Orbital chronology of the Pliensbachian Â Toarcian ...pure.au.dk/portal/files/110283456/s3.pdf · Middle Atlas Oran Meseta Central High Atlas Anti Atlas Sahara Atlas Emerged lands

Newsletters on Stratigraphy Vol 501 (2017) 47ndash69 Open Access Article Published online October 2016 published in print January 2017

Orbital chronology of the PliensbachianndashToarciantransition from the Central High Atlas Basin(Morocco)

Mathieu Martinez1 Franccedilois-Nicolas Krencker23 Emanuela Mattioli4 and Steacutephane Bodin25

With 9 figures and 1 table

Abstract The PliensbachianndashToarcian transition has been studied in depth for the major environmentalchanges and the marine invertebrate biodiversity crisis observed at that time Despite a large number of stud-ies performed the time frames provided for this interval show large discrepancies from author to author Ma-jor environmental changes occurring at that time impacted the sedimentation pattern and sedimentation ratesmaking uncertain the construction of time scales Here we provide a new astrochronological frameworkbased on an expanded hemipelagic section from the Central High Atlas Basin (Morocco) δ13C and CaCO3

measurements performed on the studied section allowed the construction of an orbital time scale based on the405-kyr eccentricity and the obliquity cycles This orbital time scale is then compared to the Peniche section(GSSP of the Toarcian Stage) in order to limit the effects of eventual condensation and erosion events on theconstruction of the orbital time scale The duration of the early Toarcian Polymorphum Zone is then assessedat 09ndash10 myr while the interval from the base of the Toarcian Stage to the FO of C superbus is assessed at051 myr This long duration of the Polymorphum Zone highlights the fact that numerous sections in Europeare affected by long-term condensation and hiati around the PliensbachianndashToarcian transition Finally wealso explore the potential of the Central High Atlas basin to provide a refined time scale for the late Pliens-bachian Preliminary data lead to a duration assessment of the NJ5b calcareous nannofossil zone of at least207 myr and to a mean duration of the Emaciatum ammonite zone of 205 myr These durations are ~ 1 myrlonger than the durations proposed in the Geological Time Scale 2012 which illustrates the potential of theCentral High Atlas Basin for calibrating the Pliensbachian times

Key words Toarcian Pliensbachian cyclostratigraphy P-To event High Atlas carbon-isotopes

copy 2016 The authorsDOI 101127nos20160311 Gebruumlder Borntraeger Stuttgart Germany wwwborntraeger-cramerde

Authorsrsquo addresses1 MARUM Center for Marine Environmental Sciences Universitaumlt Bremen Leobenerstr 28359 Bremen Germany2 Ruhr-Universitaumlt Bochum Institut fuumlr Geologie Mineralogie und Geophysik 44870 Bochum Germany3 Present address Halliburton (Neftex) 97 Jubilee Avenue Milton Park Abingdon Oxfordshire OX14 4RW United King-dom4 Univ Lyon Universiteacute Claude Bernard Lyon 1 Ens de Lyon CNRS UMR 5276 LGL-TPE F-69622 VilleurbanneFrance5 Present address Department of Geoscience Aarhus University DK-8000 Aarhus C Denmark Corresponding author mmartinezmarumde

1 Introduction

The construction of a robust Geological Time Scale is of critical importance for assessing the rhythms ofgeodynamic changes palaeoceanographic and palaeo-climatic processes The last update of the GeologicalTime Scale 2012 (GTS 2012 Gradstein et al 2012) hasshown to contain some non-negligible uncertaintieswhich can reach several millions of years (Pellenard etal 2013 De Vleeschouwer and Parnell 2014 Vennariet al 2014 Martinez et al 2015) Yet the developmentof extended astrochronological frameworks has al-ready contributed to the construction of a robust geo-logical time frame for the Cenozoic (e g Lourens et al2004) The construction of new astrochronologicalframeworks are currently extended for Jurassic andCretaceous successions in order to decrease the timeuncertainty of those periods by at least one order ofmagnitude (Weedon and Jenkyns 1999 Huang et al2010 Martinez et al 2015)

One of the critical intervals of the Jurassic Period isthe PliensbachianndashToarcian transition This time in-terval is affected by two global palaeoenvironmentalchanges respectively at the PliensbachianndashToarciantransition (the PliensbachianndashToarcian event or P-Toevent) and the Toarcian oceanic anoxic event (T-OAE)at the base of the LevisoniSerpentinum Zone Theseevents are characterised by excursions in the δ13Crecords (Hesselbo et al 2007 Suan et al 2008a Bodinet al 2010 2016) increased accumulation of organicmatter observed during the T-OAE (e g Jenkyns1988) higher levels of continental weathering and nutrient supply (Cohen et al 2004 Dera et al 2009Bodin et al 2010 2011) demise of the carbonate plat-form factories (Bassoullet and Baudin 1994 Suan etal 2008a Wilmsen and Neuweiler 2008 Leacuteonide et al2012 Krencker et al 2014) and extinction events af-fecting marine invertebrates (Little and Benton 1995Caruthers et al 2013) These environmental changeswere further accompanied by major changes inpalaeotemperature (Jenkyns 2003 Suan et al 2008a2010 Dera et al 2011a) and sea level (Hesselbo 2008Sabatino et al 2009 Suan et al 2010 and referencestherein Pittet et al 2014) likely linked to the growthand decay of polar ice caps (Suan et al 2010 Korteand Hesselbo 2011) All these environmental changestriggered major turnovers in facies environment andor sedimentation rate (Bassoullet and Baudin 1994 deGraciansky et al 1998 Hesselbo and Jenkyns 1998Leacuteonide et al 2012 Pittet et al 2014 Ruebsam et al2014) Major sea-level changes are notably responsi-

ble for the recurrence of condensed intervals and hiatalsurfaces recorded in the early Toarcian (Leacuteonide et al2012 Pittet et al 2014) As a consequence attempts tobuild a robust time scale in this time interval led to diverging astrochronological interpretations (Suan etal 2008b Kemp et al 2011 Huang and Hesselbo2014 Ruebsam et al 2014) The first ammonite zoneof the Toarcian (i e the Tenuicostatum or Polymor-phum Zone) is particularly representative of this de-bate duration estimates based on orbital time scalesfluctuating over almost two orders of magnitude from009 myr to ~ 115 myr (Mattioli and Pittet 2004 Suanet al 2008b Boulila et al 2014 Ruebsam et al 2014)The construction of high-resolution astrochronologi-cal frameworks ideally requires a continuous and ex-panded sedimentary record with a minimum of con-densation suggesting that the previously studied sec-tions were not suited for improving of the Pliensbachi-anndashToarcian time scale

The Central High Atlas Basin of Morocco has ex -perienced high tectonic subsidence in the Triassic renewed at a moderate rate during the Early Jurassic(Frizon de Lamotte et al 2008) As a result during the PliensbachianndashToarcian expanded sections weredeposited in hemipelagic environments (Bodin et al2011 2016) These sections are much expanded com-pared to the European sections reported at the Pliens-bachianndashToarcian transition which is expected to lim-it the occurrence of condensation or hiati

In the Foum Tillicht section spectral analyses havebeen performed on high-resolution δ13C and CaCO3

records covering the PliensbachianndashToarcian transi-tion In addition δ13C and CaCO3 were measured inthe Pliensbachian part of the series although at a lowerresolution which provides the opportunity to evaluatethe potential of the Foum Tillicht section to record thelong eccentricity cycle (405 kyr) Further we test if itcan be used as a reference section for further calibra-tions of the late Pliensbachian time scale

2 Geological setting

21 The Central High Atlas Basin

The Central High Atlas Basin is part of an Atlanticaulacogen rift system (Frizon de Lamotte et al 2008)This is a rift basin opened in the Triassic during thedislocation of Gondwana as the result of transtensivemovements A renewed phase of tectonic subsidencestarted in the late Pliensbachian (Frizon de Lamotte et

M Martinez et al48

al 2008) The subsequent creation of accommodationspace allowed for the deposition of an expanded andcontinuous sedimentary record spanning the Pliens-bachianndashToarcian interval (Piqueacute et al 2002)

During the Early Jurassic the Central High AtlasBasin was located at the northern margin of Gond-wana at a palaeolatitude of ~ 15deg N It was separatedfrom the nascent Atlantic Ocean by the MoroccanMeseta (also called West Moroccan Arch) and open atits eastern side to the Tethys Ocean (Fig 1 Bassouletet al 1993) The southern western and northwesternborders of the Central High Atlas Basin were the lociof extensive shallow-water carbonate production dur-ing the HettangianndashPliensbachian (du Dresnay 1971Milhi et al 2002 Wilmsen and Neuweiler 2008) Thiswas followed by a rapid demise in neritic carbonate

production occurring at the PliensbachianndashToarciantransition and related to a climatic change from aridtowards more humid conditions during the earliestToarcian (Wilmsen and Neuweiler 2008 Bodin et al2010 2016 Krencker et al 2015) As a consequencea major lithological break marks the PliensbachianndashToarcian transition in Morocco in both shallow- anddeep-water settings carbonate-rich Pliensbachian sed-imentary rocks are overlain by siliciclastic-rich Toar-cian sediments

22 Lithology and biostratigraphy of the Foum Tillicht section

The here-studied Foum Tillicht section is situatedwithin the central part of the Central High Atlas Basin

Orbital chronology of the PliensbachianndashToarcian transition 49

50deg

40deg

30deg

20deg

10deg

0deg

-10deg-20deg

Tethys

Gondwana

Emerged landsShallow seasDeeper basins

MoroccanMeseta

Rif

Tell

Middle

Atlas

Oran Meseta

Central High

Atlas

Anti Atlas

Sahara

Atlas

Emerged landsShallow seasOpen ocean

westernHigh Atlas

Laurasia

A B

SaharaCraton

Foum Tillichtsection1

C D

Tagoudite Fm Ouchbis Fm

Tagoudite Fm

Ouchbis Fm

Fig 1 Geological setting of the Foum Tillicht section A Palaeogeographic map of the western Tethys during the EarlyJurassic The dashed rectangle shows the limit of the second map Mark ldquo1rdquo indicates the location of the Peniche sectionB Geographic map of Morocco and western Algeria showing the main geological provinces and the location of the FoumTillicht section within the Central High Atlas basin (maps from Bodin et al 2010) C Overview of the Foum Tillicht sectionshowing the Ouchbis and Tagoudite formations Contrasts have been enhanced to show colour variations in the Tagouditeformation D Detailed view of the PliensbachianndashToarcian transition in the Foum Tillicht section

approximately 10 km northwest of the city of Rich(Fig 1) on the eastern side of the N13 main road It encompasses the upper part of the Ouchbis Formationand the lower part of the Tagoudite Formation andcovers the PliensbachianndashToarcian transition (Fig 1Wilmsen and Neuweiler 2008) The Ouchbis Forma-tion is composed of fine-grained marl-limestone alter-nations showing rhythmic changes of the limestone tomarl ratio deposited in a hemipelagic environment(Fig 1) Ammonites belemnites and calcareous nan-nofossils have been encountered The Ouchbis Forma-tion is followed by the Tagoudite Formation (Fig 1) afine-grained clayey carbonate sequence showing in itsmedium and upper part numerous intercalations offine-to-medium grained siliciclastic beds interpretedas turbidite deposits (Bodin et al 2016)

The integration of biostratigraphic data from Euro-pean basins led to the definition of three standard am-monite zonations (Subboreal Tethyan and Mediter-anean) and two standard calcareous nannofossil zona-tions for northwestern Europe and western Mediter-ranean countries (Cariou and Hantzpergue 1997Bown and Cooper 1998 Mattioli and Erba 1999 Page2003 Bilotta et al 2010 Gradstein et al 2012 Mat -tioli et al 2013 Fraguas et al 2015) The ammonitezonation of the Foum Tillicht section is based on theMediterranean zonation while the calcareous nanno-

fossil zonation is based on the Tethyan zonation (Bo -din et al 2016) Figures 2 and 3 detail the chronostrati-graphic relationships between the different zonationscovering the PliensbachianndashToarcian transition

Scarcity of ammonite in the Ouchbis Formation didnot allow the ammonite zones in the late Pliensbachianto be precisely bounded The FO of nannofossil Lo -tharingius sigillatus defining the base of the NJ5bnannofossil zone is recorded at 524 m (Bodin et al2016) Nonetheless the first sample analysed for nan-nofossil assemblages below 524-m level is located at36 m implying that the uncertainty of the location ofthe FO of L sigillatus is at least 164 m The Pliens-bachianndashToarcian boundary is marked by the massiveappearance of ammonite Dactylioceras sp in the lastthree beds of the Ouchbis Formation This is con-firmed by the first occurrence (FO) of the coccolithDiscorhabdus ignotus at 109 m (Bodin et al 20102016 Mattioli et al 2013)

In the transition from the Ouchbis Formation to the Tagoudite Formation Wilmsen et al (2002) report-ed several specimen of Harpoceras sp According tothese authors this dates the base of the Tagoudite For-mation at Foum Tillicht from the lowermost but notbasal PolymorphumTenuicostatum ammonite Zonesuggesting a biostratigraphic condensation at the tran-sition between the two formations However no phys-

M Martinez et al50

NJ5b

NJT6Carinolithus

superbus

Lotharingius sigillatus

Pleurocerasspinatum

Dactyliocerastenuicostatum

Harpocerasfalciferum

NW EuropeAmmonites Calc nanno

NJT5app

NJ5b

NJT6

Carinolithussuperbus



Harpocerasserpentinum

Italy S FranceAmmonites Calc nanno

NJ5Tb

NJT6



Pleurocerasspinatum



N SpainAmmonites Calc nanno

NJT5app

NJ5b

NJT6pp



LatePliensbachian

pp

Early Toarcianpp

Substages

Stages

Emaciaticerasemaciatum

Dactylioceraspolymorphum

Hildaiteslevisoni

Lusitanian BasinAmmonites Calc nanno

Discorhabdusstriatus


Mattioli et al (2013) Mattioli and Erba (1999) Perilli et al (2004) Fraguas et al (2015) Bown and Cooper (1998)

Pleurocerasspinatum

Crepidolithusimpontus

Fig 2 Comparison of ammonite and calcareous nannofossil zones from Portugal (Lusitanian Basin) Italy and SouthernFrance Northern Spain and Northwestern Europe modified from Perilli et al (2004) The correlation scheme from Perilliet al (2004) is modified as follows Lusitanian Basin correlations between ammonite zones and calcareous nannofossilzones are from Mattioli et al (2013) ItalyS France correlations between ammonite zones and calcareous nannofossil zonesare from Mattioli and Erba (1999) The question mark positioned between the D tenuicostatum and the H serpentinum zonestakes into account the biostratigraphic data from Bilotta et al (2010) N Spain correlations between ammonite zones andcalacareous nannofossil zones are from Perilli et al (2004) with updates from Fraguas et al (2015) NW Europe correlationsare from Bown and Cooper (1998)


LatePliensbachian

pp

Early Toarcianpp




Pleurocerasspinatum



NJ5a

NJ5b

NJ6





Hildaiteslevisoni

Substages Mediterranean SubborealTethyan

Standard ammonite zones Standard calc nannofossil zonesBoreal (NJ)

Stages

CrepidolithusimpontusArieticeras

algovianumArieticerasalgovianum

Cariou and Hantzpergue (1997)GTS 2012 (Gradstein et al 2012)

NJT5a

NJ5Tb

NJT6



Tethyan (NJT)

Lotharingiussigillatus

Fig 3 Standard zonation schemesat the PliensbachianndashToarcian tran-sition (from Cariou and Hantzpergue1997 Gradstein et al 2012) Corre-lations between the standard Tethyanand Subboreal ammonite zones withTethyan and Boreal calcareous nan-nofossil zones reported in the GTS2012 (Gradstein et al 2012) are gen-erated here using software TimeScale Creator 64

-29 -28 -27 -26 -25 -24 -23 -22 -21-31 -30 -3 -2 -1 0 1 2 30 m

50

100

150

200

250

300

350

400

440

massive appearance of Dactylioceras sp

FO Carinolithus superbus

T-OAE

P-To event

13Corg (permil VPDB) 13Ccarb (permil VPDB)

mMWPGFsltfsmscsg vcs

RB

PLIE

NSB

AC

HIA

NTO

AR

CIA

N

Ouc

hbis

Fm

Ta

goud

ite F

m

Pol

ymo

Levi

soni

Em

acia

tum

Upp

erM

iddl

eU

pper

Low

er

Bifr

ons

Gra

data

Ago

udim

Fm

hiatus

Tauromeniceras sp

Arieticeras spEmaciaticeras sp

Lioceratoides sp

Eleganticeras sp

Hildoceras lusitanicum

Hildoceras semipolitum

Hammatoceras sp cf insigne

FO Lotharingius sigillatus

FO Discorhabdus ignotus

Alg

ov

Stu

died

inte

rval

(see

Fig

4)

Fig 4 Biostratigraphic lithostratigraphic and carbon-isotope chemostratigraphic framework of the Foum Tillicht section(from Bodin et al 2016)

ical evidence for condensation such as high-densitybioturbation glauconite or any other mineralizationwas observed at this level At 12924 m the FO ofCarinolithus superbus defining the base of the NJT6nannofossil zone has been recorded (Bodin et al2016) This zone usually corresponds to the upper partof the PolymorphumTenuicostatum ammonite Zone(Mattioli and Erba 1999 Mattioli et al 2013) In thisinterval nannofossil assemblages were analysed every15 m giving the minimum uncertainty on the positionof the FO of C superbus At 14225 m a hiatus hasbeen interpreted based on carbon isotope chemo strati -graphy (Bodin et al 2016 Fig 4) This coincides withthe base of one prominent turbidite bed Using organicmatter carbon isotope chemostratigraphy Bodin et al(2016) were able to show that this hiatus correspondsto the upper part of the Polymorphum zone and thelower part of the Levisoni ammonite zone (Fig 4)

The boundary between the Ouchbis Formation andthe Tagoudite Formation corresponds to the interval ofthe P-To event recorded by a reduction in the valuesand amplitudes of the δ13C and CaCO3 data (see sec-tion 4 Figs 4 5) Bodin et al (2016) defined the P-Toevent as the interval starting from the lithologicalchange at 10538 m and ending at the local maximumof δ13Ccarb values at 11791 m

3 Material and Methods

31 Measurements of δ13C and CaCO3

A total of 237 bulk micrite samples from the upperPliensbachian to lower Toarcian interval were collect-ed across the Foum Tillicht section at an average un-even step of 208 m from the base of the series to6755 m at an average uneven step of 105 m from6755 to 10937 m and then with an even step of 020 m from 10937 m to the top of the studied seriesFor each horizon several milligrams of the micriticpart of non-weathered limestone and marlstone sam-ples lacking allochems and diagenetic veins were se-lected ground to powder and homogenised in an agatemortar Geochemical analyses performed on all sam-ples include carbon (δ13Ccarb) isotope composition andcarbonate contents These analyses complement theones presented in Bodin et al (2016)

32 Carbonate content analyses

The carbonate content of bulk rock samples weremeasured from 697 m to 14215 m Carbonate con-

tents were determined using the total inorganic carbon(TIC) contents of the samples at the Ruhr Universityof Bochum The TIC values were determined using aCarbon Sulfur Determinator CS 500 (Eltra GmbH)Depending on the lithology (marlstone or limestone)between 100 to 500 mg of material were weighted inan Erlenmeyer flask and reacted with 125 mL of di-luted phosphoric acid (H3PO4H2O 11) injected inthree doses The amount of CO2 produced by this re-action was measured by infrared detector through anoxygen stream and used to determine the sample TICcontents The quality of the measurements was con-trolled and corrected using calibration curves based on internal standards with known carbonate contentsIndividual samples were measured with a precisionbetter than 5 Replicate analyses of samples have aprecision better than 6 on average

33 Inorganic carbon isotope analyses

Carbon isotope analyses of bulk micrite carbonate(δ13Ccarb) was performed in the whole studied intervalusing a Gasbench II coupled to a Finnigan MAT 253mass spectrometer Depending on the calcium carbon-ate content of individual samples between 04 to17 mg of powder were weighed in vials and dried for48 h in a 105degC preheated oven and subsequentlycooled in a refrigerator for 1 h The air present in thevials was flushed using helium in order to avoid anycontamination Carbonates were sublimated by addinganhydrous phosphoric acid (104) using an auto-sampler The isotopic composition is reported as δ-value in parts per mil [permil] relative to the internation-al Vienna PDB (V-PDB) standard The quality of themeasurements was controlled by NBS19 NBS18 andRUB internal standards Isotope data were correctedusing CO1 and CO8 carbonate standards For micritesamples the reproducibility (3 n 4) calculatedwith the Ruhr University of Bochum internal standardwas better than 008permil for δ13Ccarb Sample process-ing and stable isotope analyses were carried out at theRuhr University of Bochum

34 Spectral analyses

The long-term evolutions of the δ13Ccarb and CaCO3

series are marked by a sudden decrease of the δ13Ccarb

and wt CaCO3 values at the transition between theOuchbis and Tagoudite formations (Fig 5) Prior tospectral analyses the long-term trends of the serieswere thus calculated and subtracted using piecewiselinear regressions Since the data are not collected at

M Martinez et al52


CaC

O3

()

2030

4050

6070

stan

dard

ized

CaC

O3

+ E

cc 4

05 k

yr-2

-10

12

-2-1

01

2

stan

dard

ized

CaC

O3

+ O

bliq

uity

0 m

100

140

PLIENSBACHIANTOARCIANPolymorphum AlgovianumEmaciatum

C superbus

13 C

(permil

PD

B)

-10

12

80120 40 2060

Ouchbis FmTagoud Fm

01

02

03

04

01

25

Fre

quen

cy(c

ycle

sm

)F

requ

ency

(cyc

les

m)

01

02

03

04

01

25

Fre

quen

cy(c

ycle

sm

)F

requ

ency

(cyc

les

m)

-20

2-2

02

Sta

ndar

dize

d 1

3 C+

Obl

iqui

ty

13241513211615

69

6345

7053

76

17

23

64

405-kyr eccentricity

obliquity100-kyr eccentricity

15

82

2315

41

~5392

5

16


173-kyr obliquity


obliquity


505 plusmn 44 kyr

AB

CD

EF

GH

IJ

StageAmmo Zone

Formation

L sigillatus

177 plusmn 11 kyr (option 2)273 plusmn 20 kyr (option 1)

Sta

ndar

dize

d 1

3 C+

Ecc

405

kyr

P-To event

NJT5b NJT5aNJT6

Fig

5

Tim

e-fr

eque

ncy

spec

tral

ana

lyse

s an

d or

bita

l tun

ing

of th

e Fo

um T

illic

ht s

ectio

n A

Raw

δ13

C s

igna

l In

red

th

e lo

ng-t

erm

tren

d B

Tan

er lo

w-p

ass

filte

r of

the

405-

kyr

ecce

ntri

city

on

the

detr

ende

d δ13

C (

freq

uenc

y cu

t 1

038

10

ndash1

cycl

esm

ro

ll-of

f ra

te

1012

) C

Ta

ner

band

-pas

s fi

lter

of t

he o

bliq

uity

(lo

wer

fre

quen

cy c

ut

390

6

10ndash

1cy

cles

m u

pper

freq

uenc

y cu

t 7

935

10

ndash1

cycl

esm

rol

l-of

f rat

e 1

012)

D4

0-m

-win

dow

spe

ctro

gram

of t

he δ

13C

ser

ies

with

mai

n pe

riod

s la

belle

d in

met

ers

E1

5-m

-win

dow

spe

ctro

gram

of

the

δ13C

ser

ies

with

mai

n pe

riod

s la

belle

d in

met

ers

FR

aw C

aCO

3si

gnal

In

red

the

long

-ter

m t

rend

GT

aner

low

-pas

s fi

lter

of t

he40

5-ky

r ec

cent

rici

ty o

n th

e de

tren

ded

CaC

O3

(fre

quen

cy c

ut 7

324

10

ndash2

cycl

esm

rol

l-of

f ra

te 1

012)

HF

ilter

of

the

obliq

uity

on

the

detr

ende

d C

aCO

3(l

ower

fre

quen

cycu

t 3

297

10

ndash1

cycl

esm

upp

er fr

eque

ncy

cut

934

1

10ndash

1cy

cles

m r

oll-

off r

ate

1012

) I

40-

m-w

indo

w s

pect

rogr

am o

f the

CaC

O3

with

mai

n pe

riod

s la

belle

d in

met

ers

J15

-m-w

indo

w s

pect

rogr

am o

f th

e C

aCO

3w

ith m

ain

peri

ods

labe

lled

in m

eter

s

an even sample step the series were linearly resam-pled every 020 m in order to allow the multi-tapermethod (MTM) to be applied to the series Signi -ficance levels of spectral peaks were assessed usingthe LOWSPEC method (Meyers 2012) and the robustmethod of Mann and Lees (1996) modified in Meyers(2014) Time-frequency weighted fast Fourier trans-forms (TF-WFFT e g Martinez et al 2013 2015)were then applied to constrain the evolution of the periods throughout the sedimentary series A first TF-WFFT was applied on 40-m width windows to betterconstrain the low frequencies and a TF-WFFT on20-m width windows was applied to focus on the evo-lution of the short periods The cross multi-taper andthe cross-phase spectra were also calculated betweenthe δ13Ccarb and CaCO3 signals using the algorithm de-veloped in Huybers and Denton (2008) and providedin the following url link httpwwwpeoplefasharvardedu~phuybersMfiles

Taner low-pass and band-pass filters were then ap-plied to isolate each signal interpreted as an orbitalforcing Orbital tuning procedures are then used to anchor the sedimentary cycles to their correspondingorbital periods allowing depth-time conversions to bedone Here minima of filtered series are used to definethe anchor points Between two anchor points a dura-tion of 405 kyr or 349 kyr is attributed depending if the 405-kyr eccentricity or the main obliquity(349 kyr) are used to anchor the series Within eachrepetition of the target cycle a constant sedimentationrate is assumed Above the last complete cycle or be-low the first complete cycle the sedimentation rate isassumed to be the same as within the last or the firstcomplete cycle respectively A relative age is thus at-tributed to each point Durations are then estimated bycalculating the difference of relative ages Error mar-gins are estimated by calculating the standard devia-tion of the duration estimates for each time interval

4 Results

41 Geochemical data

411 Inorganic carbon isotopesThe carbon-isotope profile of the Foum Tillicht sectioncan be divided into two chemostratigraphic intervalsbased on their specific pattern (Figs 4 5) The intervalfrom 0 m to 110 m (Pliensbachian part of the series) is characterised by an overall decreasing trend of theδ13Ccarb values from +25 to +05permil This trend is mod-

ulated by regular 6-m thick small amplitude (05permil)fluctuations of the δ13Ccarb values The interval from110 m to 14225 m (Toarcian part) records an increaseof the δ13Ccarb ratios from ndash1permil to ndash06permil The trend ismodulated by 2-m fluctuations of the δ13Ccarb valuesoscillating between 0permil and ndash2permil The transition be-tween the first and the second interval is abrupt andcharacterised by a sharp and prominent 2permil decrease ofthe δ13Ccarb values (Fig 4) This abrupt shift has beenlinked to the P-To event based on organic and inorganiccarbon isotope chemostratigraphy constrained by am-monite and nannofossil biostratigraphy (Bodin et al2016) The top part of the second interval is also markedby a hiatus inferred from chemostratigraphic correla-tion (Bodin et al 2016 see Fig 4) Most likely this dis-continuity is due to subaqueous erosion as supported bythe overall deep marine environmental setting charac-terising the Foum Tillicht section and also the commonoccurrence of turbidite-rich interval above the base ofthe hiatus at 14225 m (Fig 4 Bodin et al 2016)

412 Carbonate contentsAs for the carbon isotopes the carbonate content seriescan be divided into two intervals The first interval ofthe series from 697 m to 11361 m shows a trend ofCaCO3 values decreasing from 72 to 42 (Fig 5F)Within this trend high-amplitude fluctuations (20ndash50) are observed with a thickness of 4ndash6 m Thetransition from the first to the second interval is moreprogressive than observed for the δ13Ccarb series Thevalues and high-frequency amplitudes of the CaCO3

series rapidly decrease from 10538 m to 11361 mThis interval corresponds to the transition from theOuchbis Formation and the Tagoudite Formation andis related to the P-To event (see section 22) The sec-ond interval from 11361 m to 14225 m shows lowvalues and rather stable values of CaCO3 around 20High-frequency fluctuations are still observed but withmuch lower amplitudes compared to the first interval(~ 10)

42 Results from spectral analyses

The 2π-MTM spectrum of the δ13Ccarb series showssignificant bands at periods 176 m 17 m (on average)and 09 m (Figs 6A C E) On spectrograms the~ 17-m peak is observed throughout the series havingperiods evolving from 24 m to 13 m (Fig 5D) The15-m-width-window spectrogram (Fig 5E) showsfrom the base of the series to level 102 m a band of pe-riods ranging from 45 m to 76 m On the multi-taper

M Martinez et al54

spectrum the amplitude of this cycle is not enough toexceed the 95 confidence level (Fig 6) From 107 mto the top of the series the spectrogram shows a bandof periods ranging from 23 to 17 m (Fig 5E)

The 2π-MTM spectrum of the CaCO3 series showssignificant bands of periods at 18 m on average and09 m (Fig 6B D F) Another period at 182 mevolves from 15 to 23 m and displays high amplitudesfrom the levels 70 m to 124 m (Figs 6B 5I) On the40-m-width-windows of the CaCO3 periods at 82 mand 41 m appear from the 70 m to 90 m (Fig 5I) Onthe 15-m-width-windows of the CaCO3 a band of pe-riods ranging from 5 to 39 m appears from levels 70 mto 102 m (Fig 5J) Another band of periods rangingfrom 25 to 16 m appears from levels 110 m to the topof the series

The cross-MTM analysis is performed with theδ13Ccarb and CaCO3 signals that have been both linear-ly interpolated every 020 m from 697 to 1421 m andstandardised Significant coherence values are ob-served between the two signals at 161 m a band of period centred on 17 m and a band of periods centredon 09 m (Fig 7A) The average phase of these signif-icantly coherent periods is 7deg (Fig 7B) In addition the phase lag observed for each significant frequencyindividually reaches the equivalent of twice the samplestep for the 16-m period and corresponds to a valuelower than the sample step otherwise The two signalsare roughly in phase the bulk δ13Ccarb increases withincreasing CaCO3 values This is also shown with asimple cross-plot in which the δ13Ccarb values of lime-stone beds are higher than the δ13Ccarb values of marl-stone beds (Fig 7C)

5 Discussion

51 Interpretation of the sedimentarycycles

On the multi-taper spectrum of the δ13Ccarb series thethree significant periods of 09 m 17 m and 176 mdisplay a ratios of periods of 119196 close to theperiod ratios between the precession (average period199 kyr) the obliquity (main period 349 kyr) and the405 kyr eccentricity cycles (ratios 118204) Theaverage period of 48 m showing high amplitudes onthe spectrogram (Fig 5D) has a period ratio of 136with the period of 176 m 128 with the period of17 m and 153 with the period of 09 m This 48-mperiod is likely related to the 100-kyr eccentricity

On the multi-taper spectrum of the CaCO3 seriesthe significant periods of 18 m and 09 m display a period ratio of 12 related to the period ratio betweenthe obliquity and the precession cycles The period of182 m has a ratio of 110 with the period at 18 m anda ratio of 120 with the period of 09 m The 182-mpeak is likely related to the 405-kyr eccentricity cycleThe peak at 41 m observed on the spectrograms has aperiod ratio of 144 with the 182-m peak 123 withthe 18-m peak and 146 with the 09-m peak This pe-riod of 41 m can be related to the 100-kyr eccentricityAlso observed on the spectrograms the period of82 m shows a ratio of 122 with the period of 182 ma ratio of 12 with the period of 41 m and a ratio of146 with the period of 18 m This period of 82 mcan be related to the 173-kyr obliquity a period shownin the astronomical solutions as an amplitude modula-tion of the obliquity cycles and related to s3ndashs6 thesecular frequencies of the inclination of the Earth andSaturn orbits (Laskar et al 2004 2011)

In summary the 405-kyr eccentricity is recorded on17ndash18 m of sediment thickness the 100-kyr eccentric-ity on 41ndash48 m the main obliquity on 17ndash19 m andthe precession on 09 m

52 Significance of the δ13Ccarb signal

Cyclic fluctuations in the δ13Ccarb record has been pre-viously documented from the Cenozoic to the Jurassicarchives mostly related to the long ( 405 kyr) eccen-tricity and obliquity cycles (Zachos et al 2001 Crameret al 2003 Paumllike et al 2006 Voigt et al 2007 Wanget al 2010 Giorgioni et al 2012 Laurin et al 2015Martinez and Dera 2015) Several explanations havebeen brought forward by these authors in order to ex-plain the transfer of the orbital forcing into the carbonisotope record involving regional or global processesHere the long-term trend of the δ13Ccarb curve obtainedat Foum Tillicht fits neither with the long-term of theδ13Corg curve from the same section (Fig 4) nor withother δ13Ccarb curves obtained from the NorthernTethyan margin (see compilation in Pittet et al 2014)This favours a basin-scale control of the δ13Ccarb atleast in part decoupled from organic carbon reservoirs

The δ13Ccarb and CaCO3 signals are significantly co-herent and in phase at the Milankovitch band (Fig 7)In other words the δ13Ccarb is higher in limestone thanin marl beds Bodin et al (2016) have notably noticedthat the major negative shift in δ13Ccarb at the Pliens-bachianndashToarcian transition was likely related to thedemise of the neritic carbonate factory around the


M Martinez et al56

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High Atlas Basin leading to a halt of neritic carbonatemud shedding into the basinal setting In addition carbonates in the Ouchbis Formation have high Srcontents suggesting an aragonitic origin in agreementwith platform shedding (Wilmsen and Neuweiler2008) Given that this neritic carbonate mud is likelyenriched in 13C compared to pelagic carbonates (Swartand Eberli 2005 Swart 2008 Oehlert et al 2012) themixing of neritic mud with pelagic ooze will tend toaugment the bulk δ13Ccarb signal in limestone beds

Conversely detrital and organic matter inputs fromcontinental areas associated to the deposit of marlbeds will tend to decrease the δ13Ccarb values as it hasbeen shown in early stages of the Jurassic sedimenta-tion in the Central High Atlas Basin (Wilmsen andNeuweiler 2008) In hemipealgic marl-limestone alter-nations marls are commonly associated to higher lev-els of primary productivity associated to basin fertil-ization (Mutterlose and Ruffell 1999 Greacuteselle et al2011 Giraud et al 2013) contributing in a reduction


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Fig 6 2π-Multi-taper method (2π-MTM) spectra from the δ13C (left column) and CaCO3 (right column) of the FoumTillicht section A 2π-MTM spectrum of the δ13C series focused on the low powers Inset 2π-MTM spectrum showing thehighest-power peaks Confidence levels are calculated from the red-noise fit assessed with the robust method of Mann andLees (1996) modified in the astrochron R package (Meyers 2014) B 2π-MTM spectrum of the CaCO3 series Confidencelevels are calculated from the red-noise fit assessed with the robust method modified in the astrochron R packageC Prewhitened 2π-MTM spectrum of the δ13C series Confidence levels are calculated from the red-noise fit assessed withthe LOWSPEC method (Meyers 2012) D Prewhitened 2π-MTM spectrum of the CaCO3 series Confidence levels are cal-culated from the red-noise fit assessed with the LOWSPEC method E Summary of confidence levels from the robust andLOWSPEC methods of the δ13C series F Summary of confidence levels from the robust and LOWSPEC methods of the theCaCO3 series Main periods are labelled in meters BW BandWidth CL Confidence Level E 405-kyr eccentricity e 100-kyr eccentricity O main obliquity (349 kyr) P mean precession (199 kyr)

Fig 7 Cross-MTM analysis and cross-plot of the δ13C and CaCO3 signals A Coherency spectrum B Cross-phase spec-trum The numbers in italic indicate the equivalent of the phase lag in meters C Cross-plot The ρ-value indicates the cor-relation coefficient Notice that here the data set is divided in two groups differentiated by their lithology making the ρ-valuevery high The correlation coefficient is used here as a guide to show that the δ13C is higher in limestone beds than in marl-stone beds

of the values in δ13Ccarb marls Partial remineralizationof organic matter in the marly interval during burialmight have also reinforced the initial contrast inδ13Ccarb values at all Milankovitch bands

It is worth noting that the sedimentation rate re-mains stable at the passage from the Ouchbis to theTagoudite formations (Fig 5) If marl-limestone alter-nations were only triggered by dilution effects by carbonate exports or detrital supplies the passage tothe Tagoudite Formation would respectively imply astrong decrease or increase in the sedimentation rateThe stability of the sedimentation rate from the Pliens-bachian to the Toarcian implies that marl-limestone al-ternations reflect a balance between detrital suppliesand carbonate shedding linked to successive humidarid and sea-level fluctuations (see for instance Hoede-maeker 1998 Mutterlose and Ruffell 1999 Moiroud etal 2012)

53 Calibration of the Foum Tillichtsection

The 405-kyr eccentricity cycle has high amplitudesthroughout the whole δ13Ccarb series and high ampli-tudes in the CaCO3 series from levels 70 m to 124 mwhile the obliquity cycle shows high amplitudes in thedensely sampled interval of the series (from 109 m tothe top of the series Fig 5) Both obliquity and the 405-kyr eccentricity are thus used for calibrating the seriesand estimating durations For both proxies two agemodels have been calculated (Table 1) one based onthe 405-kyr eccentricity only and one based on theobliquity in the densely sampled part of the series(from 109 m to the top of series) and on the 405-kyr ec-centricity on the least densely sampled part of the series(from the base of the series to 109 m) Spectral analyseson both series calibrated with the 405-kyr eccentricityreveal strong period at ca 04 myr ndash expected for a se-ries calibrated with the 405-kyr cycle ndash but also mainperiods at 41ndash42 kyr (associated with the obliquity)and from 25 to 16 kyr (associated with the precession)(Fig 8) Spectral analyses on both series calibratedwith the 405-kyr eccentricity and the obliquity revealstrong powers for the 405-kyr band and the obliquityband ndash expected ndash and significant peaks at 100 kyr as-sociated to the eccentricity and from 24 kyr to 14 kyrassociated to the precession (Fig 8) The spectra of theseries calibrated with only the 405-kyr eccentricity cy-cle reveal periods of 41ndash42 kyr for the obliquity whichis higher than the value predicted in the astronomicalmodels for the Toarcian Stage (349 kyr Laskar et al

2004) This difference can be due to the existence ofshort-term hiati in the Toarcian part of the series whichdecreases the number of obliquity cycles recorded pereccentricity cycle This uncertainty impacts the dura-tion estimates of the biozones Another source of un-certainty exists at low frequencies and corresponds to the accuracy with which the limits of the 405-kyr cycles have been positioned Differences thus exist in the duration estimate of a considered time intervalfrom one age model to another The difference betweenthe average estimate and an extremum estimate reachesa maximum of 007 myr for the Polymorphum Zone(Table 1) In the following paragraph the average du-ration estimates are given Full range of duration esti-mates can be found in Table 1

The average duration estimate of the whole studiedseries is assessed at 341 myr with estimates rangingfrom 335 myr to 347 myr (Table 1) The duration of the P-To event as defined in Bodin et al (2016) is assessed at 027 myr (option 1 in Fig 5) the durationof the interval from the base of the Toarcian to the FO of C superbus at 051 myr (Fig 5) and the mini-mum duration of the Polymorphum ammonite zone at081 myr In addition in the Pliensbachian the dura-tion of the Emaciatum ammonite zone is assessed at205 0318 myr The error margin here reflects theuncertainty in the position of the lower boundary of thisammonite zone (Figs 3 4) The minimum durationfrom the FO of L sigillatus to the base of the ToarcianStage is assessed at 155 Ma Finally the calcareousnannofossil Subzone NTJ5b spanning the intervalfrom the FO of L sigillatus to the FO of C superbushas a minimum duration assessed here at 207 myr Thedurations implying the FO of L sigillatus are given asminimum values since the position of this FO is uncer-tain at Foum Tillicht The durations of intervals of par-ticular interests are discussed in the next sections

54 Stratigraphic extension and duration of the P-To event

The P-To event is an episode of rapid environmentalchanges It is associated with a transient warming event(Suan et al 2008a) an acceleration of the rate of extinc-tion in marine macrofauna (Caruthers et al 2013) in-tensification of continental weathering (Bodin et al2010 Krencker et al 2015 Brazier et al 2015) wide-spread carbonate platform drowning (Dromart et al1996 Leacuteonide et al 2012 Bodin et al 2016) and a neg-ative excursion in the carbonate carbon isotopes partic-ularly well observed at Peniche (Hesselbo et al 2007)

M Martinez et al58

The P-To event starts with a significant increase in themarl-to-limestone ratio both observed in Morocco andin the Lusitanian basins (Elmi 2009 Bodin et al 20102016) and accompanied by a decrease in the δ13Ccarb

values (Pittet et al 2014) The end of the P-To eventshows various trends across the Tethyan and Subborealareas At Peniche the end of the P-To event is markedby a return of the δ13Ccarb values to the pre-P-To trend(Hesselbo et al 2007 Fig 9) At Foum Tillicht theδ13Ccarb values remain low after the rapid decrease ob-served at ~ 110 m and then show smooth low-ampli-tude fluctuations (Figs 5 9) Bodin et al (2016) tenta-tively positioned the end of the P-To event at FoumTillicht at the local maximum of the δ13Ccarb values at11781 m (Fig 4) This suggestion is also reported inFig 9 as Option 1 Based on the various astrochrono-logical frameworks provided here the duration of theP-To event would thus be assessed as 027 myr

The local maximum of δ13Ccarb values at 11781 moccurs in a smooth cyclic trend so that one can ques-tion whether or not the interval after the sharp decreaseof the δ13Ccarb values still belongs to the P-To event(Bodin et al 2016) The P-To event corresponds to acrisis in the carbonate platform production marked bya sharp decrease in the δ13Ccarb and in the wt CaCO3

values (Figs 5 9) This feature is observed at a region-

al scale (Hesselbo et al 2007 Suan et al 2008a Tre-calli et al 2012 Bodin et al 2016) The decrease inwt CaCO3 values ends at 11381 m Above the wtCaCO3 series has low amplitudes and never exceeds30 The P-To event at Foum Tillicht can thus be de-fined as the transition interval from high-amplitudeand high δ13Ccarb and wt CaCO3 values to low-am-plitude and low δ13Ccarb and wt CaCO3 values Ac-cording to this definition (Option 2 Fig 9) and takinginto account the various astrochronological frame-works provided here the P-To event would have a du-ration of 018 myr

The decreasing trend of the δ13Ccarb values closelymatches the lithological changes in most of the differ-ent studied basins (Hesselbo et al 2007 Trecalli et al 2012 Pittet et al 2014 Bodin et al 2016) and the extension from the base of the P-To event to the minimum of the δ13Ccarb values appears to be reliablefor establishing regional correlations In the FoumTillicht section this interval has a duration assessed at012 myr (Table 1)

Detailed astrochronological frameworks were pro-vided in the Peniche section at the PliensbachianndashToarcian boundary (Suan et al 2008b Huang and Hes-selbo 2014) the GSSP of the Toarcian Stage (Rochaet al 2016) The duration of the P-To event at Peniche


Table 1 Summary of the duration assessments from the various age models Note (a) the average duration corresponds tothe average of the maximum and minimum extension of the Emaciatum Zone considering the uncertainty in thelower boundary of this zone NA not available

Stratigraphic interval Orbital tuning on δ13C Orbital tuning on CaCO3

Durations Durations Durations Durations Average based on based on based on based on duration 405 kyr combined 405 kyr combined (myr)only (myr) 405 kyr and only (myr) 405 kyr and

obliquity obliquity (myr) (myr)

Studied series 347 335 NA NA 341

P-To Event ndash Option 1 029 026 029 025 027P-To Event ndash Option 2 019 017 019 017 018Base Toarcian to minimum δ13C during P-To Event 012 011 012 011 012

Polymorphum (minimum) 088 076 085 075 081Base Emaciatum (maximum extension) 227 227 NA NA 205 (a)Base Emaciatum (minimum extension) 182 182 NA NA

Base Toarcian to FO C superbus 055 047 053 047 051FO L sigillatus to base Toarcian 155 155 NA NA 155

NJT5b 211 203 NA NA 207

could be deduced at 005 myr while the duration fromthe base of the P-To event to the minimum of δ13Ccarb

values could be deduced at 004 myr All these dura-tions are significantly lower than the durations calcu-lated at Foum Tillicht suggesting a condensation inthe Peniche section at the PliensbachianndashToacianboundary as already proposed by Pittet et al 2014(Discontinuity surface D1) This condensation will notably impact on the duration estimate of the Poly-morphumTenuicostatum ammonite zone

55 Implication for the duration of thePolymorphumTenuicostatum Zone

The recent astrochronological studies show divergingdurations of the biozones and carbon-isotope excursionevents in the Early Toarcian (Suan et al 2008b Kempet al 2011 Boulila et al 2014 Huang and Hesselbo

2014 Ruebsam et al 2014) Notably the duration of the first ammonite zone of the Toarcian (equivalentPolymorphum or Tenuicostatum Zone see Figs 2 3) ishighly uncertain ranging from 009 myr to ~ 115 myr(Mattioli and Pittet 2004 Boulila et al 2014)

Using the 100-kyr-eccentricity cycle identified inSuan et al (2008b) the duration of the TenuicostatumZone could be assessed at 082 myr Using the 100-kyrand the 405-kyr eccentricity identified in Huang andHesselbo (2014) leads to a duration of 081 and077 myr respectively From these astrochronologicalframeworks an average duration of the TenuicostatumZone can be calculated as 080 myr Minimum dura-tions of the Tenuicostatum Zone were also reported at 555 kyr in the Lorraine sub-basin of the Paris Basin(core FR-210-78 Ruebsam et al 2014) and at 009ndash05 myr in the southern Paris Basin (Sancerre coreBoulila et al 2014) In these two latter studies the

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Fig 8 2π-MTM spectra of the δ13C and CaCO3 series after calibration based on the 405-kyr eccentricity only and on the405-kyr eccentricity and obliquity The main periods are labelled in kyr BW BandWidth E 405-kyr eccentricity e 100-kyr eccentricity O obliquity P precession


2040

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authors warned about the possibility of condensationor hiatus affecting the astrochronological frameworkinferred from these drill cores In addition significantbiostratigraphic uncertainties exist at Sancerre on theposition of lower and upper boundaries of the Tenui -costatum Zone (Boulila et al 2014) In the Lorrainesub-basin the FO of Dactylioceras tenuicostatum hasnot been formally recognised the base of the Tenui -costatum Zone being positioned on the last occurrenceof Pleuroceras spinatum (Gueacuterin-Franiatte et al2010) Such biostratigraphic uncertainties are addi-tional sources of errors in these duration estimates ofthe Tenuicostatum Zone The GTS 2012 used the cal-ibration of the Sancerre core to provide the duration ofthe Toarcian Stage with an arbitrarily added durationto take into account possible condensation at Sancerre(Huang et al 2010 Gradstein et al 2012) The accu-rate duration estimate of the Tenuicostatum Zone isthus crucial to provide a reliable time scale for theToarcian Stage

The duration of the Polymorphum Zone calculatedfrom the Foum Tillicht section is nonetheless a mini-mum duration since a hiatus is observed at the transi-tion between the Polymorphum and the Levisonizones and also since a biostratigraphic condensationis potentially present at the transition between theOuchbis and the Tagoudite Formations The hiatus atthe PolymorphumndashLevisoni transition is notably atthe base of a stratigraphic interval characterised by asharp increase in the occurrence and thickness of tur-bidite levels A sudden 5-permil decrease of δ13Corg is ob-served throughout the PolymorphumndashLevisoni transi-tion while other sections in the Central High AtlasBasin show a smoother initial decrease at the onset ofthe T-OAE (Bodin et al 2016) Finally δ13Ccarb curvestypically show a return to the pre-P-To values in theupper 13 of the Polymorphum Zone which is not ob-served in the Foum Tillicht section (Bodin et al 2016)

Conversely the Peniche section appears to have ashort-term condensation at the PliensbachianndashToar-cian transition (Pittet et al 2014) as also documentedby the longer duration assessment found in the FoumTillicht section The PliensbachianndashToarcian transi-tion in the Peniche section is condensed by 01 to02 myr according to the various scenarios retained forthe extension of the P-To event at Foum Tillicht Thisimplies a total duration of the PolymorphumTenui -costatum Zone ranging from 09 to 10 myr Mattioliand Pittet (2004) identified in central Italy ~ 115 litho-logical sequences attributed to the 100-kyr eccentricityin the Tenuicostatum Zone implying a duration of

115 myr In the Amellago section (Central High AtlasBasin) the return to the pre-P-To δ13Ccarb values (lack-ing at Foum Tillicht) covers 22 m With a sedimenta-tion rate evaluated as 94 mmyr for the early Toarcian(Bodin et al 2016) this leads to a duration estimate of 023 myr Although the visual identification of thesequences or the estimate of average sedimentationrates can lead to some errors both observations sup-port a long duration of the PolymorphumTenuicosta-tum Zone The duration of 09ndash10 myr for this zonedagrees with the GTS 2012 who arbitrarily added02 myr to the orbital chronology of Suan et al(2008b) However the integration of the orbital timescales of Foum Tillicht and Peniche show that this is areasonable estimate

56 Implications for the FO of C superbus

In the GTS 2012 the first appearance of C superbusin the Tethyan domain is aligned to its position in theEuro-Boreal domain i e at the base of the FalciferumZone (Gradstein et al 2012) However some discrep-ancies between authors have been reported (these ad-ditional comments can be found in Time Scale Cre-ator 64 available at the following link httpsengineeringpurdueeduStratigraphytscreatorindexindexphp) In most of Euro-Boreal basins including York-shire (Bucefalo Palliani et al 2002 Boomer et al2009) and Northern Spain (Perilli 1999 2000) the FOof C superbus occurs either at the base or within theSerpentinumFalciferum Zone (see Fig 2) Two no-ticeable exceptions are noted in the Euro-Boreal do-main in the Asturias (Spain) and in Dotternhausen(Germany) in which the FO of C superbus is locatedbefore the start of SerpentinumFalciferum Zone (Mat-tioli et al 2004 Fraguas et al 2015) In the PenicheAmellago and Foum Tillicht sections the FO of C su-perbus occurs in the middle part of the TenuicostatumZone In Italy the FO of C superbus occurs below theblack shale facies related to the T-OAE and within theTenuicostatum Zone although the ammonite biostrati-graphic scheme is flawed in Italy by the scarcity of ammonites within the black shale interval (Sabatino etal 2009 Mattioli et al 2013) obscuring the boundarybetween the Tenuicostatum and Serpentinus zones(Bilotta et al 2010) The FO of C superbus thus ap-pears to occur earlier in most of Tethyan sections i ebelow the T-OAE than in most of Euro-Boreal sec-tions where it occurs at the base or within the T-OAE(Mattioli and Erba 1999 Mailliot et al 2006)

M Martinez et al62

In this study the time interval from the base of thePolymorphum Zone to the FO of C superbus is as-sessed at 051 myr (range 047ndash053 myr) in the FoumTillicht section while this time interval has a durationassessment of 043 myr in the Peniche section (Fig 9)Considering that the P-To boundary in the Peniche sec-tion is condensed by 01 to 02 myr the duration fromthe base of the Toarcian to the FO of C superbus atPeniche is re-evaluated as 053ndash063 myr The nanno-fossil assemblages have been analyzed at Foum Til -licht every 15 m which highlights the maximum un-certainty on the position of the FO of C superbus Theaverage sedimentation rate of the Polymorphum Zonededuced from astrochronology is calculated at 44 mmyr so that the uncertainty on the position of the FOof C superbus at Foum Tillicht is assessed at 003 myrSimilarly at Peniche the nannofossil assemblageshave been observed with a step of 04ndash05 m corre-sponding to an uncertainty of 004 myr With this cor-rected evaluation and considering the error marginsthe duration from the base of the Toarcian to the FO ofC superbus cannot be distinguished between Penicheand Foum Tillicht

The GTS 2012 provides a zonation scheme of cal-careous nannofossil from the Tethyan domain separat-ed from the Euro-Boreal domain Taking into accountthat (i) the FO of C superbus occurs in the middle partof the TenuicostatumPolymorphum Zone in most ofthe Tethyan sections and (ii) the duration between thebase of the Toarcian and the FO of C superbus rangesfrom 051 to 063 myr at Foum Tillicht and Penichewe suggest placing the FO of C superbus (and conse-quently the base of the NJT6 calcareous nannofossilZone) in the Tethyan domain to ~ 055 myr after thebeginning of the TenuicostatumPolymorphum Zonein the next compilation of the Geological Time Scale

57 Environmental disturbances during the P-To and its impact on the astrochronology of the Toarcian Stage

The hiatus observed at the boundary between the Poly-morphum and the Levisoni zones in the Foum Tillichtsection represents a time span of 01ndash02 myr In addi-tion an interval of decreasing δ13Ccarb values in lower -most part of the Levisoni Zone is observed at Penicheand Amellago but is missing in the δ13Corg series atFoum Tillicht (Fig 4) By correlation with Penichethis hiatus represents a total time of 023ndash033 myr notpreserved at Foum Tillicht This time interval notably

corresponds to the phase of gently decreasing δ13Cvalues observed at the top of the Polymorphum Zonein bulk rock belemnites and wood in the Peniche sec-tion (Hesselbo et al 2007 Pittet et al 2014) Theδ13Ccarb from the Foum Tillicht section cannot be di-rectly compared with Peniche since it represents thelocal dynamics of the basin (Bodin et al 2016) but thetrends of the δ13Corg are less affected by mixing effectof δ13C from the carbonate platform and can thus beused for global correlations The δ13Corg only showsthe trend towards increasing values in the Tenuicosta-tum Zone then sharply decrease by 75permil at the hiatuslevel (Fig 4) The phase of gently decreasing values ofδ13C observed in the Peniche section from cycle 9 tocycle 10 is thus missing in the Foum Tillicht sectionThe stable trend of bulk rock and wood δ13C observedin the middle part of the Peniche section is not ob-served in the Foum Tillicht section (Figs 4 9 Hessel-bo et al 2007) This phase starts below the FO of C su-perbus and the fact that the FO of C superbus is foundin the middle part of the Polymorphum Zone in theFoum Tillicht section as well as at Peniche is incom-patible with a hiatus spanning the whole second half of the Polymorphum Zone This is rather linked to var-ious trends in the δ13C values as suggest the correla-tion of δ13C curves between Central High Atlas sec-tions and Peniche (Bodin et al 2010 2016) The δ13Cvalues from belemnite guards display at Peniche asimilar trend as the δ13Corg from the Foum Tillicht sec-tion with an increasing phase immediately followedby a gently decreasing phase lasting ~ 015 myr (Hes-selbo et al 2007) which is close to the trend of δ13Corg

observed at Foum TillichtThe hiatus observed in the Foum Tillicht section

spans the time interval from the upper part of the Poly-morphum Zone to the lower Levisoni Zone (Fig 4)Two discontinuities have been defined within this timeinterval in the Lusitanian Basin and then correlatedthroughout Euro-Boreal and Tethyan domains (Pittetet al 2014 Ruebsam et al 2014) Discontinuity D2 isan erosion surface that corresponds to the developmentof marine erosion in offshore environments as a con-sequence of a major sea-level drop while discontinu-ity D3 is a condensed or non-deposition surface relatedto a major transgression The merging of D2 and D3as observed in the Foum Tillicht section and in someparts of the Lusitanian Basin has been interpreted asthe consequence of marine erosional processes duringthe sea-level drop followed by the development of aravinement surface during the early phase of the fol-lowing major transgression (Pittet et al 2014)


It is noteworthy that the Foum Tillicht section is notaffected by phase D1 occurring at the PliensbachianndashToarcian boundary This phase corresponds to a se-quence condensed or lacking in multiple offshore sec-tions due to basin starvation during a transgressionevent starting at the base of the Toarcian (Pittet et al2014) In contrast to European sections the deep ma-rine sections of the High Atlas Basin show expandedsedimentation rates Higher nutrient levels and fluvial-derived siliciclastic inputs were observed at the P-Toboundary of shallow and deep marine sections likelyrelated to higher continental weathering (Bodin et al2010 Bodin et al 2011 Krencker et al 2015) Higherlevels of detrital supply are indeed commonly observedwith increase of continental weathering (Mutterloseand Ruffell 1999 Moiroud et al 2012) As such in-creasing levels of detrital supply at the P-To boundarywould have thus provided sediment supply to deep-ma-rine sections in the High-Atlas Basin therefore pre-venting these sections from basin starvation

58 Further extensions in the Pliensbachian

From the base of the series to 10960 m two mainbands of periods are observed the first band rangingfrom 23 m to 13 m and the second from 76 m to 45 m(see the spectrograms on Fig 5) These periods are attributed to the 405-kyr eccentricity and the 100-kyreccentricity although the band of period 76 to 45 mis under the confidence levels on the multi-taper spec-trum (Fig 6) The sample spacing in the Foum Tillichtsection from the base of the succession to 10960 mranges from 035 m to 275 m with an average of15 m which limits the exploration of the high fre-quencies Considering the sampling density in this in-terval the band of 100-kyr eccentricity contains ~ 3ndash4samples per 100-kyr eccentricity which is not enoughto accurately observe the amplitude of the 100-kyr cycle Notably 4 to 10 samples per cycle are needed toaccurately describe the amplitude of a cycle otherwisethe amplitude of the targeted cycle should be dimin-ished and its frequency affected (Herbert 1994 Mar-tinez et al 2016) The only cycle correctly describedfrom the base of the series to 10937 m is the cycle at-tributed to the 405-kyr eccentricity

The recognition of the 405-kyr eccentricity cycle inthis part of the series allows significant differenceswith the GTS 2012 to be observed in the biozone du-rations In the Pliensbachian part of the series the FOof Lotharingius sigillatus is observed at least 155 myr

before the base of the Toarcian Stage The GTS 2012positions this event at the base of the Tenuicostatumammonite Zone following the biochronostratigraphicchart in Hardenbol et al (1998) (details can be foundin Time Scale Creator 64) Mattioli and Erba (1999)noticed sporadic occurrence of L sigillatus in the LatePliensbachian In the Lusitanian Basin and in NorthernSpain the FO of L sigillatus is reported within theSpinatumEmaciatum Zone (Reggiani et al 2010Mattioli et al 2013 Fraguas et al 2015 Fig 2) As forthe FO of C superbus it appears with these new datathat there is a mismatch between the bioevents frombiostratigraphic data and the bioevents reported in theGTS 2012 (Figs 2 3) Consequently the average du-ration of the NJT5b Subzone assessed here at 207 myris much longer than the 107-myr duration of theNJT5b Subzone reported in the GTS 2012 (Gradsteinet al 2012) Due to the sampling density of nanno -fossil assemblage analyses the position of the FO ofL sigillatus shows an uncertainty of at least 164 mwhich represents a time span of 043 myr The orbitalchronology provided in the Foum Tillicht sectionnonetheless shows that the duration of the NJT5b issignificantly underestimated in the GTS 2012

Other differences are observed in the duration esti-mates of the Emaciatum Zone and the Spinatum ZoneThe duration estimated here for the Emaciatum Zoneis 2044 0318 myr the uncertainty being related tothe uncertainty of the position of the base of the Ema-ciatum Zone (Fig 4) Conversely the GTS 2012 pro-vides a duration estimate of the Emaciatum Zone of079 myr (Gradstein et al 2012) Ammonite-zone du-rations of the Late Pliensbachian are based on therecognition of the precession in Italy and Englandproviding a minimum duration of the Spinatum Zonethen constrained on a linear trend of Sr-isotope ratiosfrom the Hettangian to the Pliensbachian (Weedon andJenkyns 1999 Weedon et al 1999) In the GTS 2012the base of the Emaciatum Zone was then located onthe upper third of the Apyrenum Subzone the firstsubzone of Spinatum Zone (Hardenbol et al 1998Gradstein et al 2012) This approach has at leastthree weaknesses Correlations between the Emacia-tum and the Spinatum zones are still unclear due to a strong provincialism between Mediterranean andEuro-boreal faunas (Dera et al 2011b) the calibrationbased on precession cycles can easily be affected byshort-term hiatuses (Weedon and Jenkyns 1999) andthe trend of Sr-isotope in not necessarily linear Envi-ronmental conditions such as modifications in the lev-els of continental weathering can modify the rate of

M Martinez et al64

change of Sr-isotope ratios at a time scale of ~ 100 myr(McArthur et al 2007 Kemp et al 2011 Bodin et al2015) Notably orbital calibrations of ammonite zonescan lead to higher or lower durations compared to du-rations calculated by linear trend of Sr-isotope ratios(e g Martinez et al 2012)

6 Conclusions

A new orbital chronology is provided for the Pliens-bachianndashToarcian transition performed for the firsttime in the expanded hemipelagic section of FoumTillicht from the Central High Atlas Basin (Morocco)Based on the recognition of the obliquity and 405-kyreccentricity cycles and correlations with Europeansections the duration of the Polymorphum Zone couldbe evaluated as 09ndash10 myr while the duration of theP-To event is estimated as 018ndash027 myr By corre -lating the orbital time scales from the Foum Tillichtand the Peniche sections the condensation phase D1have affected a time span of 01ndash02 myr of sedimentwhile the time missing at Foum Tillicht at the Poly-morphumndashLevisoni boundary is assessed as 023ndash033 myr Although the orbital chronology of both sec-tions is impacted by the major environmental changesrecorded in the Early Toarcian an integrated approachdecreased the impact of local hiati or condensed inter-vals on the construction of the orbital time scale Fi-nally the record of the 405-kyr eccentricity cycle inthe Pliensbachian part of the series allowed the aver-age minimum duration of the NJ5b calcareous nanno-fossil zone to be assessed at 207 myr while the dura-tion of the Emaciatum zone is estimated as 205

032 myr Although weak biostratigraphic control onthe Pliensbachian part of the series affects the two lat-ter durations these are significantly longer than in theGeological Time Scale 2012 and highlight the poten-tial of the expanded sections of the High Atlas Basinto provide a reliable orbital time scale of the Pliens-bachian Stage

Acknowledgements Mathieu Martinez is supplied byEuropean Research Council (ERC) Consolidated GrantEarthSequencing Steacutephane Bodin and Franccedilois-NicolasKrencker are supplied by the Deutsche Forschungsgemein-schaft (DFG project ndeg BO 36551-1) We would like tothank Prof Andreacute Strasser Dr Markus Wilmsen and ananonymous reviewer for their very constructive and positivecomments Will Brocas is also acknowledged for English-proof reading as well as Dr Jochen Erbacher for having edited the manuscript

References

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Bassoullet J-P and Baudin F 1994 Le Toarcien infeacuterieurune peacuteriode de crise dans les bassins et sur les plate-formes carbonateacutees de lrsquoEurope du Nord-Ouest et de laTeacutethys Geobios 17 645ndash654

Bilotta M Venturi F Sassaroli S 2010 Ammonite fau-nas OAE and the PliensbachianndashToarcian boundary(Early Jurassic) in the Apennines Lethaia 43 357ndash380

Bodin S Froumlhlich S Boutib L Lahsini S Redfern J2011 Early Toarcian source-rock potential in the CentralHigh Atlas Basin (central Morocco) regional distributionand depositional model Journal of Petroleum Geology34 345ndash363

Bodin S Krencker F-N Kothe T Hoffmann R Matti-oli E Heimhofer U Lahcen K 2016 Perturbation ofthe carbon cycle during the late PliensbachianndashearlyToarcian New insight from high-resolution carbon iso-tope records in Morocco Journal of African Earth Sci-ences 116 89ndash104

Bodin S Mattioli E Froumlhlich S Marshall J D BoutibL Lahsini S Redfern J 2010 Toarcian carbon isotopeshifts and nutrient changes from the Northern margin ofGondwana (High Atlas Morocco Jurassic) Palaeoenvi-ronmental implications Palaeogeography Palaeoclima-tology Palaeoecology 297 377ndash390

Bodin S Meissner P Janssen N M M Steuber T Mut-terlose J 2015 Large igneous provinces and organiccarbon burial Controls on global temperature and conti-nental weathering during the Early Cretaceous Globaland Planetary Change 133 238ndash253

Boomer I Lord A Page K Bown P Lowry F RidingJ B 2009 The biostratigraphy of the Upper Pliensbachi-anndashToarcian (Lower Jurassic) sequence at IlminsterSomerset Journal of Micropalaeontology 28 67ndash85

Boulila S Galbrun B Huret E Hinnov L A Rouget IGardin S Bartolini A 2014 Astronomical calibrationof the Toarcian Stage Implications for sequence strati -graphy and duration of the early Toarcian OAE Earth andPlanetary Science Letters 386 98ndash111

Bown P and Cooper M 1998 Jurassic In Bown P(Eds) Calcareous nannofossil biostratigraphy KluwerAcademy London 34ndash85

Brazier J-M Suan G Tacail T Simon L Martin J EMattioli E Balter V 2015 Calcium isotope evidencefor dramatic increase of continental weathering duringthe Toarcian oceanic anoxic event (Early Jurassic) Earthand Planetary Science Letters 411 164ndash176

Bucefalo Palliani R Mattioli E Riding J B 2002 Theresponse of marine phytoplankton and sedimentary or-ganic matter to the early Toarcian (Lower Jurassic)


oceanic anoxic event in northern England Marine Micro -paleontology 46 223ndash245

Cariou E and Hantzpergue P 1997 Biostratigraphie duJurassique ouest-europeacuteen et meacutediterraneacuteen zonationsparrallegraveles et distribution des inverteacutebreacutes et microfossilesBulletin des Centres de Recherches Exploration-Produc-tion Elf Aquitaine Meacutemoire 17 422 pp

Caruthers A H Smith P L Groumlcke D R 2013 ThePliensbachianndashToarcian (Early Jurassic) extinction aglobal multi-phased event Palaeogeography Palaeocli-matology Palaeoecology 386 104ndash118

Cohen A S Coe A L Harding S M Schwark L 2004Osmium isotope evidence for the regulation of atmos-pheric CO2 by continental weathering Geology 32 157ndash160

Cramer B S Wright J D Kent D V Aubry M P 2003Orbital climate forcing of δ13C excursions in the late Paleocenendashearly Eocene (chrons C24nndashC25n) Paleo-ceanography 18 1097

De Graciansky P-C Dardeau G Dommergues J-LDurlet C Marchand D Dumont T Hesselbo S PJacquin T Goggin V Meister C Mouterde R ReyJ Vail P R 1998 Ammonite biostratigraphic correla-tion and Early Jurassic sequence stratigraphy in Francecomparisons with some UK sections In de GracianskyP-C Hardenbol J Jacquin T Vail P R (Eds) Meso-zoic and Cenozoic Sequence Stratigraphy of EuropeanBasins 60 SEPM Special Publications Tulsa OK USA583ndash622

De Vleeschouwer D Parnell A C 2014 Reducing time-scale uncertainty for the Devonian by integrating astro -chronology and Bayesian statistics Geology 42 491ndash494

Dera G Brigaud B Monna F Laffont R Puceat EDeconinck J F Pellenard P Joachimski M M DurletC 2011a Climatic ups and downs in a disturbed Jurassicworld Geology 39 215ndash218

Dera G Neige P Dommergues J-L Brayard A 2011bAmmonite paleobiogeography during the PliensbachianndashToarcian crisis (Early Jurassic) reflecting paleoclimateeustasy and extinctions Global and Planetary Change78 92ndash105

Dera G Pellenard P Neige P Deconinck J-F Puceacuteat EDommergues J-L 2009 Distribution of clay minerals inEarly Jurassic Peritethyan seas Palaeoclimatic signifi-cance inferred from multiproxy comparisons Palaeogeog-raphy Palaeoclimatology Palaeoecology 271 39ndash51

Dromart G Allemand P Garcia J-P Robin C 1996Variation cyclique de la production carbonateacutee au Juras-sique le long drsquoun transect Bourgogne-Ardegraveche Est-France Bulletin de la Socieacuteteacute geacuteologique de France 167423ndash433

Du Dresnay R 1971 Extension et deacuteveloppement despheacutenomegravenes reacutecifaux jurassiques dans le domaine at-lasique marocain particuliegraverement au Lias moyen Bul-letin de la Socieacuteteacute geacuteologique de France 46ndash56

Elmi S 2009 PliensbachianndashToarcian boundary ndash the pro-posed GSSP of Peniche Ciecircncias da Terra (UNL) 16 7ndash16

Fraguas Aacute Comas-Rengifo M J Perilli N 2015 Cal-careous nannofossil biostratigraphy of the Lower Jurassicin the Cantabrian Range (Northern Spain) Newsletterson Stratigraphy 48 179ndash199

Frizon de Lamotte D Zizi M Missenard Y Hafid MEl Azzouzi M Maury R C Charriegravere A Taki Z Benammi M Michard A 2008 The Atlas System InMichard A Saddiqi O Chalouan A Frizon de Lam-otte D (Eds) Continental Evolution The Geology ofMorocco Lecture Notes in Earth Sciences 116 Springer-Verlag Berlin 133ndash202

Giorgioni M Weissert H Bernasconi S M HochuliP A Coccioni R Keller C E 2012 Orbital control oncarbon cycle and oceanography in the mid-Cretaceousgreenhouse Paleoceanography 27 PA1204

Giraud F Reboulet S Deconinck J-F Martinez MCarpentier A Breacuteziat C 2013 The Mid-CenomanianEvent in southeastern France Evidence from palaeonto-logical and clay mineralogical data Cretaceous Research46 43ndash58

Gradstein F M Ogg J G Schmitz M Ogg G 2012The Geologic Time Scale 2012 Elsevier B V pp 1176

Greacuteselle B Pittet B Mattioli E Joachimski M Bar-barin N Riquier L Reboulet S Puceacuteat E 2011 TheValanginian isotope event A complex suite of palaeoen-vironmental perturbations Palaeogeography Palaeocli-matology Palaeoecology 306 41ndash57

Gueacuterin-Franiatte S Maquil R Muumlnzberger P 2010 LeToarcien au Grand-Ducheacute de Luxembourg Biostratigra-phie dans la reacutegion de Belvaux In Weis R and Gueacuterin-Franiatte S (Eds) Le Jurassique infeacuterieur et moyen auLuxembourg Ferrantia 62 Museacutee national drsquohistoire na-turelle Luxembourg Luxembourg 19ndash34

Hardenbol J Thierry J Farley M B Jacquin T de Gra-ciansky P-C Vail P R 1998 Mesozoic and CenozoicSequence Stratigraphic Framework of European BasinsIn de Graciansky P-C Hardenbol J Jacquin T VailP R (Eds) Mesozoic and Cenozoic Sequence Stratigra-phy of European Basins 60 SEPM Special PublicationsTulsa OK USA 3ndash13

Hoedemaeker P J 1998 Berriasian-Barremian sequencesin the Riacuteo Argos succession near Caravaca (SoutheastSpain) and their correlation with some sections in South-east France In de Graciansky P-C Hardenbol JJacquin T Vail P R (Eds) Mesozoic and Cenozoic Se-quence Stratigraphy of European Basins SEPM SpecialPublications 60 Society for Sedimentary Geology TulsaUSA pp 423ndash441

Herbert T D 1994 Reading orbital signals distorted bysedimentation models and examples In de Boer P Land Smith D G (Eds) Orbital Forcing and Cyclic Se-quences 19 SEPM Special Publications Tulsa OKUSA 483ndash507

Hesselbo S P 2008 Sequence stratigraphy and inferred rel-ative sea-level change from the onshore British JurassicProceedings of the Geologistsrsquo Association 119 19ndash34

Hesselbo S P and Jenkyns H C 1998 British lowerJurassic sequence stratigraphy In de Graciansky P C

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Hardenbol J Jacquin T Vail P R (Eds) Mesozoicand Cenozoic Sequence Stratigraphy of European Basins60 SEPM Special Publications Tulsa OK USA 561ndash581

Hesselbo S P Jenkyns H C Duarte L V OliveiraL C V 2007 Carbon-isotope record of the Early Juras-sic (Toarcian) Oceanic Anoxic Event from fossil woodand marine carbonate (Lusitanian Basin Portugal) Earthand Planetary Science Letters 253 455ndash470

Huang C and Hesselbo S P 2014 Pacing of the ToarcianOceanic Anoxic Event (Early Jurassic) from astronomicalcorrelation of marine sections Gondwana Research 251348ndash1356

Huang C Hinnov L Ogg J Galbrun B Boulila SHuret E 2010 Astronomical calibration of the Jurassictime scale Earth Science Frontiers 17 108ndash109

Huybers P and Denton G 2008 Antarctic temperature atorbital timescales controlled by local summer durationNature Geoscience 1 787ndash792

Jenkyns H C 1988 The early Toarcian (Jurassic) anoxicevent stratigraphic sedimentary and geochemical evi-dence American Journal of Science 288 101ndash151

Jenkyns H C 2003 Evidence for rapid climate change inthe MesozoicndashPalaeogene greenhouse world Philosoph-ical Transactions of the Royal Society of London AMathematical Physical and Engineering Sciences 3611885ndash1916

Kemp D B Coe A L Cohen A S Weedon G P 2011Astronomical forcing and chronology of the early Toar-cian (Early Jurassic) oceanic anoxic event in YorkshireUK Paleoceanography 26 PA4210

Korte C and Hesselbo S P 2011 Shallow marine carbonand oxygen isotope and elemental records indicate ice-house-greenhouse cycles during the Early Jurassic Pale-oceanography 26 PA4219

Krencker F-N Bodin S Suan G Heimhofer U KabiriL Immenhauser A 2015 Toarcian extreme warmth ledto tropical cyclone intensification Earth and PlanetaryScience Letters 425 120ndash130

Krencker F-N Bodin S Hoffmann R Suan G Mat -tioli E Kabiri L Foumlllmi K B Immenhauser A 2014The middle Toarcian cold snap Trigger of mass extinc-tion and carbonate factory demise Global and PlanetaryChange 117 64ndash78

Laskar J Fienga A Gastineau M Manche H 2011La2010 a new orbital solution for the long-term motionof the Earth Astronomy amp Astrophysics 532 A89

Laskar J Robutel P Joutel F Gastineau M CorreiaA C M Levrard B 2004 A long-term numerical solu-tion for the insolation quantities of the Earth Astronomyand Astrophysics 428 261ndash285

Laurin J Meyers S R Uličnyacute D Jarvis I SagemanB B 2015 Axial obliquity control on the greenhousecarbon budget through middle- to high-latitude reser-voirs Paleoceanography 30 133ndash149

Leacuteonide P Floquet M Durlet C Baudin F Pittet BLeacutecuyer C 2012 Drowning of a carbonate platform asa precursor stage of the Early Toarcian global anoxic

event (Southern Provence sub-Basin South-east France)Sedimentology 59 156ndash184

Little C T and Benton M J 1995 Early Jurassic mass ex-tinction a global long-term event Geology 23 495ndash498

Lourens L Hilgen F Shackleton N Laskar J WilsonD 2004 The Neogene Period In (Eds) A geologic timescale 2004 409ndash440

Mailliot S Mattioli E Guex J Pittet B 2006 The EarlyToarcian anoxia a synchronous event in the WesternTethys An approach by quantitative biochronology(Unitary Associations) applied on calcareous nannofos-sils Palaeogeography Palaeoclimatology Palaeoecology240 562ndash586

Mann M E and Lees J M 1996 Robust estimation ofbackground noise and signal detection in climatic timeseries Climatic Change 33 409ndash445

Martinez M Deconinck J-F Pellenard P Reboulet SRiquier L 2013 Astrochronology of the ValanginianStage from reference sections (Vocontian Basin France)and palaeoenvironmental implications for the WeissertEvent Palaeogeography Palaeoclimatology Palaeoecol-ogy 376 91ndash102

Martinez M Deconinck J-F Pellenard P Riquier LCompany M Reboulet S Moiroud M 2015 Astro -chronology of the ValanginianndashHauterivian stages (EarlyCretaceous) Chronological relationships between theParanaacutendashEtendeka large igneous province and the Weis-sert and the Faraoni events Global and Planetary Change131 158ndash173

Martinez M and Dera G 2015 Orbital pacing of carbonfluxes by a ~ 9-My eccentricity cycle during the Meso-zoic Proceedings of the National Academy of Sciencesof the United States of America 112 12604ndash12609

Martinez M Kotov S De Vleeschouwer D Pas D Pauml-like H 2016 Testing the impact of stratigraphic uncer-tainty on spectral analyses of sedimentary time seriesClimate of the Past Discussions doi105194cp-2015-188

Martinez M Pellenard P Deconinck J-F Monna FRiquier L Boulila S Moiroud M Company M2012 An orbital floating time scale of the HauterivianBarremian GSSP from a magnetic susceptibility signal(Riacuteo Argos Spain) Cretaceous Research 36 106ndash115

Mattioli E and Erba E 1999 Synthesis of calcareous nan-nofossil events in Tethyan Lower and Middle Jurassicsuccessions Rivista Italiana di Paleontologia e Strati-grafia 105 343ndash376

Mattioli E and Pittet B 2004 Spatial and temporal distri-bution of calcareous nannofossils along a proximalndashdis-tal transect in the Lower Jurassic of the UmbriandashMarcheBasin (central Italy) Palaeogeography Palaeoclimatol-ogy Palaeoecology 205 295ndash316

Mattioli E Pittet B Bucefalo Palliani R Roumlhl H-JSchmid-Roumlhl A Morettini E 2004 Phytoplankton ev-idence for the timing and correlation of palaeoceano-graphical changes during the early Toarcian oceanicanoxic event (early Jurassic) Journal of the GeologicalSociety London 161 685ndash693


Mattioli E Plancq J Boussaha M Duarte L V PittetB 2013 Calcareous nannofossil biostratigraphy newdata from the Lower Jurassic of the Lusitanian Basin Co-municaccedilotildees Geoloacutegicas 100 69ndash76

McArthur J M Janssen N M M Reboulet S LengM J Thirlwall M F van de Schootbrugge B 2007Palaeotemperatures polar ice-volume and isotope stra ti -graphy (MgCa δ18O δ13C 87Sr86Sr) The Early Creta-ceous (Berriasian Valanginian Hauterivian) Pa laeo geo -graphy Palaeoclimatology Palaeoecology 248 391ndash430

Meyers S R 2012 Seeing red in cyclic stratigraphy Spec-tral noise estimation for astrochronology Paleoceanogra-phy 27 PA3228

Meyers S R 2014 astrochron An R Package for Astro -chronology httpcranr-projectorgpackage=astrochron

Milhi A Ettaki M Chellai E Hadri M 2002 Les for-mations lithostratigraphiques jurassiques du Haut-Atlascentral (Maroc) correacutelations et reconstitutions paleacuteogeacuteo-graphiques Revue de Paleacuteobiologie 21 241ndash256

Moiroud M Martinez M Deconinck J-F Monna FPellenard P Riquier L Company M 2012 High-res-olution clay mineralogy as a proxy for orbital tuning Ex-ample of the HauterivianndashBarremian transition in theBetic Cordillera (SE Spain) Sedimentary Geology 282336ndash346

Mouterde R 1955 Le Lias de Peniche Comunicaccedilotildees dosServiccedilos Geoloacutegicos de Portugal 36 1ndash33

Mutterlose J and Ruffell A 1999 Milankovitch-scalepalaeoclimate changes in palendashdark bedding rhythmsfrom the Early Cretaceous (Hauterivian and Barremian)of eastern England and northern Germany Palaeogeogra-phy Palaeoclimatology Palaeoecology 154 133ndash160

Oehlert A M Lamb-Wozniak K A Devlin Q B Mac -kenzie G J Reijmer J J Swart P K 2012 The stablecarbon isotopic composition of organic material in plat-form derived sediments implications for reconstructingthe global carbon cycle Sedimentology 59 319ndash335

Page K N 2003 The Lower Jurassic of Europe its sub -division and correlation Geological Survey of Denmarkand Greenland Bulletin 1 23ndash59

Paumllike H Norris R D Herrle J O Wilson P A CoxallH K Lear C H Shackleton N J Tripati A K WadeB S 2006 The heartbeat of the Oligocene climate sys-tem Science 314 1894ndash1898

Pellenard P Nomade S Martire L De Oliveira RamalhoF Monna F Guillou H 2013 The first 40Arndash39Ardate from Oxfordian ammonite-calibrated volcanic layers(bentonites) as a tie-point for the Late Jurassic Geologi-cal Magazine 150 1136ndash1142

Perilli N 1999 Calibration of EarlyndashMiddle Toarcian nan-nofossil events in two expanded and continuous sectionsfrom the Basque-Cantabrian area (Northern Spain) Re-vista Espantildeola de Micropaleontologiacutea 31 393ndash401

Perilli N 2000 Calibration of earlyndashmiddle Toarcian nan-nofossil events based on high-resolution ammonite bio -stratigraphy in two expanded sections from the IberianRange (East Spain) Marine Micropaleontology 39 293ndash308

Perilli N Comas-Rengifo M J Goy A 2004 Calibrationof the PliensbachianndashToarcian calcareous nannofossilzone boundaries based on ammonites (Basque-Cantabri-an area Spain) Rivista Italiana di Paleontologia e Strati-grafia 110 97ndash107

Piqueacute A Tricart P Guiraud R Laville E Bouaziz SAmrhar M Ait Ouali R 2002 The MesozoicndashCeno-zoic Atlas belt (North Africa) an overview GeodinamicaActa 15 185ndash208

Pittet B Suan G Lenoir F Duarte L V Mattioli E2014 Carbon isotope evidence for sedimentary disconti-nuities in the lower Toarcian of the Lusitanian Basin (Por-tugal) Sea level change at the onset of the Oceanic Anox-ic Event Sedimentary Geology 303 1ndash14

Reggiani L Mattioli E Pittet B Duarte L V Veiga de Oliveira L C Comas-Rengifo M J 2010 Pliens-bachian (Early Jurassic) calcareous nannofossils from thePeniche section (Lusitanian Basin Portugal) A clue forpalaeoenvironmental reconstructions Marine Micropale-ontology 75 1ndash16

Rocha R B Mattioli E Duarte L V Pittet B Elmi SMouterde R Cabral M C Comas-Rengifo M JGoacutemez J J Goy A Hesselbo S P Jenkyns H C Litt -ler K Mailliot S Veiga de Oliveira L C Osete M LPerilli N Pinto S Ruget C Suan G 2016 Base ofthe Toarcian Stage of the Lower Jurassic defined by theGlobal Boundary Stratotype Section and Point (GSSP) atthe Peniche section (Portugal) Episodes 39 460ndash481

Ruebsam W Muumlnzberger P Schwark L 2014 Chronol-ogy of the Early Toarcian environmental crisis in the Lor-raine Sub-Basin (NE Paris Basin) Earth and PlanetaryScience Letters 404 273ndash282

Sabatino N Neri R Bellanca A Jenkyns H C BaudinF Parisi G Masetti D 2009 Carbon-isotope recordsof the Early Jurassic (Toarcian) oceanic anoxic eventfrom the Valdorbia (UmbriandashMarche Apennines) andMonte Mangart (Julian Alps) sections palaeoceano-graphic and stratigraphic implications Sedimentology56 1307ndash1328

Suan G Mattioli E Pittet B Leacutecuyer C Sucheacuteras-Marx B Duarte L V Philippe M Reggiani L Mar-tineau F 2010 Secular environmental precursors to Ear-ly Toarcian (Jurassic) extreme climate changes Earth andPlanetary Science Letters 290 448ndash458

Suan G Mattioli E Pittet B Mailliot S Leacutecuyer C2008a Evidence for major environmental perturbationprior to and during the Toarcian (Early Jurassic) oceanicanoxic event from the Lusitanian Basin Portugal Paleo-ceanography 23 PA1202

Suan G Pittet B Bour I Mattioli E Duarte L Mail-liot S 2008b Duration of the Early Toarcian carbon iso-tope excursion deduced from spectral analysis Conse-quence for its possible causes Earth and Planetary Sci-ence Letters 267 666ndash679

Swart P K 2008 Global synchronous changes in the car-bon isotopic composition of carbonate sediments unrelat-ed to changes in the global carbon cycle Proceedings ofthe National Academy of Sciences 105 13741ndash13745

M Martinez et al68

Swart P K and Eberli G 2005 The nature of the δ13C ofperiplatform sediments implications for stratigraphy andthe global carbon cycle Sedimentary Geology 175 115ndash129

Trecalli A Spangenberg J Adatte T Foumlllmi K B Pa -rente M 2012 Carbonate platform evidence of oceanacidification at the onset of the early Toarcian oceanicanoxic event Earth and Planetary Science Letters 357ndash358 214ndash225

Vennari V V Lescano M Naipauer M Aguirre-UrretaB Concheyro A Schaltegger U Armstrong R Pimen -tel M Ramos V A 2014 New constraints on the Juras-sicndashCretaceous boundary in the High Andes using high-precision U-Pb data Gondwana Research 26 374ndash385

Voigt S Aurag A Leis F Kaplan U 2007 Late Ceno-manian to Middle Turonian high-resolution carbon iso-tope stratigraphy New data from the Muumlnsterland Creta-ceous Basin Germany Earth and Planetary Science Let-ters 253 196ndash210

Wang P Tian J Lourens L J 2010 Obscuring of longeccentricity cyclicity in Pleistocene oceanic carbon iso-tope records Earth and Planetary Science Letters 290319ndash330

Weedon G P and Jenkyns H C 1999 Cyclostratigraphyand the Early Jurassic timescale Data from the Belemnite

Marls Dorset southern England Geological Society ofAmerica Bulletin 111 1823ndash1840

Weedon G P Jenkyns H C Coe A L Hesselbo S P1999 Astronomical calibration of the Jurassic time-scalefrom cyclostratigraphy in British mudrock formationsPhilosophical Transactions of the Royal Society of Lon-don A Mathematical Physical and Engineering Sciences357 1787ndash1813

Wilmsen M Blau J Meister C Mehdi M NeuweilerF 2002 Early Jurassic (Sinemurian to Toarcian) am-monites from the central High Atlas (Morocco) betweenEr-Rachidia and Rich Revue de Paleacuteobiologie 21 149ndash175

Wilmsen M Neuweiler F 2008 Biosedimentology of theEarly Jurassic post-extinction carbonate depositional sys-tem central High Atlas rift basin Morocco Sedimentol-ogy 55 773ndash807

Zachos J C Shackleton N J Revenaugh J S Paumllike HFlower B P 2001 Climate response to orbital forcingacross the OligocenendashMiocene boundary Science 292274ndash278

Manuscript received January 11 2016Revised version accepted August 30 2016


1 Introduction

The construction of a robust Geological Time Scale is of critical importance for assessing the rhythms ofgeodynamic changes palaeoceanographic and palaeo-climatic processes The last update of the GeologicalTime Scale 2012 (GTS 2012 Gradstein et al 2012) hasshown to contain some non-negligible uncertaintieswhich can reach several millions of years (Pellenard etal 2013 De Vleeschouwer and Parnell 2014 Vennariet al 2014 Martinez et al 2015) Yet the developmentof extended astrochronological frameworks has al-ready contributed to the construction of a robust geo-logical time frame for the Cenozoic (e g Lourens et al2004) The construction of new astrochronologicalframeworks are currently extended for Jurassic andCretaceous successions in order to decrease the timeuncertainty of those periods by at least one order ofmagnitude (Weedon and Jenkyns 1999 Huang et al2010 Martinez et al 2015)

One of the critical intervals of the Jurassic Period isthe PliensbachianndashToarcian transition This time in-terval is affected by two global palaeoenvironmentalchanges respectively at the PliensbachianndashToarciantransition (the PliensbachianndashToarcian event or P-Toevent) and the Toarcian oceanic anoxic event (T-OAE)at the base of the LevisoniSerpentinum Zone Theseevents are characterised by excursions in the δ13Crecords (Hesselbo et al 2007 Suan et al 2008a Bodinet al 2010 2016) increased accumulation of organicmatter observed during the T-OAE (e g Jenkyns1988) higher levels of continental weathering and nutrient supply (Cohen et al 2004 Dera et al 2009Bodin et al 2010 2011) demise of the carbonate plat-form factories (Bassoullet and Baudin 1994 Suan etal 2008a Wilmsen and Neuweiler 2008 Leacuteonide et al2012 Krencker et al 2014) and extinction events af-fecting marine invertebrates (Little and Benton 1995Caruthers et al 2013) These environmental changeswere further accompanied by major changes inpalaeotemperature (Jenkyns 2003 Suan et al 2008a2010 Dera et al 2011a) and sea level (Hesselbo 2008Sabatino et al 2009 Suan et al 2010 and referencestherein Pittet et al 2014) likely linked to the growthand decay of polar ice caps (Suan et al 2010 Korteand Hesselbo 2011) All these environmental changestriggered major turnovers in facies environment andor sedimentation rate (Bassoullet and Baudin 1994 deGraciansky et al 1998 Hesselbo and Jenkyns 1998Leacuteonide et al 2012 Pittet et al 2014 Ruebsam et al2014) Major sea-level changes are notably responsi-

ble for the recurrence of condensed intervals and hiatalsurfaces recorded in the early Toarcian (Leacuteonide et al2012 Pittet et al 2014) As a consequence attempts tobuild a robust time scale in this time interval led to diverging astrochronological interpretations (Suan etal 2008b Kemp et al 2011 Huang and Hesselbo2014 Ruebsam et al 2014) The first ammonite zoneof the Toarcian (i e the Tenuicostatum or Polymor-phum Zone) is particularly representative of this de-bate duration estimates based on orbital time scalesfluctuating over almost two orders of magnitude from009 myr to ~ 115 myr (Mattioli and Pittet 2004 Suanet al 2008b Boulila et al 2014 Ruebsam et al 2014)The construction of high-resolution astrochronologi-cal frameworks ideally requires a continuous and ex-panded sedimentary record with a minimum of con-densation suggesting that the previously studied sec-tions were not suited for improving of the Pliensbachi-anndashToarcian time scale

The Central High Atlas Basin of Morocco has ex -perienced high tectonic subsidence in the Triassic renewed at a moderate rate during the Early Jurassic(Frizon de Lamotte et al 2008) As a result during the PliensbachianndashToarcian expanded sections weredeposited in hemipelagic environments (Bodin et al2011 2016) These sections are much expanded com-pared to the European sections reported at the Pliens-bachianndashToarcian transition which is expected to lim-it the occurrence of condensation or hiati

In the Foum Tillicht section spectral analyses havebeen performed on high-resolution δ13C and CaCO3

records covering the PliensbachianndashToarcian transi-tion In addition δ13C and CaCO3 were measured inthe Pliensbachian part of the series although at a lowerresolution which provides the opportunity to evaluatethe potential of the Foum Tillicht section to record thelong eccentricity cycle (405 kyr) Further we test if itcan be used as a reference section for further calibra-tions of the late Pliensbachian time scale

2 Geological setting

21 The Central High Atlas Basin

The Central High Atlas Basin is part of an Atlanticaulacogen rift system (Frizon de Lamotte et al 2008)This is a rift basin opened in the Triassic during thedislocation of Gondwana as the result of transtensivemovements A renewed phase of tectonic subsidencestarted in the late Pliensbachian (Frizon de Lamotte et

M Martinez et al48







50deg

40deg

30deg

20deg

10deg

0deg

-10deg-20deg

Tethys

Gondwana


MoroccanMeseta

Rif

Tell

Middle

Atlas

Oran Meseta

Central High

Atlas

Anti Atlas

Sahara

Atlas


westernHigh Atlas

Laurasia

A B

SaharaCraton


C D


Tagoudite Fm

Ouchbis Fm







M Martinez et al50

NJ5b

NJT6Carinolithus

superbus


Pleurocerasspinatum




NJT5app

NJ5b

NJT6






NJ5Tb

NJT6



Pleurocerasspinatum




NJT5app

NJ5b

NJT6pp



LatePliensbachian

pp

Early Toarcianpp

Substages

Stages



Hildaiteslevisoni





Pleurocerasspinatum




LatePliensbachian

pp

Early Toarcianpp




Pleurocerasspinatum



NJ5a

NJ5b

NJ6





Hildaiteslevisoni



Stages




NJT5a

NJ5Tb

NJT6



Tethyan (NJT)



-29 -28 -27 -26 -25 -24 -23 -22 -21-31 -30 -3 -2 -1 0 1 2 30 m

50

100

150

200

250

300

350

400

440



T-OAE

P-To event



RB

PLIE

NSB

AC

HIA

NTO

AR

CIA

N

Ouc

hbis

Fm

Ta

goud

ite F

m

Pol

ymo

Levi

soni

Em

acia

tum

Upp

erM

iddl

eU

pper

Low

er

Bifr

ons

Gra

data

Ago

udim

Fm

hiatus

Tauromeniceras sp


Lioceratoides sp

Eleganticeras sp






Alg

ov

Stu

died

inte

rval

(see

Fig

4)
















M Martinez et al52


CaC

O3

()

2030

4050

6070

stan

dard

ized

CaC

O3

+ E

cc 4

05 k

yr-2

-10

12

-2-1

01

2

stan

dard

ized

CaC

O3

+ O

bliq

uity

0 m

100

140


C superbus

13 C

(permil

PD

B)

-10

12

80120 40 2060

Ouchbis FmTagoud Fm

01

02

03

04

01

25

Fre

quen

cy(c

ycle

sm

)F

requ

ency

(cyc

les

m)

01

02

03

04

01

25

Fre

quen

cy(c

ycle

sm

)F

requ

ency

(cyc

les

m)

-20

2-2

02

Sta

ndar

dize

d 1

3 C+

Obl

iqui

ty

13241513211615

69

6345

7053

76

17

23

64



15

82

2315

41

~5392

5

16


173-kyr obliquity


obliquity


505 plusmn 44 kyr

AB

CD

EF

GH

IJ

StageAmmo Zone

Formation

L sigillatus


Sta

ndar

dize

d 1

3 C+

Ecc

405

kyr

P-To event

NJT5b NJT5aNJT6

Fig

5

Tim

e-fr

eque

ncy

spec

tral

ana

lyse

s an

d or

bita

l tun

ing

of th

e Fo

um T

illic

ht s

ectio

n A

Raw

δ13

C s

igna

l In

red

th

e lo

ng-t

erm

tren

d B

Tan

er lo

w-p

ass

filte

r of

the

405-

kyr

ecce

ntri

city

on

the

detr

ende

d δ13

C (

freq

uenc

y cu

t 1

038

10

ndash1

cycl

esm

ro

ll-of

f ra

te

1012

) C

Ta

ner

band

-pas

s fi

lter

of t

he o

bliq

uity

(lo

wer

fre

quen

cy c

ut

390

6

10ndash

1cy

cles

m u

pper

freq

uenc

y cu

t 7

935

10

ndash1

cycl

esm

rol

l-of

f rat

e 1

012)

D4

0-m

-win

dow

spe

ctro

gram

of t

he δ

13C

ser

ies

with

mai

n pe

riod

s la

belle

d in

met

ers

E1

5-m

-win

dow

spe

ctro

gram

of

the

δ13C

ser

ies

with

mai

n pe

riod

s la

belle

d in

met

ers

FR

aw C

aCO

3si

gnal

In

red

the

long

-ter

m t

rend

GT

aner

low

-pas

s fi

lter

of t

he40

5-ky

r ec

cent

rici

ty o

n th

e de

tren

ded

CaC

O3

(fre

quen

cy c

ut 7

324

10

ndash2

cycl

esm

rol

l-of

f ra

te 1

012)

HF

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of

the

obliq

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on

the

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ende

d C

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fre

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10

ndash1

cycl

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934

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J15

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e C

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ain

peri

ods

labe

lled

in m

eter

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4 Results

41 Geochemical data







M Martinez et al54




5 Discussion









M Martinez et al56

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86deg(038 m)

-94deg(005 m)

338deg(015 m)

223deg(008 m)

286deg(008 m)

-456deg(011 m)

115deg(003 m)

CaCO3 ()

10 20 30 40 50 60 70 80

13 C

(permil

PD

B)

-2

-15

-1

-05

0

05

1

15

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marl

limestone


A

B

C











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NJT5b 211 203 NA NA 207







M Martinez et al60

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2040

6080

wt

CaC

O3

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PLIENSBACHTOARCIAN


SigillatusSuperbus


Stage Amm

o Zon

eFor

mati

on

Calc n

anno

Zon

e

0 m51015202530354045

Leve

l (m

)

-20

2

13 C

bulk (

permil P

DB

)

-11

3

234567891011121314151617

CaC

O3

()

25

stan

d C

aCO

3

+ E

cc 4

05 k

yr

-2-1

01

2-2

-10

12

stan

d C

aCO

3

+ O

bliq

uity

100

140


C superbus1

3 C (

permil P

DB

)

-10

12

120

Ouchbis FmTagoud Fm

-20

2-2

02

Sta

nd

13C

+ O

bliq

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505 plusmn 44 kyr

Stage

Ammo ZoneFormation

5075

Sta

nd

13C

+ E

cc 4

05 k

yr

90130

110

105

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115

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Fou

m T

illic

ht (

this

stu

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iche

(Lu

sita

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123456789101112131415161718192122 2023 E1E2E3E4E5E6


405-kyr

100-kyr

obliquity

Hua

ng

et a

l (2

014)

1



tus

11

018 - 027 myr

117 plusmn 9 kyr

38 plusmn 6 kyr

Fig

9

Cor

rela

tion

of th

e as

troc

hron

olog

ical

fra

mew

orks

of

the

Foum

Till

icht

and

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om M

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(200

4)







M Martinez et al62















M Martinez et al64


6 Conclusions




References







































M Martinez et al66























































M Martinez et al68




















50deg

40deg

30deg

20deg

10deg

0deg

-10deg-20deg

Tethys

Gondwana


MoroccanMeseta

Rif

Tell

Middle

Atlas

Oran Meseta

Central High

Atlas

Anti Atlas

Sahara

Atlas


westernHigh Atlas

Laurasia

A B

SaharaCraton


C D


Tagoudite Fm

Ouchbis Fm







M Martinez et al50

NJ5b

NJT6Carinolithus

superbus


Pleurocerasspinatum




NJT5app

NJ5b

NJT6






NJ5Tb

NJT6



Pleurocerasspinatum




NJT5app

NJ5b

NJT6pp



LatePliensbachian

pp

Early Toarcianpp

Substages

Stages



Hildaiteslevisoni





Pleurocerasspinatum




LatePliensbachian

pp

Early Toarcianpp




Pleurocerasspinatum



NJ5a

NJ5b

NJ6





Hildaiteslevisoni



Stages




NJT5a

NJ5Tb

NJT6



Tethyan (NJT)



-29 -28 -27 -26 -25 -24 -23 -22 -21-31 -30 -3 -2 -1 0 1 2 30 m

50

100

150

200

250

300

350

400

440



T-OAE

P-To event



RB

PLIE

NSB

AC

HIA

NTO

AR

CIA

N

Ouc

hbis

Fm

Ta

goud

ite F

m

Pol

ymo

Levi

soni

Em

acia

tum

Upp

erM

iddl

eU

pper

Low

er

Bifr

ons

Gra

data

Ago

udim

Fm

hiatus

Tauromeniceras sp


Lioceratoides sp

Eleganticeras sp






Alg

ov

Stu

died

inte

rval

(see

Fig

4)
















M Martinez et al52


CaC

O3

()

2030

4050

6070

stan

dard

ized

CaC

O3

+ E

cc 4

05 k

yr-2

-10

12

-2-1

01

2

stan

dard

ized

CaC

O3

+ O

bliq

uity

0 m

100

140


C superbus

13 C

(permil

PD

B)

-10

12

80120 40 2060

Ouchbis FmTagoud Fm

01

02

03

04

01

25

Fre

quen

cy(c

ycle

sm

)F

requ

ency

(cyc

les

m)

01

02

03

04

01

25

Fre

quen

cy(c

ycle

sm

)F

requ

ency

(cyc

les

m)

-20

2-2

02

Sta

ndar

dize

d 1

3 C+

Obl

iqui

ty

13241513211615

69

6345

7053

76

17

23

64



15

82

2315

41

~5392

5

16


173-kyr obliquity


obliquity


505 plusmn 44 kyr

AB

CD

EF

GH

IJ

StageAmmo Zone

Formation

L sigillatus


Sta

ndar

dize

d 1

3 C+

Ecc

405

kyr

P-To event

NJT5b NJT5aNJT6

Fig

5

Tim

e-fr

eque

ncy

spec

tral

ana

lyse

s an

d or

bita

l tun

ing

of th

e Fo

um T

illic

ht s

ectio

n A

Raw

δ13

C s

igna

l In

red

th

e lo

ng-t

erm

tren

d B

Tan

er lo

w-p

ass

filte

r of

the

405-

kyr

ecce

ntri

city

on

the

detr

ende

d δ13

C (

freq

uenc

y cu

t 1

038

10

ndash1

cycl

esm

ro

ll-of

f ra

te

1012

) C

Ta

ner

band

-pas

s fi

lter

of t

he o

bliq

uity

(lo

wer

fre

quen

cy c

ut

390

6

10ndash

1cy

cles

m u

pper

freq

uenc

y cu

t 7

935

10

ndash1

cycl

esm

rol

l-of

f rat

e 1

012)

D4

0-m

-win

dow

spe

ctro

gram

of t

he δ

13C

ser

ies

with

mai

n pe

riod

s la

belle

d in

met

ers

E1

5-m

-win

dow

spe

ctro

gram

of

the

δ13C

ser

ies

with

mai

n pe

riod

s la

belle

d in

met

ers

FR

aw C

aCO

3si

gnal

In

red

the

long

-ter

m t

rend

GT

aner

low

-pas

s fi

lter

of t

he40

5-ky

r ec

cent

rici

ty o

n th

e de

tren

ded

CaC

O3

(fre

quen

cy c

ut 7

324

10

ndash2

cycl

esm

rol

l-of

f ra

te 1

012)

HF

ilter

of

the

obliq

uity

on

the

detr

ende

d C

aCO

3(l

ower

fre

quen

cycu

t 3

297

10

ndash1

cycl

esm

upp

er fr

eque

ncy

cut

934

1

10ndash

1cy

cles

m r

oll-

off r

ate

1012

) I

40-

m-w

indo

w s

pect

rogr

am o

f the

CaC

O3

with

mai

n pe

riod

s la

belle

d in

met

ers

J15

-m-w

indo

w s

pect

rogr

am o

f th

e C

aCO

3w

ith m

ain

peri

ods

labe

lled

in m

eter

s



4 Results

41 Geochemical data







M Martinez et al54




5 Discussion









M Martinez et al56

13

13

13

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13

E161 21 16 13 10 09 08

O (17) P (09)

86deg(038 m)

-94deg(005 m)

338deg(015 m)

223deg(008 m)

286deg(008 m)

-456deg(011 m)

115deg(003 m)

CaCO3 ()

10 20 30 40 50 60 70 80

13 C

(permil

PD

B)

-2

-15

-1

-05

0

05

1

15

2

marl

limestone


A

B

C











M Martinez et al58

















NJT5b 211 203 NA NA 207







M Martinez et al60

13

13

13

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2040

6080

wt

CaC

O3

C superbus

PLIENSBACHTOARCIAN


SigillatusSuperbus


Stage Amm

o Zon

eFor

mati

on

Calc n

anno

Zon

e

0 m51015202530354045

Leve

l (m

)

-20

2

13 C

bulk (

permil P

DB

)

-11

3

234567891011121314151617

CaC

O3

()

25

stan

d C

aCO

3

+ E

cc 4

05 k

yr

-2-1

01

2-2

-10

12

stan

d C

aCO

3

+ O

bliq

uity

100

140


C superbus1

3 C (

permil P

DB

)

-10

12

120

Ouchbis FmTagoud Fm

-20

2-2

02

Sta

nd

13C

+ O

bliq

uity

505 plusmn 44 kyr

Stage

Ammo ZoneFormation

5075

Sta

nd

13C

+ E

cc 4

05 k

yr

90130

110

105

125 95135

115

433plusmn25 kyr

Fou

m T

illic

ht (

this

stu

dy)

Pen

iche

(Lu

sita

nian

Bas

in)

123456789101112131415161718192122 2023 E1E2E3E4E5E6


405-kyr

100-kyr

obliquity

Hua

ng

et a

l (2

014)

1



tus

11

018 - 027 myr

117 plusmn 9 kyr

38 plusmn 6 kyr

Fig

9

Cor

rela

tion

of th

e as

troc

hron

olog

ical

fra

mew

orks

of

the

Foum

Till

icht

and

the

Peni

che

sect

ions

aro

und

the

Plie

nsba

chia

n-To

arci

an b

ound

ary

Pen

iche

am

mon

itezo

nes

from

Mou

terd

e (1

955)

and

cal

care

ous

nann

ofos

sil e

vent

s fr

om M

attio

li et

al

(200

4)







M Martinez et al62















M Martinez et al64


6 Conclusions




References







































M Martinez et al66























































M Martinez et al68



















M Martinez et al50

NJ5b

NJT6Carinolithus

superbus


Pleurocerasspinatum




NJT5app

NJ5b

NJT6






NJ5Tb

NJT6



Pleurocerasspinatum




NJT5app

NJ5b

NJT6pp



LatePliensbachian

pp

Early Toarcianpp

Substages

Stages



Hildaiteslevisoni





Pleurocerasspinatum




LatePliensbachian

pp

Early Toarcianpp




Pleurocerasspinatum



NJ5a

NJ5b

NJ6





Hildaiteslevisoni



Stages




NJT5a

NJ5Tb

NJT6



Tethyan (NJT)



-29 -28 -27 -26 -25 -24 -23 -22 -21-31 -30 -3 -2 -1 0 1 2 30 m

50

100

150

200

250

300

350

400

440



T-OAE

P-To event



RB

PLIE

NSB

AC

HIA

NTO

AR

CIA

N

Ouc

hbis

Fm

Ta

goud

ite F

m

Pol

ymo

Levi

soni

Em

acia

tum

Upp

erM

iddl

eU

pper

Low

er

Bifr

ons

Gra

data

Ago

udim

Fm

hiatus

Tauromeniceras sp


Lioceratoides sp

Eleganticeras sp






Alg

ov

Stu

died

inte

rval

(see

Fig

4)
















M Martinez et al52


CaC

O3

()

2030

4050

6070

stan

dard

ized

CaC

O3

+ E

cc 4

05 k

yr-2

-10

12

-2-1

01

2

stan

dard

ized

CaC

O3

+ O

bliq

uity

0 m

100

140


C superbus

13 C

(permil

PD

B)

-10

12

80120 40 2060

Ouchbis FmTagoud Fm

01

02

03

04

01

25

Fre

quen

cy(c

ycle

sm

)F

requ

ency

(cyc

les

m)

01

02

03

04

01

25

Fre

quen

cy(c

ycle

sm

)F

requ

ency

(cyc

les

m)

-20

2-2

02

Sta

ndar

dize

d 1

3 C+

Obl

iqui

ty

13241513211615

69

6345

7053

76

17

23

64



15

82

2315

41

~5392

5

16


173-kyr obliquity


obliquity


505 plusmn 44 kyr

AB

CD

EF

GH

IJ

StageAmmo Zone

Formation

L sigillatus


Sta

ndar

dize

d 1

3 C+

Ecc

405

kyr

P-To event

NJT5b NJT5aNJT6

Fig

5

Tim

e-fr

eque

ncy

spec

tral

ana

lyse

s an

d or

bita

l tun

ing

of th

e Fo

um T

illic

ht s

ectio

n A

Raw

δ13

C s

igna

l In

red

th

e lo

ng-t

erm

tren

d B

Tan

er lo

w-p

ass

filte

r of

the

405-

kyr

ecce

ntri

city

on

the

detr

ende

d δ13

C (

freq

uenc

y cu

t 1

038

10

ndash1

cycl

esm

ro

ll-of

f ra

te

1012

) C

Ta

ner

band

-pas

s fi

lter

of t

he o

bliq

uity

(lo

wer

fre

quen

cy c

ut

390

6

10ndash

1cy

cles

m u

pper

freq

uenc

y cu

t 7

935

10

ndash1

cycl

esm

rol

l-of

f rat

e 1

012)

D4

0-m

-win

dow

spe

ctro

gram

of t

he δ

13C

ser

ies

with

mai

n pe

riod

s la

belle

d in

met

ers

E1

5-m

-win

dow

spe

ctro

gram

of

the

δ13C

ser

ies

with

mai

n pe

riod

s la

belle

d in

met

ers

FR

aw C

aCO

3si

gnal

In

red

the

long

-ter

m t

rend

GT

aner

low

-pas

s fi

lter

of t

he40

5-ky

r ec

cent

rici

ty o

n th

e de

tren

ded

CaC

O3

(fre

quen

cy c

ut 7

324

10

ndash2

cycl

esm

rol

l-of

f ra

te 1

012)

HF

ilter

of

the

obliq

uity

on

the

detr

ende

d C

aCO

3(l

ower

fre

quen

cycu

t 3

297

10

ndash1

cycl

esm

upp

er fr

eque

ncy

cut

934

1

10ndash

1cy

cles

m r

oll-

off r

ate

1012

) I

40-

m-w

indo

w s

pect

rogr

am o

f the

CaC

O3

with

mai

n pe

riod

s la

belle

d in

met

ers

J15

-m-w

indo

w s

pect

rogr

am o

f th

e C

aCO

3w

ith m

ain

peri

ods

labe

lled

in m

eter

s



4 Results

41 Geochemical data







M Martinez et al54




5 Discussion









M Martinez et al56

13

13

13

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)

(

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(

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13

E161 21 16 13 10 09 08

O (17) P (09)

86deg(038 m)

-94deg(005 m)

338deg(015 m)

223deg(008 m)

286deg(008 m)

-456deg(011 m)

115deg(003 m)

CaCO3 ()

10 20 30 40 50 60 70 80

13 C

(permil

PD

B)

-2

-15

-1

-05

0

05

1

15

2

marl

limestone


A

B

C











M Martinez et al58

















NJT5b 211 203 NA NA 207







M Martinez et al60

13

13

13

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(

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13

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2040

6080

wt

CaC

O3

C superbus

PLIENSBACHTOARCIAN


SigillatusSuperbus


Stage Amm

o Zon

eFor

mati

on

Calc n

anno

Zon

e

0 m51015202530354045

Leve

l (m

)

-20

2

13 C

bulk (

permil P

DB

)

-11

3

234567891011121314151617

CaC

O3

()

25

stan

d C

aCO

3

+ E

cc 4

05 k

yr

-2-1

01

2-2

-10

12

stan

d C

aCO

3

+ O

bliq

uity

100

140


C superbus1

3 C (

permil P

DB

)

-10

12

120

Ouchbis FmTagoud Fm

-20

2-2

02

Sta

nd

13C

+ O

bliq

uity

505 plusmn 44 kyr

Stage

Ammo ZoneFormation

5075

Sta

nd

13C

+ E

cc 4

05 k

yr

90130

110

105

125 95135

115

433plusmn25 kyr

Fou

m T

illic

ht (

this

stu

dy)

Pen

iche

(Lu

sita

nian

Bas

in)

123456789101112131415161718192122 2023 E1E2E3E4E5E6


405-kyr

100-kyr

obliquity

Hua

ng

et a

l (2

014)

1



tus

11

018 - 027 myr

117 plusmn 9 kyr

38 plusmn 6 kyr

Fig

9

Cor

rela

tion

of th

e as

troc

hron

olog

ical

fra

mew

orks

of

the

Foum

Till

icht

and

the

Peni

che

sect

ions

aro

und

the

Plie

nsba

chia

n-To

arci

an b

ound

ary

Pen

iche

am

mon

itezo

nes

from

Mou

terd

e (1

955)

and

cal

care

ous

nann

ofos

sil e

vent

s fr

om M

attio

li et

al

(200

4)







M Martinez et al62















M Martinez et al64


6 Conclusions




References







































M Martinez et al66























































M Martinez et al68















LatePliensbachian

pp

Early Toarcianpp




Pleurocerasspinatum



NJ5a

NJ5b

NJ6





Hildaiteslevisoni



Stages




NJT5a

NJ5Tb

NJT6



Tethyan (NJT)



-29 -28 -27 -26 -25 -24 -23 -22 -21-31 -30 -3 -2 -1 0 1 2 30 m

50

100

150

200

250

300

350

400

440



T-OAE

P-To event



RB

PLIE

NSB

AC

HIA

NTO

AR

CIA

N

Ouc

hbis

Fm

Ta

goud

ite F

m

Pol

ymo

Levi

soni

Em

acia

tum

Upp

erM

iddl

eU

pper

Low

er

Bifr

ons

Gra

data

Ago

udim

Fm

hiatus

Tauromeniceras sp


Lioceratoides sp

Eleganticeras sp






Alg

ov

Stu

died

inte

rval

(see

Fig

4)
















M Martinez et al52


CaC

O3

()

2030

4050

6070

stan

dard

ized

CaC

O3

+ E

cc 4

05 k

yr-2

-10

12

-2-1

01

2

stan

dard

ized

CaC

O3

+ O

bliq

uity

0 m

100

140


C superbus

13 C

(permil

PD

B)

-10

12

80120 40 2060

Ouchbis FmTagoud Fm

01

02

03

04

01

25

Fre

quen

cy(c

ycle

sm

)F

requ

ency

(cyc

les

m)

01

02

03

04

01

25

Fre

quen

cy(c

ycle

sm

)F

requ

ency

(cyc

les

m)

-20

2-2

02

Sta

ndar

dize

d 1

3 C+

Obl

iqui

ty

13241513211615

69

6345

7053

76

17

23

64



15

82

2315

41

~5392

5

16


173-kyr obliquity


obliquity


505 plusmn 44 kyr

AB

CD

EF

GH

IJ

StageAmmo Zone

Formation

L sigillatus


Sta

ndar

dize

d 1

3 C+

Ecc

405

kyr

P-To event

NJT5b NJT5aNJT6

Fig

5

Tim

e-fr

eque

ncy

spec

tral

ana

lyse

s an

d or

bita

l tun

ing

of th

e Fo

um T

illic

ht s

ectio

n A

Raw

δ13

C s

igna

l In

red

th

e lo

ng-t

erm

tren

d B

Tan

er lo

w-p

ass

filte

r of

the

405-

kyr

ecce

ntri

city

on

the

detr

ende

d δ13

C (

freq

uenc

y cu

t 1

038

10

ndash1

cycl

esm

ro

ll-of

f ra

te

1012

) C

Ta

ner

band

-pas

s fi

lter

of t

he o

bliq

uity

(lo

wer

fre

quen

cy c

ut

390

6

10ndash

1cy

cles

m u

pper

freq

uenc

y cu

t 7

935

10

ndash1

cycl

esm

rol

l-of

f rat

e 1

012)

D4

0-m

-win

dow

spe

ctro

gram

of t

he δ

13C

ser

ies

with

mai

n pe

riod

s la

belle

d in

met

ers

E1

5-m

-win

dow

spe

ctro

gram

of

the

δ13C

ser

ies

with

mai

n pe

riod

s la

belle

d in

met

ers

FR

aw C

aCO

3si

gnal

In

red

the

long

-ter

m t

rend

GT

aner

low

-pas

s fi

lter

of t

he40

5-ky

r ec

cent

rici

ty o

n th

e de

tren

ded

CaC

O3

(fre

quen

cy c

ut 7

324

10

ndash2

cycl

esm

rol

l-of

f ra

te 1

012)

HF

ilter

of

the

obliq

uity

on

the

detr

ende

d C

aCO

3(l

ower

fre

quen

cycu

t 3

297

10

ndash1

cycl

esm

upp

er fr

eque

ncy

cut

934

1

10ndash

1cy

cles

m r

oll-

off r

ate

1012

) I

40-

m-w

indo

w s

pect

rogr

am o

f the

CaC

O3

with

mai

n pe

riod

s la

belle

d in

met

ers

J15

-m-w

indo

w s

pect

rogr

am o

f th

e C

aCO

3w

ith m

ain

peri

ods

labe

lled

in m

eter

s



4 Results

41 Geochemical data







M Martinez et al54




5 Discussion









M Martinez et al56

13

13

13

$amp

(

(

(

(

(

(

()

(

((

)

(

)

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(

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) ) (

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(-$

130$13

13

13

13

13

(

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$amp

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(

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3413513551356

$amp130$

137((80137

13135556

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amp134135$

13135513




13

6

)

(

613

(

(

13

E161 21 16 13 10 09 08

O (17) P (09)

86deg(038 m)

-94deg(005 m)

338deg(015 m)

223deg(008 m)

286deg(008 m)

-456deg(011 m)

115deg(003 m)

CaCO3 ()

10 20 30 40 50 60 70 80

13 C

(permil

PD

B)

-2

-15

-1

-05

0

05

1

15

2

marl

limestone


A

B

C











M Martinez et al58

















NJT5b 211 203 NA NA 207







M Martinez et al60

13

13

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2040

6080

wt

CaC

O3

C superbus

PLIENSBACHTOARCIAN


SigillatusSuperbus


Stage Amm

o Zon

eFor

mati

on

Calc n

anno

Zon

e

0 m51015202530354045

Leve

l (m

)

-20

2

13 C

bulk (

permil P

DB

)

-11

3

234567891011121314151617

CaC

O3

()

25

stan

d C

aCO

3

+ E

cc 4

05 k

yr

-2-1

01

2-2

-10

12

stan

d C

aCO

3

+ O

bliq

uity

100

140


C superbus1

3 C (

permil P

DB

)

-10

12

120

Ouchbis FmTagoud Fm

-20

2-2

02

Sta

nd

13C

+ O

bliq

uity

505 plusmn 44 kyr

Stage

Ammo ZoneFormation

5075

Sta

nd

13C

+ E

cc 4

05 k

yr

90130

110

105

125 95135

115

433plusmn25 kyr

Fou

m T

illic

ht (

this

stu

dy)

Pen

iche

(Lu

sita

nian

Bas

in)

123456789101112131415161718192122 2023 E1E2E3E4E5E6


405-kyr

100-kyr

obliquity

Hua

ng

et a

l (2

014)

1



tus

11

018 - 027 myr

117 plusmn 9 kyr

38 plusmn 6 kyr

Fig

9

Cor

rela

tion

of th

e as

troc

hron

olog

ical

fra

mew

orks

of

the

Foum

Till

icht

and

the

Peni

che

sect

ions

aro

und

the

Plie

nsba

chia

n-To

arci

an b

ound

ary

Pen

iche

am

mon

itezo

nes

from

Mou

terd

e (1

955)

and

cal

care

ous

nann

ofos

sil e

vent

s fr

om M

attio

li et

al

(200

4)







M Martinez et al62















M Martinez et al64


6 Conclusions




References







































M Martinez et al66























































M Martinez et al68




























M Martinez et al52


CaC

O3

()

2030

4050

6070

stan

dard

ized

CaC

O3

+ E

cc 4

05 k

yr-2

-10

12

-2-1

01

2

stan

dard

ized

CaC

O3

+ O

bliq

uity

0 m

100

140


C superbus

13 C

(permil

PD

B)

-10

12

80120 40 2060

Ouchbis FmTagoud Fm

01

02

03

04

01

25

Fre

quen

cy(c

ycle

sm

)F

requ

ency

(cyc

les

m)

01

02

03

04

01

25

Fre

quen

cy(c

ycle

sm

)F

requ

ency

(cyc

les

m)

-20

2-2

02

Sta

ndar

dize

d 1

3 C+

Obl

iqui

ty

13241513211615

69

6345

7053

76

17

23

64



15

82

2315

41

~5392

5

16


173-kyr obliquity


obliquity


505 plusmn 44 kyr

AB

CD

EF

GH

IJ

StageAmmo Zone

Formation

L sigillatus


Sta

ndar

dize

d 1

3 C+

Ecc

405

kyr

P-To event

NJT5b NJT5aNJT6

Fig

5

Tim

e-fr

eque

ncy

spec

tral

ana

lyse

s an

d or

bita

l tun

ing

of th

e Fo

um T

illic

ht s

ectio

n A

Raw

δ13

C s

igna

l In

red

th

e lo

ng-t

erm

tren

d B

Tan

er lo

w-p

ass

filte

r of

the

405-

kyr

ecce

ntri

city

on

the

detr

ende

d δ13

C (

freq

uenc

y cu

t 1

038

10

ndash1

cycl

esm

ro

ll-of

f ra

te

1012

) C

Ta

ner

band

-pas

s fi

lter

of t

he o

bliq

uity

(lo

wer

fre

quen

cy c

ut

390

6

10ndash

1cy

cles

m u

pper

freq

uenc

y cu

t 7

935

10

ndash1

cycl

esm

rol

l-of

f rat

e 1

012)

D4

0-m

-win

dow

spe

ctro

gram

of t

he δ

13C

ser

ies

with

mai

n pe

riod

s la

belle

d in

met

ers

E1

5-m

-win

dow

spe

ctro

gram

of

the

δ13C

ser

ies

with

mai

n pe

riod

s la

belle

d in

met

ers

FR

aw C

aCO

3si

gnal

In

red

the

long

-ter

m t

rend

GT

aner

low

-pas

s fi

lter

of t

he40

5-ky

r ec

cent

rici

ty o

n th

e de

tren

ded

CaC

O3

(fre

quen

cy c

ut 7

324

10

ndash2

cycl

esm

rol

l-of

f ra

te 1

012)

HF

ilter

of

the

obliq

uity

on

the

detr

ende

d C

aCO

3(l

ower

fre

quen

cycu

t 3

297

10

ndash1

cycl

esm

upp

er fr

eque

ncy

cut

934

1

10ndash

1cy

cles

m r

oll-

off r

ate

1012

) I

40-

m-w

indo

w s

pect

rogr

am o

f the

CaC

O3

with

mai

n pe

riod

s la

belle

d in

met

ers

J15

-m-w

indo

w s

pect

rogr

am o

f th

e C

aCO

3w

ith m

ain

peri

ods

labe

lled

in m

eter

s



4 Results

41 Geochemical data







M Martinez et al54




5 Discussion









M Martinez et al56

13

13

13

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6

)

(

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13

E161 21 16 13 10 09 08

O (17) P (09)

86deg(038 m)

-94deg(005 m)

338deg(015 m)

223deg(008 m)

286deg(008 m)

-456deg(011 m)

115deg(003 m)

CaCO3 ()

10 20 30 40 50 60 70 80

13 C

(permil

PD

B)

-2

-15

-1

-05

0

05

1

15

2

marl

limestone


A

B

C











M Martinez et al58

















NJT5b 211 203 NA NA 207







M Martinez et al60

13

13

13

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(-$

130$13

13



2040

6080

wt

CaC

O3

C superbus

PLIENSBACHTOARCIAN


SigillatusSuperbus


Stage Amm

o Zon

eFor

mati

on

Calc n

anno

Zon

e

0 m51015202530354045

Leve

l (m

)

-20

2

13 C

bulk (

permil P

DB

)

-11

3

234567891011121314151617

CaC

O3

()

25

stan

d C

aCO

3

+ E

cc 4

05 k

yr

-2-1

01

2-2

-10

12

stan

d C

aCO

3

+ O

bliq

uity

100

140


C superbus1

3 C (

permil P

DB

)

-10

12

120

Ouchbis FmTagoud Fm

-20

2-2

02

Sta

nd

13C

+ O

bliq

uity

505 plusmn 44 kyr

Stage

Ammo ZoneFormation

5075

Sta

nd

13C

+ E

cc 4

05 k

yr

90130

110

105

125 95135

115

433plusmn25 kyr

Fou

m T

illic

ht (

this

stu

dy)

Pen

iche

(Lu

sita

nian

Bas

in)

123456789101112131415161718192122 2023 E1E2E3E4E5E6


405-kyr

100-kyr

obliquity

Hua

ng

et a

l (2

014)

1



tus

11

018 - 027 myr

117 plusmn 9 kyr

38 plusmn 6 kyr

Fig

9

Cor

rela

tion

of th

e as

troc

hron

olog

ical

fra

mew

orks

of

the

Foum

Till

icht

and

the

Peni

che

sect

ions

aro

und

the

Plie

nsba

chia

n-To

arci

an b

ound

ary

Pen

iche

am

mon

itezo

nes

from

Mou

terd

e (1

955)

and

cal

care

ous

nann

ofos

sil e

vent

s fr

om M

attio

li et

al

(200

4)







M Martinez et al62















M Martinez et al64


6 Conclusions




References







































M Martinez et al66























































M Martinez et al68















CaC

O3

()

2030

4050

6070

stan

dard

ized

CaC

O3

+ E

cc 4

05 k

yr-2

-10

12

-2-1

01

2

stan

dard

ized

CaC

O3

+ O

bliq

uity

0 m

100

140


C superbus

13 C

(permil

PD

B)

-10

12

80120 40 2060

Ouchbis FmTagoud Fm

01

02

03

04

01

25

Fre

quen

cy(c

ycle

sm

)F

requ

ency

(cyc

les

m)

01

02

03

04

01

25

Fre

quen

cy(c

ycle

sm

)F

requ

ency

(cyc

les

m)

-20

2-2

02

Sta

ndar

dize

d 1

3 C+

Obl

iqui

ty

13241513211615

69

6345

7053

76

17

23

64



15

82

2315

41

~5392

5

16


173-kyr obliquity


obliquity


505 plusmn 44 kyr

AB

CD

EF

GH

IJ

StageAmmo Zone

Formation

L sigillatus


Sta

ndar

dize

d 1

3 C+

Ecc

405

kyr

P-To event

NJT5b NJT5aNJT6

Fig

5

Tim

e-fr

eque

ncy

spec

tral

ana

lyse

s an

d or

bita

l tun

ing

of th

e Fo

um T

illic

ht s

ectio

n A

Raw

δ13

C s

igna

l In

red

th

e lo

ng-t

erm

tren

d B

Tan

er lo

w-p

ass

filte

r of

the

405-

kyr

ecce

ntri

city

on

the

detr

ende

d δ13

C (

freq

uenc

y cu

t 1

038

10

ndash1

cycl

esm

ro

ll-of

f ra

te

1012

) C

Ta

ner

band

-pas

s fi

lter

of t

he o

bliq

uity

(lo

wer

fre

quen

cy c

ut

390

6

10ndash

1cy

cles

m u

pper

freq

uenc

y cu

t 7

935

10

ndash1

cycl

esm

rol

l-of

f rat

e 1

012)

D4

0-m

-win

dow

spe

ctro

gram

of t

he δ

13C

ser

ies

with

mai

n pe

riod

s la

belle

d in

met

ers

E1

5-m

-win

dow

spe

ctro

gram

of

the

δ13C

ser

ies

with

mai

n pe

riod

s la

belle

d in

met

ers

FR

aw C

aCO

3si

gnal

In

red

the

long

-ter

m t

rend

GT

aner

low

-pas

s fi

lter

of t

he40

5-ky

r ec

cent

rici

ty o

n th

e de

tren

ded

CaC

O3

(fre

quen

cy c

ut 7

324

10

ndash2

cycl

esm

rol

l-of

f ra

te 1

012)

HF

ilter

of

the

obliq

uity

on

the

detr

ende

d C

aCO

3(l

ower

fre

quen

cycu

t 3

297

10

ndash1

cycl

esm

upp

er fr

eque

ncy

cut

934

1

10ndash

1cy

cles

m r

oll-

off r

ate

1012

) I

40-

m-w

indo

w s

pect

rogr

am o

f the

CaC

O3

with

mai

n pe

riod

s la

belle

d in

met

ers

J15

-m-w

indo

w s

pect

rogr

am o

f th

e C

aCO

3w

ith m

ain

peri

ods

labe

lled

in m

eter

s



4 Results

41 Geochemical data







M Martinez et al54




5 Discussion









M Martinez et al56

13

13

13

$amp

(

(

(

(

(

(

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(

((

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130$13

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13

6

)

(

613

(

(

13

E161 21 16 13 10 09 08

O (17) P (09)

86deg(038 m)

-94deg(005 m)

338deg(015 m)

223deg(008 m)

286deg(008 m)

-456deg(011 m)

115deg(003 m)

CaCO3 ()

10 20 30 40 50 60 70 80

13 C

(permil

PD

B)

-2

-15

-1

-05

0

05

1

15

2

marl

limestone


A

B

C











M Martinez et al58

















NJT5b 211 203 NA NA 207







M Martinez et al60

13

13

13

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(

(

(

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13

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(-$

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13



2040

6080

wt

CaC

O3

C superbus

PLIENSBACHTOARCIAN


SigillatusSuperbus


Stage Amm

o Zon

eFor

mati

on

Calc n

anno

Zon

e

0 m51015202530354045

Leve

l (m

)

-20

2

13 C

bulk (

permil P

DB

)

-11

3

234567891011121314151617

CaC

O3

()

25

stan

d C

aCO

3

+ E

cc 4

05 k

yr

-2-1

01

2-2

-10

12

stan

d C

aCO

3

+ O

bliq

uity

100

140


C superbus1

3 C (

permil P

DB

)

-10

12

120

Ouchbis FmTagoud Fm

-20

2-2

02

Sta

nd

13C

+ O

bliq

uity

505 plusmn 44 kyr

Stage

Ammo ZoneFormation

5075

Sta

nd

13C

+ E

cc 4

05 k

yr

90130

110

105

125 95135

115

433plusmn25 kyr

Fou

m T

illic

ht (

this

stu

dy)

Pen

iche

(Lu

sita

nian

Bas

in)

123456789101112131415161718192122 2023 E1E2E3E4E5E6


405-kyr

100-kyr

obliquity

Hua

ng

et a

l (2

014)

1



tus

11

018 - 027 myr

117 plusmn 9 kyr

38 plusmn 6 kyr

Fig

9

Cor

rela

tion

of th

e as

troc

hron

olog

ical

fra

mew

orks

of

the

Foum

Till

icht

and

the

Peni

che

sect

ions

aro

und

the

Plie

nsba

chia

n-To

arci

an b

ound

ary

Pen

iche

am

mon

itezo

nes

from

Mou

terd

e (1

955)

and

cal

care

ous

nann

ofos

sil e

vent

s fr

om M

attio

li et

al

(200

4)







M Martinez et al62















M Martinez et al64


6 Conclusions




References







































M Martinez et al66























































M Martinez et al68
















4 Results

41 Geochemical data







M Martinez et al54




5 Discussion









M Martinez et al56

13

13

13

$amp

(

(

(

(

(

(

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(

((

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amp134135$

13135513




13

6

)

(

613

(

(

13

E161 21 16 13 10 09 08

O (17) P (09)

86deg(038 m)

-94deg(005 m)

338deg(015 m)

223deg(008 m)

286deg(008 m)

-456deg(011 m)

115deg(003 m)

CaCO3 ()

10 20 30 40 50 60 70 80

13 C

(permil

PD

B)

-2

-15

-1

-05

0

05

1

15

2

marl

limestone


A

B

C











M Martinez et al58

















NJT5b 211 203 NA NA 207







M Martinez et al60

13

13

13

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(

(

(

(

13

13

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13

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45$-$45

245$-

245$-$45

3413513551356

$amp130$

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13135556

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0137

956131356$

amp134135$

13135513

13(((

(-$

130$13

13



2040

6080

wt

CaC

O3

C superbus

PLIENSBACHTOARCIAN


SigillatusSuperbus


Stage Amm

o Zon

eFor

mati

on

Calc n

anno

Zon

e

0 m51015202530354045

Leve

l (m

)

-20

2

13 C

bulk (

permil P

DB

)

-11

3

234567891011121314151617

CaC

O3

()

25

stan

d C

aCO

3

+ E

cc 4

05 k

yr

-2-1

01

2-2

-10

12

stan

d C

aCO

3

+ O

bliq

uity

100

140


C superbus1

3 C (

permil P

DB

)

-10

12

120

Ouchbis FmTagoud Fm

-20

2-2

02

Sta

nd

13C

+ O

bliq

uity

505 plusmn 44 kyr

Stage

Ammo ZoneFormation

5075

Sta

nd

13C

+ E

cc 4

05 k

yr

90130

110

105

125 95135

115

433plusmn25 kyr

Fou

m T

illic

ht (

this

stu

dy)

Pen

iche

(Lu

sita

nian

Bas

in)

123456789101112131415161718192122 2023 E1E2E3E4E5E6


405-kyr

100-kyr

obliquity

Hua

ng

et a

l (2

014)

1



tus

11

018 - 027 myr

117 plusmn 9 kyr

38 plusmn 6 kyr

Fig

9

Cor

rela

tion

of th

e as

troc

hron

olog

ical

fra

mew

orks

of

the

Foum

Till

icht

and

the

Peni

che

sect

ions

aro

und

the

Plie

nsba

chia

n-To

arci

an b

ound

ary

Pen

iche

am

mon

itezo

nes

from

Mou

terd

e (1

955)

and

cal

care

ous

nann

ofos

sil e

vent

s fr

om M

attio

li et

al

(200

4)







M Martinez et al62















M Martinez et al64


6 Conclusions




References







































M Martinez et al66























































M Martinez et al68

















5 Discussion









M Martinez et al56

13

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13

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O (17) P (09)

86deg(038 m)

-94deg(005 m)

338deg(015 m)

223deg(008 m)

286deg(008 m)

-456deg(011 m)

115deg(003 m)

CaCO3 ()

10 20 30 40 50 60 70 80

13 C

(permil

PD

B)

-2

-15

-1

-05

0

05

1

15

2

marl

limestone


A

B

C











M Martinez et al58

















NJT5b 211 203 NA NA 207







M Martinez et al60

13

13

13

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2040

6080

wt

CaC

O3

C superbus

PLIENSBACHTOARCIAN


SigillatusSuperbus


Stage Amm

o Zon

eFor

mati

on

Calc n

anno

Zon

e

0 m51015202530354045

Leve

l (m

)

-20

2

13 C

bulk (

permil P

DB

)

-11

3

234567891011121314151617

CaC

O3

()

25

stan

d C

aCO

3

+ E

cc 4

05 k

yr

-2-1

01

2-2

-10

12

stan

d C

aCO

3

+ O

bliq

uity

100

140


C superbus1

3 C (

permil P

DB

)

-10

12

120

Ouchbis FmTagoud Fm

-20

2-2

02

Sta

nd

13C

+ O

bliq

uity

505 plusmn 44 kyr

Stage

Ammo ZoneFormation

5075

Sta

nd

13C

+ E

cc 4

05 k

yr

90130

110

105

125 95135

115

433plusmn25 kyr

Fou

m T

illic

ht (

this

stu

dy)

Pen

iche

(Lu

sita

nian

Bas

in)

123456789101112131415161718192122 2023 E1E2E3E4E5E6


405-kyr

100-kyr

obliquity

Hua

ng

et a

l (2

014)

1



tus

11

018 - 027 myr

117 plusmn 9 kyr

38 plusmn 6 kyr

Fig

9

Cor

rela

tion

of th

e as

troc

hron

olog

ical

fra

mew

orks

of

the

Foum

Till

icht

and

the

Peni

che

sect

ions

aro

und

the

Plie

nsba

chia

n-To

arci

an b

ound

ary

Pen

iche

am

mon

itezo

nes

from

Mou

terd

e (1

955)

and

cal

care

ous

nann

ofos

sil e

vent

s fr

om M

attio

li et

al

(200

4)







M Martinez et al62















M Martinez et al64


6 Conclusions




References







































M Martinez et al66























































M Martinez et al68














M Martinez et al56

13

13

13

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(

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13

E161 21 16 13 10 09 08

O (17) P (09)

86deg(038 m)

-94deg(005 m)

338deg(015 m)

223deg(008 m)

286deg(008 m)

-456deg(011 m)

115deg(003 m)

CaCO3 ()

10 20 30 40 50 60 70 80

13 C

(permil

PD

B)

-2

-15

-1

-05

0

05

1

15

2

marl

limestone


A

B

C











M Martinez et al58

















NJT5b 211 203 NA NA 207







M Martinez et al60

13

13

13

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2040

6080

wt

CaC

O3

C superbus

PLIENSBACHTOARCIAN


SigillatusSuperbus


Stage Amm

o Zon

eFor

mati

on

Calc n

anno

Zon

e

0 m51015202530354045

Leve

l (m

)

-20

2

13 C

bulk (

permil P

DB

)

-11

3

234567891011121314151617

CaC

O3

()

25

stan

d C

aCO

3

+ E

cc 4

05 k

yr

-2-1

01

2-2

-10

12

stan

d C

aCO

3

+ O

bliq

uity

100

140


C superbus1

3 C (

permil P

DB

)

-10

12

120

Ouchbis FmTagoud Fm

-20

2-2

02

Sta

nd

13C

+ O

bliq

uity

505 plusmn 44 kyr

Stage

Ammo ZoneFormation

5075

Sta

nd

13C

+ E

cc 4

05 k

yr

90130

110

105

125 95135

115

433plusmn25 kyr

Fou

m T

illic

ht (

this

stu

dy)

Pen

iche

(Lu

sita

nian

Bas

in)

123456789101112131415161718192122 2023 E1E2E3E4E5E6


405-kyr

100-kyr

obliquity

Hua

ng

et a

l (2

014)

1



tus

11

018 - 027 myr

117 plusmn 9 kyr

38 plusmn 6 kyr

Fig

9

Cor

rela

tion

of th

e as

troc

hron

olog

ical

fra

mew

orks

of

the

Foum

Till

icht

and

the

Peni

che

sect

ions

aro

und

the

Plie

nsba

chia

n-To

arci

an b

ound

ary

Pen

iche

am

mon

itezo

nes

from

Mou

terd

e (1

955)

and

cal

care

ous

nann

ofos

sil e

vent

s fr

om M

attio

li et

al

(200

4)







M Martinez et al62















M Martinez et al64


6 Conclusions




References







































M Martinez et al66























































M Martinez et al68

















13

6

)

(

613

(

(

13

E161 21 16 13 10 09 08

O (17) P (09)

86deg(038 m)

-94deg(005 m)

338deg(015 m)

223deg(008 m)

286deg(008 m)

-456deg(011 m)

115deg(003 m)

CaCO3 ()

10 20 30 40 50 60 70 80

13 C

(permil

PD

B)

-2

-15

-1

-05

0

05

1

15

2

marl

limestone


A

B

C











M Martinez et al58

















NJT5b 211 203 NA NA 207







M Martinez et al60

13

13

13

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13



2040

6080

wt

CaC

O3

C superbus

PLIENSBACHTOARCIAN


SigillatusSuperbus


Stage Amm

o Zon

eFor

mati

on

Calc n

anno

Zon

e

0 m51015202530354045

Leve

l (m

)

-20

2

13 C

bulk (

permil P

DB

)

-11

3

234567891011121314151617

CaC

O3

()

25

stan

d C

aCO

3

+ E

cc 4

05 k

yr

-2-1

01

2-2

-10

12

stan

d C

aCO

3

+ O

bliq

uity

100

140


C superbus1

3 C (

permil P

DB

)

-10

12

120

Ouchbis FmTagoud Fm

-20

2-2

02

Sta

nd

13C

+ O

bliq

uity

505 plusmn 44 kyr

Stage

Ammo ZoneFormation

5075

Sta

nd

13C

+ E

cc 4

05 k

yr

90130

110

105

125 95135

115

433plusmn25 kyr

Fou

m T

illic

ht (

this

stu

dy)

Pen

iche

(Lu

sita

nian

Bas

in)

123456789101112131415161718192122 2023 E1E2E3E4E5E6


405-kyr

100-kyr

obliquity

Hua

ng

et a

l (2

014)

1



tus

11

018 - 027 myr

117 plusmn 9 kyr

38 plusmn 6 kyr

Fig

9

Cor

rela

tion

of th

e as

troc

hron

olog

ical

fra

mew

orks

of

the

Foum

Till

icht

and

the

Peni

che

sect

ions

aro

und

the

Plie

nsba

chia

n-To

arci

an b

ound

ary

Pen

iche

am

mon

itezo

nes

from

Mou

terd

e (1

955)

and

cal

care

ous

nann

ofos

sil e

vent

s fr

om M

attio

li et

al

(200

4)







M Martinez et al62















M Martinez et al64


6 Conclusions




References







































M Martinez et al66























































M Martinez et al68






















M Martinez et al58

















NJT5b 211 203 NA NA 207







M Martinez et al60

13

13

13

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13



2040

6080

wt

CaC

O3

C superbus

PLIENSBACHTOARCIAN


SigillatusSuperbus


Stage Amm

o Zon

eFor

mati

on

Calc n

anno

Zon

e

0 m51015202530354045

Leve

l (m

)

-20

2

13 C

bulk (

permil P

DB

)

-11

3

234567891011121314151617

CaC

O3

()

25

stan

d C

aCO

3

+ E

cc 4

05 k

yr

-2-1

01

2-2

-10

12

stan

d C

aCO

3

+ O

bliq

uity

100

140


C superbus1

3 C (

permil P

DB

)

-10

12

120

Ouchbis FmTagoud Fm

-20

2-2

02

Sta

nd

13C

+ O

bliq

uity

505 plusmn 44 kyr

Stage

Ammo ZoneFormation

5075

Sta

nd

13C

+ E

cc 4

05 k

yr

90130

110

105

125 95135

115

433plusmn25 kyr

Fou

m T

illic

ht (

this

stu

dy)

Pen

iche

(Lu

sita

nian

Bas

in)

123456789101112131415161718192122 2023 E1E2E3E4E5E6


405-kyr

100-kyr

obliquity

Hua

ng

et a

l (2

014)

1



tus

11

018 - 027 myr

117 plusmn 9 kyr

38 plusmn 6 kyr

Fig

9

Cor

rela

tion

of th

e as

troc

hron

olog

ical

fra

mew

orks

of

the

Foum

Till

icht

and

the

Peni

che

sect

ions

aro

und

the

Plie

nsba

chia

n-To

arci

an b

ound

ary

Pen

iche

am

mon

itezo

nes

from

Mou

terd

e (1

955)

and

cal

care

ous

nann

ofos

sil e

vent

s fr

om M

attio

li et

al

(200

4)







M Martinez et al62















M Martinez et al64


6 Conclusions




References







































M Martinez et al66























































M Martinez et al68






























NJT5b 211 203 NA NA 207







M Martinez et al60

13

13

13

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(

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(

13

13

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(

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13

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(-$

130$13

13



2040

6080

wt

CaC

O3

C superbus

PLIENSBACHTOARCIAN


SigillatusSuperbus


Stage Amm

o Zon

eFor

mati

on

Calc n

anno

Zon

e

0 m51015202530354045

Leve

l (m

)

-20

2

13 C

bulk (

permil P

DB

)

-11

3

234567891011121314151617

CaC

O3

()

25

stan

d C

aCO

3

+ E

cc 4

05 k

yr

-2-1

01

2-2

-10

12

stan

d C

aCO

3

+ O

bliq

uity

100

140


C superbus1

3 C (

permil P

DB

)

-10

12

120

Ouchbis FmTagoud Fm

-20

2-2

02

Sta

nd

13C

+ O

bliq

uity

505 plusmn 44 kyr

Stage

Ammo ZoneFormation

5075

Sta

nd

13C

+ E

cc 4

05 k

yr

90130

110

105

125 95135

115

433plusmn25 kyr

Fou

m T

illic

ht (

this

stu

dy)

Pen

iche

(Lu

sita

nian

Bas

in)

123456789101112131415161718192122 2023 E1E2E3E4E5E6


405-kyr

100-kyr

obliquity

Hua

ng

et a

l (2

014)

1



tus

11

018 - 027 myr

117 plusmn 9 kyr

38 plusmn 6 kyr

Fig

9

Cor

rela

tion

of th

e as

troc

hron

olog

ical

fra

mew

orks

of

the

Foum

Till

icht

and

the

Peni

che

sect

ions

aro

und

the

Plie

nsba

chia

n-To

arci

an b

ound

ary

Pen

iche

am

mon

itezo

nes

from

Mou

terd

e (1

955)

and

cal

care

ous

nann

ofos

sil e

vent

s fr

om M

attio

li et

al

(200

4)







M Martinez et al62















M Martinez et al64


6 Conclusions




References







































M Martinez et al66























































M Martinez et al68




















M Martinez et al60

13

13

13

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(

(

(

(

13

13

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(

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13

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45$-$45

245$-

245$-$45

3413513551356

$amp130$

137((80137

13135556

$amp13

0137

956131356$

amp134135$

13135513

13(((

(-$

130$13

13



2040

6080

wt

CaC

O3

C superbus

PLIENSBACHTOARCIAN


SigillatusSuperbus


Stage Amm

o Zon

eFor

mati

on

Calc n

anno

Zon

e

0 m51015202530354045

Leve

l (m

)

-20

2

13 C

bulk (

permil P

DB

)

-11

3

234567891011121314151617

CaC

O3

()

25

stan

d C

aCO

3

+ E

cc 4

05 k

yr

-2-1

01

2-2

-10

12

stan

d C

aCO

3

+ O

bliq

uity

100

140


C superbus1

3 C (

permil P

DB

)

-10

12

120

Ouchbis FmTagoud Fm

-20

2-2

02

Sta

nd

13C

+ O

bliq

uity

505 plusmn 44 kyr

Stage

Ammo ZoneFormation

5075

Sta

nd

13C

+ E

cc 4

05 k

yr

90130

110

105

125 95135

115

433plusmn25 kyr

Fou

m T

illic

ht (

this

stu

dy)

Pen

iche

(Lu

sita

nian

Bas

in)

123456789101112131415161718192122 2023 E1E2E3E4E5E6


405-kyr

100-kyr

obliquity

Hua

ng

et a

l (2

014)

1



tus

11

018 - 027 myr

117 plusmn 9 kyr

38 plusmn 6 kyr

Fig

9

Cor

rela

tion

of th

e as

troc

hron

olog

ical

fra

mew

orks

of

the

Foum

Till

icht

and

the

Peni

che

sect

ions

aro

und

the

Plie

nsba

chia

n-To

arci

an b

ound

ary

Pen

iche

am

mon

itezo

nes

from

Mou

terd

e (1

955)

and

cal

care

ous

nann

ofos

sil e

vent

s fr

om M

attio

li et

al

(200

4)







M Martinez et al62















M Martinez et al64


6 Conclusions




References







































M Martinez et al66























































M Martinez et al68















2040

6080

wt

CaC

O3

C superbus

PLIENSBACHTOARCIAN


SigillatusSuperbus


Stage Amm

o Zon

eFor

mati

on

Calc n

anno

Zon

e

0 m51015202530354045

Leve

l (m

)

-20

2

13 C

bulk (

permil P

DB

)

-11

3

234567891011121314151617

CaC

O3

()

25

stan

d C

aCO

3

+ E

cc 4

05 k

yr

-2-1

01

2-2

-10

12

stan

d C

aCO

3

+ O

bliq

uity

100

140


C superbus1

3 C (

permil P

DB

)

-10

12

120

Ouchbis FmTagoud Fm

-20

2-2

02

Sta

nd

13C

+ O

bliq

uity

505 plusmn 44 kyr

Stage

Ammo ZoneFormation

5075

Sta

nd

13C

+ E

cc 4

05 k

yr

90130

110

105

125 95135

115

433plusmn25 kyr

Fou

m T

illic

ht (

this

stu

dy)

Pen

iche

(Lu

sita

nian

Bas

in)

123456789101112131415161718192122 2023 E1E2E3E4E5E6


405-kyr

100-kyr

obliquity

Hua

ng

et a

l (2

014)

1



tus

11

018 - 027 myr

117 plusmn 9 kyr

38 plusmn 6 kyr

Fig

9

Cor

rela

tion

of th

e as

troc

hron

olog

ical

fra

mew

orks

of

the

Foum

Till

icht

and

the

Peni

che

sect

ions

aro

und

the

Plie

nsba

chia

n-To

arci

an b

ound

ary

Pen

iche

am

mon

itezo

nes

from

Mou

terd

e (1

955)

and

cal

care

ous

nann

ofos

sil e

vent

s fr

om M

attio

li et

al

(200

4)







M Martinez et al62















M Martinez et al64


6 Conclusions




References







































M Martinez et al66























































M Martinez et al68




















M Martinez et al62















M Martinez et al64


6 Conclusions




References







































M Martinez et al66























































M Martinez et al68




























M Martinez et al64


6 Conclusions




References







































M Martinez et al66























































M Martinez et al68




















M Martinez et al64


6 Conclusions




References







































M Martinez et al66























































M Martinez et al68















6 Conclusions




References







































M Martinez et al66























































M Martinez et al68







































M Martinez et al66























































M Martinez et al68




































































M Martinez et al68







































M Martinez et al68



























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Orbital chronology of the Pliensbachian Â Toarcian ...pure.au.dk/portal/files/110283456/s3.pdf · Middle Atlas Oran Meseta Central High Atlas Anti Atlas Sahara Atlas Emerged lands