tens of km2 large transferring material towards the trunk stream. The opposing valley side is dissected by <150 m deep, supply-limited, bedrock channels.Quantifying these effects is however difficult as surface sediment transfer rates in the dip-slope case may not reflect the depth integrated sliding rate. We approach this problem with multiple methods, morphometric analysis and 10Be derived hillslope and channel denudation rates. We analyse the relationship between upstream size of drainage basins A and channel gradients S. In case where channels are graded and shaping the landscape, then channels gradients S are related to the size to the contributing area A following Flint’s (1974) law: S=ksnA-θ where ksn and θ denote the channels steepness and concavity, respectively. The type, magnitude, and relative contributions of hillslope and channel processes can result in deviations from this relationship, which are readily identified by changes in the concavity and steepness. Accordingly, we calculated these parameters from tributary streams on dip slope and non-dip slope valley sides. Tributary channels on dip-slope valley side are characterized by low concavity ranging from 0.1 to 0.2, and equally display low steepness of approximately 100 m0.9. Streams on the non-dip slope valley side have substantially higher concavity between 0.3 and 0.8 and higher steepness, reaching maximum of ca. 200 m0.9. The high steepness and concavity on non-dip slope valley sides support the interpretation of rapid dissection of the channel network into landscape where low hillslope slip rates allow the channel network to stabilize and actively shape the landscape. This is in contrast to the dip-slope valley side, where low steepness and concavity values suggest that the channel network is continually destabilized by rapid deep-seated landsliding.10Be-derived denudation rates are expected to yield similar distinct relationships between landsliding, fluvial dissection and overall sediment yield.

References1. Flint, J. J. 1974. Stream gradient as a function of order, magnitude, and discharge. Water Resour. Res. 10:969–

973.2. Schwab, M., Schlunegger, F., Schneider, H., Stöckli, G., Rieke-Zapp, D., 2009. Contrasting sediment flux in Val

Lumnezia (Graubünden eastern Swiss Alps), and implications for landscape development. Swiss J. Geosci. 2: 211-222.

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S18-P-345

BERYLLIUM ISOTOPES IN THE DEAD SEA DRAINAGE BASIN AND THE LASCHAMP EXCURSION

BELMAKER R.(1), STeIn M.(2), beeR J.(3), cHRISTl M.(4), fInK D.(5), laZaR b.(1)

(1) Hebrew University of Jerusalem, JeRUSaleM, ISRael;(2) Geological Survey of Israel, JeRUSaleM, ISRael;(3) eaWaG, Swiss federal Institute of aquatic Science and Technology, DUebenDoRf, SWITZeRlanD;(4) laboratory of Ion beam Physics, eTH, ZURIcH, SWITZeRlanD;(5) Institute for environmental Research, australian nuclear Science and Technology organization, MenaI, aUSTRalIa

Abstract10Be (t1/2: 1.39 Ma) concentrations in sediments of lakes with large catchment areas depend not only on the production rate but also on climate related transport and erosion processes. In this study we evaluated the potential use of the annually laminated and accurately dated (by U-Th) lacustrine sediments of the Lisan Formation (deposited from Lake Lisan, the late Pleistocene precursor of the Dead Sea) as a high-resolution production-rate archive of atmospheric 10Be. Lisan sediments comprise of annual pairs of primary aragonite and silty-detritus material that originated from desert dust blown to the lake’s vicinity. 10Be is mainly contained within the detritus laminae, while the aragonite laminae store information on the geochemical-limnological history of the lake. 7Be (t1/2: 53.3 d) was used as a proxy for the recycled 10Be component and was measured in flood suspended load, dust and mud-cracks. The relative contributions of production and climate to the overall 10Be signal were evaluated by measuring the 10Be and chemical compositions of the detritus laminae in intervals representing lake level changes and intervals representing rapid change in the 10Be production (i.e. the Laschamp excursion). Our results demonstrate that during periods in which the 10Be production rate varies moderately the recycled 10Be component is significant. During these periods the 10Be concentration correlates with the combined Al and Fe content (R2 = 0.88) and lake level variations. Yet, during the Laschamp excursion interval (~ 41-40 ka BP), 10Be concentrations show a ~two fold increase (2.98±0.12 – 5.30±0.12 ×108 atoms∙gr-2) that cannot be attributed to the mentioned correlations and possibly reflect the enhanced atmospheric production. Radiocarbon measurements in primary aragonite laminae of the Lisan formation showed a significant Δ14C anomaly (up to ~ 900‰) across the Laschamp interval. We will combine 10Be and radiocarbon data to deduce the non-production fraction of the radiocarbon anomaly.

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S18-P-346

COSMOGENIC 14C AND 10BE IN EXTRATERRESTRIAL MATERIALS

JULL A.J.T.(1), GIScaRD M.D.(2), HUTZleR a.(3), ScHnITZeR c.J.(1), ZaHn D.(1), bURR G.S.(1), McHaRGUe l.R.(1)

(1) University of arizona, TUcSon, aZ, UnITeD STaTeS;(2) Imperial college, lonDon, UnITeD KInGDoM;(3) ceReGe, aIX-en-PRoVence, fRance

AbstractRadionuclides produced by galactic cosmic radiation are useful for understanding both the exposure ages [1] and terrestrial residence ages [2] of meteorites. The terrestrial age, or the terrestrial residence time of a meteorite, together with its exposure history provides us with useful insight into the history of the meteorite. A general observation is that meteorites found in semi-arid and arid environments can survive for long times. Meteorites in arid and semi-arid environments can survive for at least 50,000 yr, beyond the range of 14C. Some meteorites have been reported with over 250,000 yr terrestrial age from these locations, using other radionuclide chronometers [1]. We will show the wide range of terrestrial ages from different environments. The terrestrial age also gives us information which can be applied to studies of infall rates, meteorite distributions, weathering of meteorites and meteorite concentration mechanisms. We would expect that weathering of meteorites and their eventual destruction would be a function of the terrestrial age. In addition, weathering affects trace-element composition [3]. A direct connection of weathering rates to the terrestrial survival times of meteorites was initially shown by Wlotzka et al. [4] and later by Bland et al. [5,6], who were able to correlate degrees of weathering with terrestrial age for chondrites collected in the same area. Terrestrial ages of meteorites have been determined by the concentration of 36Cl, 14C or 41Ca, measured independently or also in combination. With measurement of more than one radionuclide, we can correct for the depth dependence of production rate or “shielding” [1]. At our laboratory, we make measurements of 14C and 14C/10Be. The ratio of 14C/10Be can be used to get better precision on terrestrial ages. We will discuss the application of terrestrial-age measurements to meteorites from desert environments, including polar regions, and their significance for understanding of climatic effects in the region of collection.

References[1] A. J. T. Jull 2006. Terrestrial ages of meteorites. In Meteorites and the early solar system II (eds. D. Lauretta

and H. McSween, Tucson: University of Arizona Press, pp. 889-905.[2] O. Eugster et al. 2006. Irradiation records, cosmic-ray exposure ages and transfer times of meteorites. In

Meteorites and the early solar system II (eds. D. Lauretta and H. McSween, Tucson: University of Arizona Press, pp. 829-851.

[3] A. Al-Kathiri et al. 2005. Meteoritics and Planetary Science 40: 1215. [4] F. Wlotzka et al., 1995. Lunar & Planetary Institute Technical Report 95-02: 72.[5] P. A. Bland et al., 1996. Monthly Notices, Royal Astronomical Society 238: 551.[6] P. A. Bland et al. 2000, Quaternary Research 53: 131

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S18-P-347

COSMOGENIC EXPOSURE DATING THE PRE-COLUMBIAN ARCHAEOLOGICAL STRUCTURES AT TIWANAKU, BOLIVIA

LEVCHENKO V.(1), fInK D.(1), RIVeRa caSanoVaS c.(2), MIfSUD c.(1)

(1) australian nuclear Science and Technology organisation, MenaI, aUSTRalIa;(2) Univesidad Mayor de San andres, la PaZ, bolIVIa

AbstractWe have attempted to use in-situ cosmogenic radionuclides 10Be and 14C to date the construction of vertical pillars from the Kalasasaya Platform within the UNESCO Heritage archaeological site of the ancient city of Tiwanaku, Bolivia. The unique site is located within the altiplano valley of Tiwanaku at 3870 m a.s.l. near the southern shores of Lake Titicaca. The monuments at Tiwanaku were constructed as ceremonial and civic buildings of exceptional precision and quality by an Andean pre-Hispanic civilization, who were precursors of the Inca Empire. The structures are made of andesite and sandstone blocks quarried from sites tens of kilometers distance. The date of construction is basically unknown. Earliest settlement is believed to be ~3,000 to 3,500 years ago and the Tiwanaku Empire probably entered its most powerful phase during the 6-8th century AD. The political dominance of Tiwanaku began to decline in the 11th century, and archeological evidence supports a drought-based empire collapsed in the first half of the 12th century. Radiocarbon dating of construction material and other debris ranges from 300 to 950 AD. At its apogee Tiwanaku is estimated to have extended over an area of as much as 6 km2 and to have housed between 70,000 and 125,000 inhabitants. The most imposing monuments at Tiwanaku are the pyramid temple of Akapana and the intricately carved Gate of the Sun. On the northern side of the Akapana is the Kalasasaya Platform, a large rectangular open temple, believed to have been used as an observatory. The courtyard area is enclosed by a modern reconstructed sandstone block wall with intermediate massive vertical pillars from 4 to 6 meters in height and about a square meter in section, which have remained in their original location. We gained permission to sample ~1.0 kg from the very tops of 3 of these pillars, a number of meter-sized abandoned blocks and carved bedrock from excavation quarries at 4270 m a.s.l., 20 km distance from Tiwanaku, and low-lying upright standing stone blocks at the archaeological site of Kalsana, ~10 km east from Tiwanaku. Results of our AMS 10Be measurements and age determinations will be presented.

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S18-P-348

EXTENT, TIMING AND PALAEOCLIMATIC SIGNIFICANCE OF LATE PLEISTOCENE GLACIATION IN THE HIGH ATLAS, MOROCCO

FINK D.(1), HUGHeS P.(2), fenTon c.(3)

(1) Institute for environmental Research, anSTo, SYDneY, aUSTRalIa;(2) Quaternary environments and Geoarchaeology Research Group, UnIVeRSITY of MancHeSTeR, UnITeD KInGDoM;(3) Geoforschungs Zentrum Potsdam, PoTSDaM, GeRManY

AbstractGlacial geomorphological mapping, 10Be cosmogenic exposure ages of 30 erratics from 3 valley systems and palaeoglacier-climate modelling in the highest peaks of the Atlas Mountains, Morocco (31.1°N, 7.9°W), provides new and novel insights as to the history and evolution of the largest desert region on Earth. The Atlas Mountains display evidence of extensive and multiple late Pleistocene glaciations whose extent is significantly larger than that recognised by previous workers. The largest ice field and valley glaciers formed in the Toubkal massif and here we find 3 distinct phases of glacial advances within the Last glacial cycle. The oldest moraines occurring at the lowest elevations have yielded 10Be ages from 30.5 to 87.3 ka. Five of seven samples from moraines at intermediate elevations gave ages of 13.8 to 24.2 ka (2 outliers) which correlates well with the global Last Glacial Maximum (ca. 22-19 ka) and the last termination. Five erratics from the youngest and most elevated moraines yielded a suite of well peaked exposure ages from 11.1 to 12.9 ka which unequivocally falls within the northern hemisphere Younger Dryas (12.9-11.7 ka) chronosequence. The glacial record of the High Atlas effectively reflects moisture supply to the north-western Sahara Desert and can provide an indication of shifts between arid and pluvial conditions. The low altitude range from 2000-2500 m of the glaciations in all three glacial episodes recorded in the High Atlas indicate that climate was not only significantly cooler than today, but also very much wetter. The new evidence on the extent, timing and palaeoclimatic significance of glaciations in this region has major implications for understanding moisture transfer between the North Atlantic Ocean and the Sahara Desert during Pleistocene cold stages. Glacier advance in the High Atlas during this interval provides insight into the seasonal distribution of precipitation and provides valuable insight into the respective roles of moisture supply from the North Atlantic depressions and the West African Monsoon. This in turn then has important bearing on the strengths of meridional vs. zonal circulation at mid-latitudes during pluvial phases.

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S18-P-349

PRODUCTION OF 14C IN TERRESTRIAL AND STELLAR NUCLEOSYNTHESIS

WALLNER A.(1), bUcZaK K.(2), DIllMann I.(3), feIGe J.(2), KÄPPeleR f.(3), KoRScHIneK G.(4), KRaSa a.(5), leDeReR c.(2), MenGonI a.(6), PaUl M.(7), PloMPen a.(5), ScHÄTZel G.(2), STeIeR P.(2), bIcHleR M.(8)

(1) Research School of Physics and engineering, The australian national University, canbeRRa, aUSTRalIa;(2) VeRa laboratory, faculty of Physics, Univ. of Vienna, VIenna, aUSTRIa;(3) Karlsruhe Institute of Technology (KIT), campus nord, Institut für Kernphysik, Karlsruhe, Germany, KaRlSRUHe, GeRManY;(4) Physik Department der Technischen Universität München, Germany, MUnIcH, GeRManY;(5) european commission, Joint Research centre, Institute for Reference Materials and Measurements, b-2440 Geel, belgium,

Geel, belGIUM;(6) International atomic energy agency, nuclear Data Section, austria, VIenna, aUSTRIa;(7) Racah Institute of Physics, Hebrew University, Jerusalem, Israel, JeRUSaleM, ISRael;(8) atominstitut, Vienna University of Technology, austria, VIenna, aUSTRIa

AbstractA key ingredient to our understanding of terrestrial production rates of 14C but also in stellar nucleosynthesis is the accurate knowledge of the respective cross-section data. 14N(n,p) is the dominat production of 14C in the atmosphere. 13C(n,γ)14C and 14N(n,p)14C act as neutron poisons in s-process nucleosynthesis. Moreover, 14N(n,p) is also of concern in fusion reactors as large quantities might be produced over the life time of a reactor. Interestingly, not much data is available for these reactions.Solid samples were irradiated with neutrons with energies from thermal up to 20 MeV at different neutron producing facilities. After neutron activation the amount of 14C nuclides generated in the samples was quantified by AMS at the VERA (Vienna Environmental Research Accelerator) facility. We will discuss the experimental approach and new data are presented which were found lower than in previous measurements for keV neutrons. At higher neutron energies first experimental data were obtained. Finally, we will also discuss the knowledge of potential terrestrial 14C production from other nuclear reactions.

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S18-P-350

MARINE SEDIMENTS AND BERYLLIUM-10 RECORD OF THE GEOMAGNETIC MOMENT VARIATIONS OF THE 20-50KA INTERVAL

MÉNABRÉAZ L., THoUVenY n., boURlÈS D.

aix-Marseille Université, ceReGe, aIX-en-PRoVence, fRance

AbstractTo reconstruct the cosmogenic nuclide 10Be production variations in the atmosphere from 50 to 20 ka, interpreted as responding to changes in the Earth’s dipole moment (Elsasser et al., 1956; Lal, 1988), we investigated the authigenic 10Be/9Be record of two marine sequences from Portuguese and Papua-New Guinea margins (see Ménabréaz et al., 2011). Mid and low latitude sites were preferred in order to benefit from the most efficient modulation by the magnetospheric shielding. These individual records both fully agree with the 10Be deposition flux recorded in the Greenland ice sheet. They decipher an almost doubling of the 10Be production created by the geomagnetic dipole low associated to the Laschamp excursion at ~41 ka. However, they fail to document any significant 10Be overproduction at the age of the Mono Lake excursion (~34 ka), which do not allow demonstrating its global character. These authigenic 10Be/9Be data were integrated with another 10Be/9Be record (Carcaillet al., 2004) into a 1 ka-averaged marine composite curve. Its remarkable match with the 1 ka-smoothed 10Be deposition flux in Greenland ice cores attests of a global signal and points out the atmospheric redistribution of the 10Be production modulated by the geomagnetic dipole field. A calibration of this composite authigenic 10Be/9Be record with virtual dipole moments, obtained from absolute paleointensity measurements determined on lavas (GEOMAGIA-50 database), allowed reconstructing the dipole moment variations spanning the 20-50 ka time interval. This reconstruction, totally independent from paleomagnetic methods applied to sediments, is further compared to the GLOPIS-75 and SINT-800 relative paleointensity reference records. The presented records of the 10Be atmospheric production also take part to the necessity to supplement the knowledge of the atmospheric Δ14C variations in the interval 30-45 ka BP, during which a discrepancy of about 5500 yr between the 14C and U-Th ages is due to the Laschamp geomagnetic dipole low. This study is funded through the MAG-ORB project ANR- 09-BLAN-0053-01.

References1. Carcaillet, J., D.L. Bourlès, N. Thouveny, and M. Arnold, (2004), A high resolution authigenic 10Be/9Be record

of geomagnetic moment variations over the last 300 ka from sedimentary cores of the Portuguese margin, earth Planet. Sci. lett. 219, 397-412.

2. Elsasser, W., E.P. Ney, and J.R. Winckler (1956), Cosmic-ray intensity and geomagnetism, nature 178, 1226-1227.

3. Lal, D. (1988), Theoretically expected variations in the terrestrial cosmic-ray production rates of isotopes, Soc. Italia. di fisica-bologna-Italy XcV corso, 216-233.

4. Ménabréaz, L., N. Thouveny, D. L Bourlès, P. Deschamps, B. Hamelin, and F. Demory (2011), The Laschamp geomagnetic dipole low expressed as a cosmogenic 10Be atmospheric overproduction at ~41 ka, earth Planet. Sci. lett. 312, 305-317.

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S18-P-351

PALEORAINFALL RECONSTRUCTION ON THE CHINESE LOESS PLATEAU USING 10BE AND MAGNETIC SUSCEPTIBILITY

BECK W.(1), WeIJan Z.(2), cHenG l.(3), KonG X.(2), an Z.(2), QIanG X.(2), WU Z.(2), XIan f.(2), ao H.(2), WHITe l.(3)

(1) University of arizona, Physics and Geosciences Departments, TUcSon, aRIZona, UnITeD STaTeS;(2) State Key laboratory of loess and Quaternary Geology, chinese academy of Sciences, XIan, cHIna;(3) University of arizona, aMS facility, TUcSon, aRIZona, UnITeD STaTeS

Abstract10Be is a cosmogenic nuclide produced in the atmosphere and carried to the ground attached to aerosols, primarily by rain or snow. Its flux to the ground is thus proportional to wet precipitation amount. Here we measure 10Be concentration in Chinese loess using it to reconstruct paleorainfall, which on the loess plateau is mainly related to the summer East Asian Monsoon. This exercise is complicated by three issues:

1) dust recycling,

2) changes in the Earth’s magnetic field intensity, and

3) variations in loess accumulation rate.

Recycled dust carries with it some 10Be that fell to the earth some time in the past, which must be corrected for. Changes in the magnetic field intensity causes changes in the 10Be production rate, which changes the relationship between 10Be flux and rain or snow amount. We correct for both of these using loess magnetic susceptibility. We then use the age/depth relationship to convert the corrected 10Be variations into flux variations related to rainfall amount. Finally we use modern 7Be vs rainfall amount and tropospheric 10Be/7Be ratio to convert loess 10Be paleoflux into quantitative rainfall measurements. Here we use this proxy to determine variations in paleorainfall over the last 600 ka from a loess profile from Luochuan China, and discuss these variations in the context of orbital forcing of the Asian Monsoon system.

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S18-P-352

COMPARING EXPOSURE DATES AND RADIOCARBON DATES FROM GLACIAL SETTINGS IN THE ALPS: WHAT CAN WE LEARN?

IVY-OCHS S.(1)(2), HaJDaS I.(1), aKcaR n.(3), MaIScH M.(2), KeRScHneR H.(4), ScHlÜcHTeR c.(3)

(1) Ion beam Physics, eTH-Hönggerberg, ZURIcH, SWITZeRlanD;(2) Geographisches Institut, Universität Zurich-Irchel, ZURIcH, SWITZeRlanD;(3) Geologisches Institut, Universität bern, beRn, SWITZeRlanD;(4) Institut für Geographie, Universität Innsbruck, InnSbRUcK, aUSTRIa

AbstractSince its application at Alpine sites beginning already in the early 1960s, radiocarbon dating of organic material has experienced wide use in numerous and varied glacially modified sites. This was in concert with both biostratigraphic as well as lithosratigraphic studies. In contrast a much smaller data set has been amassed based on cosmogenic nuclide surface exposure dating of moraine boulders and bedrock, which began only about 20 years ago in the Alps. Here we compare data derived from these two independent dating methods that are from the same or closely related sites. We discuss sites that span the time range from the Last Glacial Maximum to the late Holocene. The information gained from more than one hundred years of mapping of Lateglacial stadial moraines in concert with carefully considered radiocarbon results may allow us to derive cosmogenic nuclide production rates. Based on this unique data set we can evaluate if recently suggested 10Be production rates that are below 4.0 atoms/gram quartz/year (St) fit with the morphostratigraphic relationships and independent dates for Alpine sites. The combination of the two types of data sets allows us to learn not only about isotopic systematics but also to refine our understanding of the timing and pace of climate variations across the Alps.

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SESSION 19

UNUSUAL APPLICATIONS OF 14C MEASUREMENT

ConvenersI. Hajdas (CHE), G. Hodgins (USA)

DescriptionSometimes radiocarbon projects are like detective stories. Often the ‘bomb peak’ is central to such cases, however, measurements of natural radiocarbon levels and admixtures of bomb and fossil C can also provide interesting testimony. We would like to call for papers that utilize either C signal (‘bomb’ or ‘natural’ 14C) to address questions of authenticity or forgery in museum studies, forensic, food, environmental or medical sciences, or other novel applications. Moreover, studies that provide ‘unexpected’ radiocarbon dating results that might lead to new interpretations of historical records would be of interest. We invite papers that present such studies from the whole range of 14C ages and disciplines.

Keywords14C dating, applications, 14C bomb peak, fossil C, authentic, fraud, forensic, environmental, historical, food, medical

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S19-P-353

RADIOCARBON DATING AND AUTHENTICATION OF OBJECTS FROM ETHNOGRAPHIC MUSEUMS

RICHARDIN P., GanDolfo n., boYeR M.

centre de recherche et de restauration des musées de france, PaRIS, fRance

AbstractSince the 15th century, many French explorers have travelled the world to discover new horizons and to extend France to new territories. From their long and hazardous trips, they reported many pieces of material evidence used to support and confirm their regarding on the traditions and customs in these distant lands. All these objects were be collected together in the curiosity cabinets and then in ethnographic museums. In these sometimes very ancient collections, many objects, removed from their archaeological or historical context, have given rise to great interrogations and controversies about their authenticity.This paper describes the contribution of the radiocarbon dating method to the authentication of ethnographic objects on some significant examples coming from the collections of the Musée du Quai Branly (Paris, France). The first one is a bludgeon of hard wood from the ethnic group of Tupinamba and supposed to be brought from Brazil (South America) by Andre Thévet, cosmographer of King Francis the 1st. This object is supposedly dated from the sixteenth century. Another example concerns a series of architectural columns, brought from Peru in 1910 by Captain Paul Berthon and coming from the archaeological site of Pachacamac, the largest sanctuary on the central coast of Peru. These pieces have induced great emotion in the French scientific community, which has described them as «some vulgar fake», because of a particular decoration and also a unique typology. We will present also the dating of two Tibetan textiles and two Pre-Columbian ponchos made with feathers, which were not very documented.Thus, all these examples illustrate the very interesting possibilities and the evident contribution of radiocarbon dating concerning museum objects without any piece of information about their origin.

References1. Lavier C, Borel T, Vigears D. 2009. Traceology applied to wooden artefacts ans works of art in French national

museums: initial examples of adaptations, technical developments and results at C2RMF. Technè 29:15–20.2. Richardin P, Gandolfo N, Moignard B, Lavier C, Moreau C, Cottereau E. 2010. Centre of Research and

Restoration of Museums of France: AMS Radiocarbon Dates List 1. Radiocarbon 52(4): 1689-1700.

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S19-P-354

CHALLENGES IN THE 14C-BASED DETERMINATION OF BIOGENIC FRACTIONS IN FUELS AND FLUE GAS CO2

PALSTRA S.W.L., MeIJeR H.a.J.

University of Groningen, GRonInGen, neTHeRlanDS

AbstractRadiocarbon (14C) has been used from the very beginning as a tracer to distinguish fossil and biogenic carbon fractions in different sample types. This specific application of 14C, which makes use of the differences in 14C abundance between fossil carbon (no 14C) and biogenic carbon (biomass < 200 years old; contains 14C similar to atmospheric values), is therefore not new. However, in recent years the interest for this specific analysis has come up in the field of energy.Fuels and flue gas CO2 samples are relatively new sample types for which the 14C method is used to determine and verify biogenic carbon fractions. This is related to the increasing use of biomass as a replacement fuel for fossil fuels. Financial incentives are given by governments to decrease the use of fossil fuels for different reasons (energy dependency, climate change). Fuel producers, fuel combusting industries and emission authorities have an (financial) interest to know or verify the biogenic/fossil carbon fractions in fuels and CO2 emissions. This requires validated and standardized methods. The 14C method is a promising method and has been described for different fuel types in different papers over the last 15 years. So far, a few standards (American, European) have been developed in which this application of 14C is used for different fuel types (including waste). Several ISO standards are currently under construction. The applicability and reliability of the 14C based method to determine the biogenic carbon fraction depends on the type of sample and its specific characteristics. Challenging factors within the 14C method for fuels and/or flue gas CO2 are:

1) Inhomogeneous biogenic/fossil carbon composition of solid fuel (sub)samples;

2) Variation in 14C reference values for 100% biogenic carbon due to variation in atmospheric 14C values over the last 50 years; and

3) Improper isotope fractionation correction for a mixed fossil + biogenic carbon sample if fossil and biogenic δ13C values differ considerably. Recently, we have investigated the use (application and validation) of the 14C method for flue gas CO2 samples taken at a power plant and a waste incineration plant [1]. Currently, we quantify systematic errors in the calculation method of the 14C-based biogenic carbon fraction if the isotope fractionation correction is not applied properly (point 3) previous section). Since biogas and natural gas have δ13C values that can differ considerably from other fuel samples, we focus in our research on these kinds of samples. We will present our results and show the implications for the accuracy of the determination of the biogenic carbon fraction for the three challenging factors.

References[1] Palstra, S.W.L., and H.A.J. Meijer (2010), Carbon-14 based determination of the biogenic fraction of industrial

CO2 emissions – Application and validation, bioresource Technology, 101, 3702-3710.

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AMS DATING OF EARLY ISLAMIC BOOKS

HIGHAM T.

oxford Radiocarbon accelerator Unit, oXfoRD, UnITeD KInGDoM

AbstractFive books thought on the basis of historical dating to be contemporary with the age of Mohammed have been analysed in Oxford. The booksare in Arabic and appear to all be dated to 11 AH (circa 632 AD) according to a date and signature of Zayed ibn Thabit on each. Zayed ibn Thabit was a scribe who was chosen by Muhammed to write down the words of the Holy Qur’an. He authenticated and collected the Qu-ranic traditions into a single volume which were left with the Caliph Abu Bakr. All of the five volumes appeared initially to be on parchment. They include the first verse of the Holy Qur’an on the cover page.ORAU became involved in the dating of the manuscripts on behalf of a client in Dubai. The pages of each of the five volumes are fused together, we assume from heat over time, so that the contents of each volume is unable to be read other than the cover page. Initial palaeographic analysis showed that the five volumes may have been copied at different times and they may in fact all be copies of an original manuscript that may have been dated 11 AH and also may or may not be a copy of the Holy Qur’an. For this reason it was necessary to radiocarbon date leaves from some of the five volumes separately. Each volume is bound by leather and this was also dated. Initial results disclosed a spread in ages, some of which were of the age expected, and then others that were much later. We did a second larger series of radiocarbon dates which showed a close correlation between the radiocarbon ages and the measured stable carbon isotopes. This, and other information, suggested that the volumes were not genuine.

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ISOTOPIC DIFFERENCES BETWEEN HAIR AND NAILS IN MODERN HUMANS: PRE-TREATMENT INADEqUACY OR NOT?

MARTINEZ DE LA TORRE H., oRMSbY K., SanToS G., fUlleR b.


AbstractIn Forensic Sciences, researchers have investigated the possibility of using radiocarbon (14C) signals from fast turnover tissues, such as hair, fingernails, and blood of modern humans to precisely acquire the year-of-death dates. Hair and nails are of particular interest, because they are formed from keratin, an extremely resilient protein that is insoluble under natural conditions. In addition, upon a criminal investigation, these tissues are easier to obtain, as they do not involve an invasive medical procedure for sampling. Recently, a longitudinal analysis of fingernails and hair from the same infant, collected from 2002 to 2004, were measured and their 14C signals were compared to one another alongside with stable isotope measurements of δ13C, δ15N and C/N (Santos et al. 2011). Interestingly, the Δ14C values of the hair were depleted by at least 10‰ relative to the fingernails, when the stable isotope signals seemed unaffected. Because these samples were chemically pre-treated to remove lipids and shampoo residues prior analyses (O’Connell and Hedges 1999), we determined that the exogenous C contaminants present were not solely external to the hair strands. To investigate the Δ14C values discrepancy, hair and fingernails from different donors as well as shampoo were subsequently measured. Hair and fingernails were offset by at least 8‰ in 14C, when the shampoo returned a bulk age of ~8.8ka yrs BP (Santos et al. 2011). Offsets were larger for hair segments farther from the roots, possibly due to longer exposure to the cosmetic product applied. These preliminary results suggest that sources of C contamination are possibly due to hair care products rather than amino acid composition differences within keratin from hair and nails (O’Connell et al. 2001). In order to determine whether hair can be cleaned of exogenous C contaminants incorporated onto their structure, various chemical treatment processes were undertaken on hair collected from a small group of individuals followed by 14C-AMS measurements coupled with δ13C, δ15N and C/N analysis. Scanning electron microscope (SEM) pictures were also used to identify how the chemical cleaning process affected the hair matrix and structure.

References1. Santos et al. (2011) Can we blame discrepancies of year-of-birth 14C determination on Mom? Preliminary

isotope results of fingernails of breastfed mother-infant pairs, abstract in AMS12, Wellington, New Zealand.2. O’Connell, T.C. and Hedges, R.E.M. (1999) Investigations into the Effect of Diet on Modern Human Hair

Isotopic Values, american Journal of Physical anthropology 108:409–425.3. O’Connell et al. (2001) Isotopic Comparison of Hair, Nail and Bone: Modern Analyses, Journal of archaeological

Science 28, 1247–1255.

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UNDER THE VOLCANO: OLD BONES AT PORTA NOCERA CEMETERY, POMPEII

ZAZZO A., SalIÈGe J.f., lePeTZ S.

UMR 7209 cnRS / MnHn, PaRIS, fRance

AbstractThe original goal of this project was to investigate the link between the social status and diet in the Roman Empire by means of geochemical analyses. More precisely, we wanted to quantify the importance of marine food in the diet of two well-identified social groups: roman citizens and slaves. Archaeological evidence from urban site of Pompeii, as well as in the rest of the Roman Empire, shows that marine food was usual in the diet but probably more specifically restricted to people with a high social status. Archaeological surveys undertaken at the cemetery of Porta Nocera in Pompeii (Lepetz and Van Andringa 2011) gave us the opportunity to sample individuals for which the name, age, date of death and social status was known. Paleodietary reconstruction based on stable isotope analysis was not possible here because most of the individuals were incinerated and collagen was lost. We therefore decided to use 14C dating of the mineral and organic fraction of burnt bones and teeth instead as a tracer for the consumption of marine resources.Eleven individuals dating from the 1st century AD (between 40 and 79 AD for most of them) were sampled. Charcoal and shells found in association with the tombs or the pyre were also dated in order to estimate the local reservoir effect. Charcoal ages (n= 4) ranging between 1960 ± 27 BP and 2328 ± 50 BP suggest an inbuilt age comprised between 0 and 400 yrs. The shells (n= 6) show a very large range in 14C age, from 2400 ± 39 BP to 4035 ± 41 BP. The dated human bones show an even larger age range, between 1805 ± 49 BP and 5570 ± 120 BP. Most of the ages are too ancient to be explained by the MRE only. This unexpected result obfuscated the original paleodietary signal and ruined our original hopes to relate diet and social status. Although never observed before in humans, this pattern had already been observed on plants living at the vicinity of a volcano (Pasquier-Cardin et al. 1999). We propose that these old ages might be due to the influence of CO2 emissions of the nearby Vesuvius volcano and the whole, large Campi Flegrei volcanic system at the Bay of Naples. This “volcano effect” could either have been recorded in vivo (through diet) or post-mortem, during incineration or fossilization. Our data do not allow us to decipher between the different scenarios, but emphasizes the need to be cautious when working in volcanic contexts.

References1. Lepetz S., Van Andringa W. (2011). Publius Vesonius Phileros vivos monumentum fecit: Investigations in a

sector of the Porta Nocera cemetery in Roman Pompeii, in: Carroll, M. & Rempel, J. éd, Living through the dead: Burial and commemoration in the Classical world, Studies in Funerary Archaeology, 5, Oxbow Books: 110-133.

2. Pasquier-Cardin A., Allard P., Ferreira T, Hatté C, Coutinho R, Fontugne M., Jaudon M. (1999) Magma-derived CO2 emissions recorded in 14C and 13C content of plants growing in Furnas caldera, Azores. J Volcano Geotherm Res 92 195–207.

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VOLCANIC HISTORY OF FUGENDAKE IN UNZEN, SW JAPAN

XU S.(1)(2), fReeMan S.P.(1), HoSHIZUMI H.(3), UTo K.(3)

(1) Scottish Universities environmental Research centre, GlaSGoW, UnITeD KInGDoM;(2) Jaea Tono Geoscience center, ToKI, JaPan;(3) Geological Survey of Japan, TSUKUba, JaPan

AbstractUnzen volcano is a large volcanic complex that begun erupting ca. 0.5 Ma ago at the center of the Unzen graben, ca. 70 km west of the volcanic front of SW Japan. The volcanic history of Unzen has been divided into the older and younger stages. The latter principally comprises Nodake, Myokendake, Fugendake and Mayuyama volcanoes. Developed in the Myokendake scar, Fugendake, the largest volcano in Unzen, has produced numerous lavas, pyroclastic flow deposits and debris-avalanche deposits. However, its first eruption is not definitely identified and the observed statigraphy is complicated.To determine the history of the Fugendake volcano 10 charcoals within lavas and pyroclastic flow deposits and 20 soil samples underlying volcanic-related products were radiocarbon-dated. Geological investigations and the radiocarbon results indicate that the eruption of the Fugendake volcano initially occurred ca. 27 ka BP, and produced the Kureishibaru pyroclastic flow deposit at 19 ka BP, the Yuegawa pyroclastic flow deposit at 14 ka BP, the Kenshu Center lava at 10 ka BP, and the Shichimenzan-Tenguyama and FugendakeSancho-Shimanomine-Kazaana lavas and the Mutsugi pyroclastic and Mizunashigawa pyroclastic flow deposits at 4 ka BP. Subsequent historical eruptions include the Furuyake lava at 1663, the Shinyake lava at 1792 and the Heisei lava in 1991~95. The eruption age of the Furue pyroclastic flow deposit, the Taruki-Higashi lava and the Inaoyama lava remain unclear.

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DETERMINATION OF THE RADIOCARBON CONTENT IN DIFFERENT HUMAN TISSUES: IMPLICATIONS FOR THE APPLICATION OF THE 14C BOMB SPIKE DATING IN FORENSIC MEDICINE

CALCAGNILE L.(1), caTTaneo c.(2), QUaRTa G.(1), D’elIa M.(1)

(1) ceDaD, DePT. of enGIneeRInG of InnoVaTIon, UnIVeRSITY of SalenTo, lecce, ITalY;(2) DePaRTMenT of HUMan MoRPHoloGY anD bIoMeDIcal ScIenceS, UnIVeRSITY of MIlano, MIlano, ITalY

AbstractThe large excursion in the atmospheric radiocarbon concentration since ~1950 AD as the result of the atmospheric nuclear detonation tests has been widely used as a powerful tool for the absolute dating of different kind of samples relevant in forensics such as illicit drugs, wines and paper documents. Nevertheless the application of this method for dating human rests with a degree of accuracy making it suitable in forensics is limited by still open issues. In particular the possibility to distinguish weather the measured 14C concentration in a sample corresponds to the rising or to the falling part of the “bomb spike” curve and to properly extrapolate from the measured 14C data the relevant information (such as the year of birth or of death) by taking into account the 14C turnover rate in the different human tissues. In order to address these issues AMS 14C analyses were carried out on different samples taken from different human bodies all born after 1950 AD. In fact the samples submitted to analysis were: hairs, cortical and trabecular fraction of skull bones and the pubic symphysis and enamel extracted from permanent teeth with different timing of formation. The results obtained were different for the different kind of samples, corresponding to the different time of formation of the teeth and of the hairs and to the different rate of re-modelling for the cortical and trabecular bones. The comparison of the obtained results with the known bomb peak curve for the Northern Hemisphere allowed to establish the degree of precision and accuracy with which the year of birth or the year of death can be determined with this method.

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RADIOCARBON AGES OF ORGANIC MATERIALS IN AN ETHNOGRAPHIC CONTEXT IN UZBEKISTAN USING THE “BOMB PEAK”

BOARETTO E.(1), MInTZ e.(1), SHaHacK- GRoSS R.(2), GUR-aRIeH S.(2)(3)

(1) Weizmann Institute of Science, ReHoVoT, ISRael;(2) Kimmel center for archaeological Science, Weizmann Institute of Science, ReHoVoT, ISRael;(3) bar-Ilan University, RaMaT Gan, ISRael

AbstractShort-lived charred organic materials and bone collagen are widely used for high resolution radiocarbon dating in archaeology. There are however at least two underlying assumptions: the radiocarbon date of these short-lived materials reflects the time of burial of the material and hence the age of the stratum, and that the states of preservation and contamination are such that the dates obtained are accurate. In order to test the first assumption, we are carrying out a modern ethnographic study on the radiocarbon contents of organic materials in a traditional village in the region of Samarkand, Uzbekistan. In this village all building materials are traditionally made and no modern technology is involved. We characterized the short-lived materials before dating and documented the oral memory of the local people about times of construction and changes in use of the buildings. We therefore expect the time range of these materials and the buildings should cover the last 60 – 80 years. By using the radiocarbon bomb peak, we should be able to determine very precisely and accurately the actual dates of these materials. This in turn should provide information about the reliability of the oral information, and most important the age distribution of contemporaneous short-lived materials in a village. This information will be of much relevance to interpreting the archaeological radiocarbon record, where it is often tacitly assumed that all preserved short-lived organic remains from a well defined context originate from a very restricted period in time.

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RADIOCARBON MEASUREMENTS ON EARLY PHOTOGRAPHS: METHODS DEVELOPMENT FOR TESTING WAXED PAPER NEGATIVES

CANOSA E.(1), HoDGInS G.(2)(3), WeaVeR G.(4)

(1) Heritage conservation Science Program, Materials Science and engineering, University of arizona, TUcSon, aRIZona, UnITeD STaTeS;

(2) nSf-arizona aMS laboratory, University of arizona, TUcSon, aRIZona, UnITeD STaTeS;(3) School of anthropology, University of arizona, TUcSon, aRIZona, UnITeD STaTeS;(4) Gawain Weaver art conservation, San anSelMo, calIfoRnIa, UnITeD STaTeS

AbstractIn 1840, an early photographic process known as the calotype was developed by William Henry Fox Talbot. Patented in 1841, the calotype was a negative process on a plain paper support, and can be more generically referred to as a paper negative. The process involved treating a good quality writing paper with solutions of potassium iodide and silver nitrate. Other chemicals such as gallic and acetic acids were also added, and there were many variations in the process throughout the 1840s and 50s. The still damp sensitized paper negative was exposed inside a camera. Upon development a negative image was formed within the paper matrix through the light catalyzed precipitation of metallic silver. Paper negatives could be contact printed to produce positive images. It was discovered that the quality of the positive improved if the negative was first impregnated with beeswax or oil to increase its transparency. The process predates the invention of negatives on glass or cellulose-based plastic supports, in which the light sensitive silver salts are contained in a transparent medium, typically gelatin or collodion in the 19th century.The earliest years of photography were full of experimentation and innovation, and a number of well-known photographers carefully documented their experimental procedures. Consequently, it is possible to produce historically accurate waxed paper negatives today. Moreover, modern waxed paper negatives made using 19th century paper can pass for historically significant 19th century negatives and thus pose problems to museums and others interested in studying or collecting authentic 19th century photographic images. We have developed methods for separating and measuring the radiocarbon content of the organic components of waxed paper negatives, as a tool for detecting modern paper negative forgeries. We have focused on the extraction and radiocarbon measurement of the wax component, reasoning that modern forgers might have easy access to 19th century papers, but would less likely use 19th century beeswax.

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CURIOUS AND ‘NOT PUBLISHABLE’ 14C AGES

HAJDAS I., bIecHele c., bonanI G., MaUReR M., WacKeR l.

laboratory of Ion beam Physics, eTH, ZURIcH, SWITZeRlanD

AbstractEvery sample submitted for radiocarbon analyses is treated as an object with an unknown age. Only in few cases there are no expectations or predicated age. Mostly age estimates returned from measurement fulfill the expectations. However, during the last 25 years of the operation of the AMS 14C laboratory at ETH Zurich numerous samples resulted in surprising 14C concentrations. History of those results is an interesting story by itself. Some such as Ötzi the Iceman (Bonani et al. 1994) would inspire new science and become celebrity for school kids. Others such as the Shroud of Turin (Damon et al. 1989) big media discussions about validity of the test. In this presentation less spectacular but interesting objects and cases will be presented. One of the examples is the cherry stone found in the stomach and tissue of a well-preserved dead body found in 1996 in lake Brienz near Interlaken. The 14C ages indicated 19th – beginning of 20th century as a time for the death of that person. These 14C results were never published but ‘Brienzi’ appeared in the news once again when a few years ago casualties of the Swiss military accident could not be found on the bottom of the lake Interlaken.

References1. Bonani, G., Ivy, S.D., Hajdas, I., Niklaus, T.R., and Suter, M., 1994, Ams C-14 Age-Determinations of Tissue,

Bone and Grass Samples from the Otztal Ice Man: Radiocarbon, v. 36, p. 247-250.2. Damon, P.E., Donahue, D.J., Gore, B.H., Hatheway, A.L., Jull, A.J.T., Linick, T.W., Sercel, P.J., Toolin, L.J., Bronk,

C.R., Hall, E.T., Hedges, R.E.M., Housley, R., Law, I.A., Perry, C., Bonani, G., Trumbore, S., Woelfli, W., Ambers, J.C., Bowman, S.G.E., Leese, M.N., and Tite, M.S., 1989, Radiocarbon Dating of the Shroud of Turin: Nature, v. 337, p. 611-615.

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A NEW BAOBAB ARCHITECTURE ASSESSED BY AMS RADIOCARBON DATING: TREES WITH FALSE INNER CAVITIES

PATRUT A.(1), Von ReDen K.f.(2), WooDboRne S.(3), loWY D.a.(4), Hall G.(3), GaRnaUD S.(5), DIaGne T.(6), PaTRUT R.(1)

(1) babes-bolyai University, clUJ-naPoca, RoManIa;(2) noSaMS facility, Woods Hole oceanographic Institution, WooDS Hole, UnITeD STaTeS;(3) natural Resources and the environment, PReToRIa, SoUTH afRIca;(4) flexel, llc, colleGe PaRK, UnITeD STaTeS;(5) Inecoba, aUlnaY-SoUS-boIS, fRance;(6) IUcn, Survial Species commission, RUfISQUe, SeneGal

AbstractIn 2008 we extended the AMS radiocarbon investigation of large angiosperm trees by introducing a methodology, which also allows the dating of standing and live specimens. This approach is based on the dating of very small wood samples, collected mainly from inner cavities and from deep incisions in the trunks of large live individuals, belonging to angiosperm species. As model species, we selected the longest living angiosperm: the African baobab (Adansonia digitata L.) Research performed on the largest individuals from several African countries allowed us to determine their age and growth rate dynamics, but also some new architectures of the investigated trees.Often, Baobabs become hollow at a relatively early age. Most old baobabs have large hollow parts, especially in the central area of their trunks/stems. Trunks/stems are hollowed with major wood removal by decay fungi, large fires, elephant damage, human activity or twisting of large branches. In many old baobabs the cavities have openings toward the exterior, which render them accessible to birds, snakes or other animals and, often, to humans, as well.For samples collected from normal cavities, the sample ages decrease from the cavity walls toward the outer part of the trunk/stem. Occasionally we found, however, that sample ages increase considerably from the inner cavity walls toward the exterior, up to a certain distance into the wood. In such cases, the inner cavities in the trunk of large individuals are in fact false cavities between perfectly fused stems. Hence, false cavities, which are always covered by bark, can form only in multi-stemmed trees and are just empty spaces between several fused stems, disposed in a ring-shaped structure.As the most relevant specimens with false inner cavities, investigated by us, we mention the well-known baobab of Samba Dia (Senegal) (circumference at 1.30 m; cbh = 26.13 m) and the Lebombo Eco Trail baobab (Mozambique) (cbh = 26.13 m). The oldest dated samples suggest ages of 600 years for the baobab of Samba Dia and 1450 years for the Lebombo baobab. In addition to age, AMS dating results indicate that for both trees different stems have different ages and belong to different generations. Hence, ring-shaped structures have formed progressively, while the false cavities closed completely or quasi-completely over time. Thus, the very large false cavity of the baobab of Samba Dia closed only 150-200 years ago.Dating results also indicate that the stems of the very old Lebombo baobab continue growing at a quasi-constant rate toward the outer part of the tree. However, the same stems basically stopped growing toward the common false cavity over the past ca. 500 years, probably for not disturbing the stable internal architecture. On the other hand, the fused stems of the baobab of Sambia Dia continue growing relatively fast both toward the outer part and toward the false cavity.

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