Proposal DAAD - Juan Pablo Navarro

8/10/2019 Proposal DAAD - Juan Pablo Navarro

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First time proposal (DAAD)

I.1. Applicants

Main applicant:Bch. Ing. J.P. Navarro.GeologistBorn 12.03.1985, PeruvianGeological Survey of Peru (INGEMMET)Geological Regional DepartmentE-mail: [email protected]

Main coordinator:

Dr. S. BodinWissenschaftlicher Mitarbeiter (employed until 14.02.2016)Born 19.05.1977, FrenchRuhr-Universitt BochumInstitut fr Geologie, Mineralogie und GeophysikUniversittsstrasse 150, D-44801 BochumPhone: +49 (0234)-32-22307, fax: +49 (0234)-32-14571E-mail: [email protected]: Krnerstrasse 13, D-58452 Witten

Co-coordinators:

Jun.-Prof. Dr. U. HeimhoferJunior-Professor (employed until 31.07.2013)Born 19.10.1971, GermanRuhr-Universitt BochumInstitut fr Geologie, Mineralogie und Geophysik

Universittsstrasse 150, D-44801 BochumPhone: +49 (0234)-32-23252, fax: +49 (0234)-32-14571E-mail: [email protected]: Plutostrasse 16, D-44651 Herne

Prof. Dr. A. ImmenhauserProfessor for Sediment and Isotope GeologyBorn 16.10.1965, SwissRuhr-Universitt BochumInstitut fr Geologie, Mineralogie und GeophysikUniversittsstrasse 150, D-44801 BochumPhone: +49 (0234)-32-28250, fax: +49 (0234)-32-14571E-mail: [email protected]

Home: Fischenbergstrasse 15, D-58455 Witten

I.2. Topic


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Impact of Middle Cretaceous climatic change on sub-equatorialPacific settings (Northern and Central Andes, Peru): A

comparison with the Tethyan realm

1. Summary

The Middle Cretaceous was a time of greenhouse climates, featuring reducedtemperature gradients from the equator to the poles, general absence of polar ice caps,and oceans at least 13C warmer than today (Larzon et al., 1993). The MiddleCretaceous represents thus a natural laboratory to study climatic extremes. However, avast majority of the studies have focussed on European and North American outcrops,strongly biasing our understanding of this time interval. This forms a strong motivationfor the project proposed here, aiming to assess the impact of Middle Cretaceousclimatic change on sub-equatorial Pacific settings (Northern and Central Andes, Peru).Indeed, the sequences in the Northern and Central Andes of Peru were depositedwithin the sub-equatorial belt of the Southern hemisphere and close to the Pacificmargin. Its faunas, surprisingly Tethyan in character, closely resembling those of NorthAfrica (Larzon et al., 1993), provide good tools for correlation with the Tethyan realm,and therefore assessing similarities and differences between these two palaeoclimaticbelts. The Northern and Central Andes of Peru offers exceptional outcrops, where itexposes evidence of shallow- to deep-water trends from east to west, which will thusallow reconstructing regional, dip-orientated transects. In order to better constrainpaleoclimatic change, a high-resolution, multi-proxy approach (C, O and Sr isotopes) isproposed. Geochemical analyses will be coupled with a detailed sedimentological andpaleo-ecological assessment of carbonate platform successions. This will lead to abetter understanding of both neritic and deep-water settings in the sub-equatorialPacific realm, which will then be compared to the Tethyan realm in order to understandthe causal linkages among these geological processes during the Middle Cretaceous.

2. Introduction and state of the art

2.1. The Middle Cretaceous Greenhouse

The long-term oceanographic record of the Middle Cretaceous (Fig. 1) has beendiscussed by Norris et al. (2001). Reconstructions suggest that the Cretaceousgreenhouse climate culminated during the Late Albian - Turonian interval. The eustaticsea-level was at its Phanerozoic maximum, and the worlds oceans were moresusceptible to development of oxygen deficits, leading to the development of severalOceanic Anoxic Events (OAE, Schlanger and Jenkyns, 1976; Jenkyns, 1980; Larson etal., 1993). These latter are characterized in deep-water settings by the deposition ofblack shales, coeval to global isotope anomalies (Jenkyns, 2010, see below). TheCretaceous involved the major OAE intervals (Wagreich et al., 2011), these were the

Weissert OAE in the Late Valanginian, the Early Aptian Selli (OAE 1a), Cenomanian-Turonian (OAE2), and Coniacian-Santonian (OAE3) (Erba, 2004; Leckie et al., 2002).The Early Aptian Oceanic Anoxic Event (OAE 1a) was characterized by intensifiedgreenhouse climate conditions, widespread accumulation of organic deposits in open-marine settings, and severe perturbation of the shallow marine realm as illustrated bycarbonate platform drowning or micro-encruster blooms (Immenhauser et al., 2005;Fllmi et al., 2006; Huck et al., 2010, 2011; Najarro et al., 2011). Records of theTethyan and Atlantic sequences on the Middle Cretaceous evidenced oxicenvironments during the AptianAlbian age (Wang et al., 2004; Hu et al., 2005, 2006;Hu et al., 2009; Xiang Li et al., 2011; Melinte-Dobrinescu and Roban, 2011). Episodes


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of Cretaceous Oceanic Red Bed (CORB) deposition have been recorded after the mid-Cretaceous OAEs in the Tethyan Realm (e.g., Hu et al., 2006), these depositcorrespond to oxic deep sea (super-oxic event) deposits such as red marls and redshales were deposited during mid- and Late Cretaceous. The latter deposits areassociated with very low content of organic carbon and oxic depositional environmentswhich dominated western Tethys in the Cretaceous (Wang et al., 2011; Neuhuber andWagreich, 2011; Li et al., 2011). The middle Cretaceous is thus characterized byseveral climatic transitions, as recorded by the alternation of anoxic and super-oxicphases (Wagreich et al., 2011; Melinte-Dobrinescu and Roban, 2011).The Cretaceous climate has been better known from stable isotopes, particularly thoseof oxygen and carbon. Oxygen isotopes of marine fossils record the paleotemperaturehistory of the ocean, indicating a cool early Cretaceous (Frakes, 1999; Zakharov et al.,2011), a hot mid-Cretaceous, and a warm late Cretaceous (Huber et al., 2002). Carbonisotopes primarily reflect the relative burial rates of organic and inorganic carbonacross the globe: a ratio controlled by terrestrial and oceanic productivity, erosion andsedimentation rates, sea level change, tectonic activity, and climate (Wagreich et al.,2011). New isotopic palaeotemperatures, estimated from 18O values in theCretaceous ammonoid shells of Southern in the Bering area evidenced penetration ofcooler waters, and the existence of warm climatic conditions in the Late Albian, latestCenomanian, Coniacian, Santonian to Early Campanian, latest Campanian, and alsolate Early Maastrichtian (Zakharov et al., 2011). Rapid transition to greenhouseconditions occurred during the Cretaceous (Jenkyns, 2003), some of them were forcedby magmatism and tectonic activity (Jahren, 2002).As noted here, a vast majority of the studies of Cretaceous climate have been focussedon the Tethyan and Atlantic outcrops strongly biasing our understanding of this timeinterval, but very little information are available from the rest of the world. As such, littleis known about climate changes studies on Middle Cretaceous in South America,especially in the Northern and Central of Peru. Previous works were focused on theCenomanian-Turonian transition (Jaillard and Vanneau, 1993) and others inbiostratigraphical studies (Benavides, 1956; Hillebrandt, 1970; Janjou, 1981; Romani,1982; Jaillard, 1986; Mourier et al., 1986; Mourier et al., 1988; Jaillard, 1990).

2.2. Oceanic anoxic eventsThe Middle Cretaceous has experienced the repetition of several Oceanic AnoxicEvents (OAEs) that can be traced by worldwide correlatable black shales horizons andisotopic anomalies (Larzon et al., 1993; Herrle et al., 2003; Jenkyns, 2010). OAEs arecommonly interpreted as being linked to periods of high carbon burial, relative oxygendepletion of oceanic bottom water and subsequent drawdown of atmospheric CO 2 (Jenkyns, 1980, 1988; Arthur et al., 1988; Weissert et al., 1998; Erbacher et al., 2001;Heimhofer et al., 2004). Widespread black shale deposition was perhaps caused byincreased preservation of organic matter due to sluggish ocean circulation (e.g.,Schlanger & Jenkyns, 1976; Erbacher et al., 2001) and/or by enhanced productivityand deposition rates of organic matter (e.g., Pedersen & Calvert, 1990; Hochuli et al.,1999; Premoli Silva et al., 1999; Erbacher et al., 2001; Mort et al., 2007).

The Upper Aptian to Early Cenomanian time include the OAE 1b ( H.planisferaPlanktonic Foraminifera zone, Aptian/Albian boundary), the OAE 1c ( R. subticinensisPlanktonic Foraminifera zone; Middle Albian), and the OAE 1d ( R. appenninicaPlanktonic Foraminifera zone; Albian/Cenomanian boundary). It is likely, however, thatdifferent OAEs have different driving mechanisms as reflected in different types oforganic matter found in specific black shale intervals (Erbacher et al., 1996; Kuypers etal. 2001). The focus of the proposed research project is on the Middle CretaceousOAEs (OAE 1b, OAE 1c, OAE 1d), which are documented in the Tethyan and Atlanticrealm (Trabucho Alexandre et al., 2010). Their Pacific counterpart is however poorlyunderstood (Fig. 1).


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2.3. Cretaceous of Peru

The sequences in the Northern and Central Andes were deposited well within the sub-equatorial belt of the Southern hemisphere and close to the Pacific margin (Fig. 2). Thesedimentological records in the Peruvian Andes show shallow- to deep-water trendsfrom east to west during the Middle Cretaceous.In the Andean fold-and-thrust belt (Central Andes), the Aptian is characterized by shelfareas made of continental/deltaic siliciclastic deposits whereas deeper areas arecharacterized by volcanic and turbiditic deposits. The Middle Albian is represented byblack, laminated limestone of the Pariatambo Formation. This unit is overlying thin-bedded, light-gray limestone with minor beds of sandy shale from the Inca-ChulecFormations (Upper Aptian-Middle Albian age; Benavides, 1956). Nodular, graylimestones are characteristic for the Yamagual -Jumasha Formations of Late Albian toEarly Cenomanian age. These units are well exposed in Cajamarca in northern Peruand in La Oroya in central Peru.In the North Andes, at the border between Peru and Ecuador, is located theCretaceous Lancones basin (Kennerley, 1973; Mourier, 1988; Bengtson and Jaillard,1997; Jaillard et al., 1999). It is located between the Paleozoic Amotape-Tahuin Massifto the west and northwest, and the continental volcanic arc to the east and southeast.Middle Albian deposits are characterized by black, laminated limestone and marls,presenting abundant planktonic foraminifera as well as some ammonites of the MuertoFormation. This unit rests conformably on laminated limestone and marls of thePananga Formation (Lower Albian; Jaillard et al., 1999). The Muerto Formation isoverlaid by turbiditic sequences of the Copa Sombrero Group (Upper Albian-Turonian

age).Little is known about the Middle Cretaceous OAEs recorded in the Peruvian Andes;nevertheless, Jaillard and Arnaud-Vanneau (1993) defined the Cenomanian-Turoniantransition that coincides with the well-known OAE2; however anoxia seems to havebeen less important than elsewhere, probably because of better oceanic circulation(Jaillard and Arnaud-Vanneau, 1993). The majority of studies in the Cretaceous werefocused in the Geodynamic evolution of the Andes of Peru, using the Tethyan model(Jaillard et al., 1990).

Figure 1 Paleographic Global map of the Middle Cretaceous reconstruction(Blakey, 2011).


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2.4. Remaining questions

Documenting the response of every physiographic setting (e.g. sub-equatorial Pacificsettings, Tethyan realms, neritic-epeiric seas, basinal settings) is of primary importancefor our understanding of the causes and consequences of Middle Cretaceous OAEs.However, a majority of the studies were focused in research related to hemi-pelagic,pelagic sections and studies from intrashelf basinal settings (e.g. Weissert et al., 1985;Arthur et al., 1990; Jenkyns et al., 1994; Erbacher et al., 1996; Weissert et al., 1998;Menegatti et al., 1998; Hesselbo et al., 2000; Heimhofer et al. 2006, McArthur et al.,2008). These were also established in sequences which belong for their vast majorityto the Tethyan realms, thus strongly biasing our understanding toward an Europeanrealm point of view. In order to get a more widespread understanding of these OAEsduring the Middle Cretaceous, modern studies are highly needed from other part of theglobe, and especially the Pacific realm. This forms a strong motivation for the presentresearch project that is guided by four crucial questions:

1. What is the impact of the Upper Aptian Early Cenomanian palaeo-environmental perturbation on the deep-to-shallow water carbonate platforms inthe equatorial Pacific setting and its relationship with the Tethyan realm?

2. What are the causal linkages of both Equatorial Pacific setting and Tethyanrealm, and if they correspond to the same Oceanic Anoxic Global Events on theMiddle Cretaceous time?

Figure 1 Map of South America showing the Andes Mountains,where the transition between the Northern and Central Andes of Peruis located near to the border of Peru and Ecuador.


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3. Did these global perturbations have a profound impact on the equatorial Pacificsettings, and if yes, what are their interactions with the epeiric-neritic realm?

4. Why are the equatorial Pacific faunas surprisingly Tethyan in character?

In order to shed light on these poorly understood issues, firstly, it is here proposed toinvestigate deep-water sections which outcrop in western side of the Northern andCentral Andes of Peru. These latter can then be correlated with punctual sections ofshallow water sections that outcrop in eastern side of the Andean mountain(Amazonian jungle).

3. Objectives, methodology and work schedule

3.1. Scientific goals

Having assessed the good quality of the Upper Aptian Early Cenomaniansedimentary sequences recorded in the Northern and Central Andes of Peru, we arenow in the position to approach the middle Cretaceous events with an equatorialPacific point of view. To understand how this poorly studied setting has reacted to, andplayed a role in profound global palaeoenvironmental changes, we intend to study twokey areas in the Andean Mountains of Peru: (1) Oroya-Cerro de Pasco regions, (2)Cajamarca-Amazonas-Lancones regions (Fig. 3). These localities have been visitedduring preliminary field-work and selected based on their excellent exposure andaccessibility. The sequences mentioned above present multi-event history of black-carbonate deep-water, and mixed siliciclastic-carbonate shallow-water depositions,respectively.

In essence, the research is driven by the following working hypotheses and the projectproposed will be instrumental to validate or reject and reformulate these concepts:

1. The middle Cretaceous OAEs (OAE 1b, OAE 1c, OAE 1d) recorded in the Tethyanrealms are part of a series of events affecting the whole Middle Cretaceous ocean-atmosphere system and biogeochemical cycling. The work proposed here will

result in an improved understanding of these events.2. The impact of these events is recorded and best known in deep-water deposits in

the Tethyan and Atlantic realms. The sedimentary expression of the sub-equatorialPacific settings introduced here is poorly known, but they are also recorded in thesub-equatorial Pacific settings, and are thus of global rather than regional origin.

3. Middle Cretaceous carbonate platform systems responded sensitively to this seriesof events. This is manifested by changes of the carbonate producing community,carbonate production rate or by the demise of the shoal-water ecosystem.

3.2. Methods

In order to test these hypotheses, it is proposed to use the following working approach:1. Establish a detailed litho-, bio- and sequence-stratigraphic framework of the deep-

water realm during the Middle Cretaceous in the above-mentioned regions (Oroya-Cerro de Pasco regions, Cajamarca-Amazonas-Lancones regions) for correlatingwith Tethyan realm sequences.

2. Characterize the depositional setting and palaeoenvironmental conditions(hydrodynamic level, trophic levels, etc.) at these localities.


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3. Establish a detailed chronostratigraphy of both deep- and shallow-water sectionsusing carbon- and Sr-isotope chemostratigraphy in combination withbiostratigraphic data.

4. Establish high-resolution multi-proxy records of palaeoenvironmental changesrecorded in the North and Central Andes using the deep-water setting record(Cajamarca-Amazonas regions), and compare it with the Tethyan realm.

5. Investigate the response of carbonate-dominated water settings to the multi-eventpalaeoenvironmental perturbations occurring during the Upper Aptian to EarlyCenomanian interval.

6. Provide a regional correlation established across shallow- to deep-water trendsfrom east to west in the Central Andes

7. Correlate the different settings and assess their link/interaction on a regional andglobal scale.

3.2.1. Fieldwork

Two regional field areas are envisaged for this project. They correspond to basinal-dominated setting sections for the first one (Oroya-Cerro de Pasco regions), and toplatform-dominated settings for the second one (Cajamarca, Amazonas and Lanconesregions) (Fig. 3). Fieldwork will involve detailed sections logging, sedimentologicalanalysis of depositional environments, field-based sequence stratigraphic interpretationand sampling. Marls and micrite-rich rocks will be favoured for bulk-rock geochemicalanalyses, whereas systematic collection of ammonites will be undertaken forbiostratigraphic analyses, as well as well preserved bivalves or belemnites forstrontium, carbon and oxygen isotope analyses.

Field-work areas:Oroya-Cerro de Pasco regions (Deep to-shallow-water settings): The clastic non-marine rocks of the Valanginian-Aptian age are overlain by marine marls andlimestones bearing rich molluscan assemblages. They have a thickness of about 1000meters in the Cerro de Pasco-Pomachaca region (Benavides, 1956; Jaillard, 1986). Inthis region, black laminated deep-water limestone of the Pariatambo Formation are

overlaid by 800 meters of very massive, thick-bedded, shallow-water dolomites andlimestones of the Jusmacha Formation. This later is dated from the latest Albian-Turonian interval. The Jusmasha Formation in Cajarmarca-Amazonas regin iscorrelated by the Pulluicana and Quillquiian Groups and by the Cajamarca Formation(Benavides et al., 1956).

Cajamarca-Amazonas-Lancones regions (Deep-to-shallow-water settings): The MiddleCretaceous system in this region is one of the best-developed and most fossiliferousCretaceous sequences in sub-equatorial Pacific settings (Hedberg, 1942; Benavides,1956; Hillebrandt, 1970; Mourier et al., 1986; Jaillard, 1986; Mourier et al., 1988;Mourier, 1988). In Cajamarca-Amazonas, the Middle Albian is represented by black,laminated deep-waters limestone of the Pariatambo Formation (Fig. 4). This latter isoverlying thin bedded, light gray limestone, with minor beds of sandy shale from the

Inca-Chulec Formations (Upper Aptian-Middle Albian age; Benavides, 1956). The LateAlbian to Early Cenomanian time is represented by gray marls and shallow waterslimestone of the Pulluicana Group. These sequences are well exposed in Cajamarcaregion and have a maximum thickness of 2000 meters. In Lancones, the Albiancarbonate shelf is represented by a thick succession of grey to black laminatedbituminous marls and limestones, which exhibit very thin calcarenites and greywackes,the thickness reaches at least 300 meters and they correspond to the MuertoFormation (Early Albian to early Late Albian age; Bristow and Hoffstetter, 1977;Shoemaker, 1982; Jaillard et al., 1999).


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Litho- and sequence stratigraphy: Depositional and diagenetic Fabrics will bedetermined using thin-section petrography and polished slabs description. This willcomplement field work observations such as top and-bottom criteria, stacking-patterns,indications of lamination and bedding, and assessment of burrowing textures, which inturn may contribute to the formation of nodular structures, along with various diageneticprocesses. A high-resolution sequence stratigraphic scheme will be established using acombination of sequence stratigraphy and cyclostratigraphy developed for deep-shallow-water carbonate platforms (Strasser et al., 2000). Depositional sequences ofdifferent scales are interpreted from detailed field-work, section logs and microfaciesanalysis. The smallest cycle of environmental change recognizable in the rock record iscalled elementary sequence. It is the basic architectural element that composes small-scale, medium-scale, and large-scale sequences, all of which again show characteristicfacies evolutions. The stacking of theses sequences frequently shows a hierarchicalpattern, which then is compared between the different sections that are also correlatedby independent methods such as biostratigraphy and chemostratigraphy. By thismeans, a best-fit correlation that satisfies the large-scale stratigraphic framework aswell as the stacking pattern will be established; this will allow to filter out depositionalsequences formed by autocyclic processes and to identify local or regional gaps in thesedimentary record. If the stacking pattern reflects a hierarchy that is comparable to theone created by orbital forcing (Milankovitch cyclicity) and if Sr-isotope dating confirmsthat the duration of the smaller-scale depositional sequences lies within theMilankovitch frequency band, then a rather precise time framework in the range of 20to 100 ka can be established.

Given that this high-resolution time framework from cyclostratigraphicinterpretation is successfully established, the sedimentary system can be analysed ingreat detail: e.g., rates and volumes of sediment production and transport can beestimated, ecological changes can be monitored (Dupraz and Strasser, 1999). Finally,the relation between climate change (inferred from ecology and sediment composition)and sea-level history (inferred from the high resolution sequence-stratigraphicinterpretation) can be analyzed with a resolution that is close to that of Cenozoicstudies where relevant data are much more abundant (Rameil, 2005).

Carbonate platform ecology: In order to trace changes in the carbonate depositionalmode, the main contributors to the carbonate budget will be assessed by qualitativeand semi-quantitative analysis from facies association determined during field-workand micro-facies analysis. Three main modes of carbonate factories are generallyrecognized during the Mesozoic (e.g. Fllmi et al., 2006; Immenhauser et al., 2005;Bodin et al., 2006): Photozoan-, heterozoan- and microbial-dominated ecosystems.Each carbonate ecosystem can be associated to specific palaeoceanographicconditions (nutrient levels, sea-surface temperature, etc) during the Early Cretaceous.This study will thus test if the same can be observed during the Middle Cretaceous.

3.2.2. Laboratory

A major objective of this project will be the establishment of a detailedchemostratigraphic framework. Two main tools are applied: (1) Detailed carbon-isotopestratigraphy of fine-grained matrix micrite. The goal is the recognition of the characteristic 13C pattern characterizing the Upper Aptian Early Cenomanian interval. Theresulting carbon-isotope curve will be compared and correlated with existing Europeanrecords (e.g., Fllmi et al., 2006; Jarvis et al., 2006), (2) Sr-isotope stratigraphy usingselected low-Mg shell material from larges bivalves, brachiopods or belemnites,frequent in the North and Central Andes of Peru. In order to select pristine low-Mgcalcite shells a number of optical and geochemical screening tests will be applied as


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described below. All sedimentological and geochemical analyses will be performed inthe laboratory of Ruhr-University Bochum.Carbon and oxygen isotope analysis will be done from samples of fine-grainedcarbonate matrix-micrites, marine cements (where present) and low-Mg calcite shellswill be analyzed on a Thermo Finnigan MAT 252 ratio mass spectrometer. Thinsections of selected organisms will be investigated for their Cathode Luminescence(CL). Shell or rostra material that has been selected based on its uniform non-luminescent pattern is then examined under the Scanning Electron Microscopy in orderto recognize the fibrous prismatic ultra-structure of the bivalve-brachiopods shell orpreserved lamina in belemnite rostra. Trace elemental analyses based on compositionsof selected low-Mg calcite shells and rostra will be performed in order to recognize thediagenetically least affected material (see details in Steuber, 1999). Strontium-isotopeanalysis using 87Sr/ 86Sr isotopic ratio of low-Mg calcite shells and rostra of screenedspecimens, selected for their pristine trace element composition is of key importancefor this study. All these laboratory analyses will be done with the facilities of thedepartment at Bochum.

3.3. Work schedule

Below it shows a detailed working programme for the three years of the PhDprogramme suggested.

1st year: Platform setting - The first two months of the project are dedicated to thefamiliarization (literature study, work with existing thin section material, etc.) of theresearch topic. Subsequently, field-work in the Oroya-Cerro de Pasco region is planned(3 weeks). Goals of the fieldwork include a detailed litho-, bio- and sequence-stratigraphic framework of selected sections that cover the Upper Aptian EarlyCenomanian interval. Then, back in Bochum, hand specimens for thin-sectionfabrication are selected and thin sections ordered. Stratigraphic sections must bedrawn and the field-based sequence stratigraphy is tested and refined based on thin-section investigations. The next step includes a detailed sampling of selected handspecimens for a detailed carbon-isotope chemostratigraphy, clay mineralogy, and

screening of selected shells and rostra for Sr-isotope stratigraphy. A compile detaileddata will be done relating to carbon and oxygen isotope stratigraphy and measure the87 Sr/ 86Sr ratio of selected belemnite, brachiopod and bivalve specimens. The remainingtime of the first year is dedicated to the compilation and, where necessary completion,of the chemostratigraphic, lithostratigraphic and sequence stratigraphic framework. Afirst summary and report of the activities and the outcome of the Oroya-Cerro de Pascoregion study will be compiled.

2nd year: Basinal setting - The beginning of the second year is mainly dedicated tofieldwork in the Cajamarca-Amazonas-Lancones regions (23 weeks). The field-workinclude a detailed litho-, bio- and sequence-stratigraphic framework of selectedsections that cover the Upper Aptian Early Cenomanian interval, then, to correlate itwith the sequences taken in Oroya-Cerro de Pasco region. The goal here is increase

the resolution of the chemostratigraphic study from this long Cretaceous basin. Bulk-rock marly samples from the Cajamarca-Amazonas-Lancones sections will be collectedand analysed with average sampling increments of 0.5 m for their carbon-isotope andclay mineral signatures. Bivalves, brachiopods and belemnites will be sampled for Sr-isotope stratigraphy and oxygen isotope palaeo-temperature purposes. After that, apreliminary first publication will be proposed.

3rd year: Platform setting - The 3rd year will be more concentrated on writing paper,with a short clean-up field-trip to the previous studied regions (2-3 weeks). This yearalso will include compilation of data, comparison the sub-equatorial Pacific data sets


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(Northern and Central Andes of Peru) with the Tethyan realm, data integration andinterpretation. Finally, publishing of the PhD thesis.

Figure 3 - Map of Peru where possible field-work in the Oroya-Cerro de Pascoregions and the Amazonas-Cajamarca-Lancones regions are beingrecommended.


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Figure 4 - Stratigraphic section near to the Cajamarca region, loggedduring a field-reconnaissance trip.


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4. References

Allan, J.R. and Matthews, R.K., 1982. Isotope signatures associated with earlymeteoric diagenesis Sedimentology 29,797-81 7.

Arthur, M.A., Jenkyns, H.C., Brumsack, H.-J., Schlanger, S.O., 1988. Stratigraphy,geochemistry, and paleoceanography of organic carbon-rich Cretaceoussequences. In: Ginsburg, R.N., Beaudoin, B. (Eds.), Cretaceous resources,events and rhythms: Background and plans for research: Digne, France, KluwerAcademic Publishers, p. 75-119.

Arthur, M.A., Jenkyns, H.C., Brumsack, H.-J., Schlanger, S.O., 1990. Stratigraphy,geochemistry and paleoceanography of organic-rich Cretaceous sequences. In:Ginsburg, R.N., Beaudoin, B. (Eds.), Cretaceous resources, events and rhythms,NATO ASI Series, Serie C: Mathematical and Physical Sciences, 304, KluwerAcademic Publishers, Netherlands, p. 75-119.

Bengtson, P. and Jaillard, E., 1997. Stratigraphic revision of the Upper Cretaceous ofthe Peruvian-Ecuadorian border region: preliminary data. Proceedings 18th I.A.S.Region. Europ. Meet. Sediment. - 2nd Europ. Meet. Paleont. Stratig. SouthAmerica, Gaea heidelbergensis, 4, 71-72, Heidelberg.

Benavides, V., 1956. Cretaceous system in Northern Peru. American Mus. Nat. Hist.Bull., Nueva York, 108: 352 494.

Blakey, R., 2011. Global Paleogeographic map of the Middle Cretaceous, Website:http://cpgeosystems.com/index.html .

Bodin, S., Godet, A., Vermeulen, J., Linder, P., Fllmi, K.B., 2006. Biostratigraphy,sedimentology and sequence stratigraphy of the latest Hauterivian - earlyBarremian drowning episode of the Northern Tethyan margin (Altmann Member,Helvetic nappes, Switzerland). Eclogae geologicae Helvetiae 99, 157-174.

Bristow, C.R. and Hoffstetter, R., 1977. Ecuador. Lexique Stratigraphique InternationalV, 5a2, CNRS ed. Paris, pp. 410.

De Boer, P.L., 1982. Cyclicity and storage of organic matter in middle Cretaceouspelagic sediments. In: Cyclic and Event stratification (ed. By G. Einsele and a.Seilacher), 456-474, Springer-Verlag, New York.

Dupraz, C., Strasser, a., 1999. Palontologie, palocologie et volution des facis

rcifaux de l'Oxfordien Moyen-Suprieur (Jura suisse et franais). GeoFocus, v.2: Fribourg, Institut de gologie et palontologie de l'Universit de Fribourg, 239p.

Erba, E., 1992. Calcareous nannofossil distribution in pelagic rhythmic sediments(Aptian-Albian Piobbico core, Central Italy). Rivista Italiana di Paleontologiaestratigrafia, 97; 455-484.

Erba, E., 2004. Calcareous nannofossils and Mesozoic oceanic anoxic events. MarneMicropaleontology 52, 85106.

Erbacher, J., Huber, B.T., Norris, R.D., Markey, M., 2001. Increased thermohalinestratification as a possible cause for an ocean anoxic event in the Cretaceousperiod. Nature 409, 325-327.

Erbacher, J., Thurow, J., Littke, R., 1996. Evolution patterns of radiolaria and organicmatter variations: A new approach to identify sea-level changes in mid-

Cretaceous pelagic environments. Geology 24, 499-502.Fischer, A.G., Herbert, T.D., Napoleone, G., Premoli Silva, I. and Ripepe, M., 1991.Albian pelagic rhythms (Piobbico core). Jour. Sed. Petrol., 61:7: 1164-1172.

Frakes, L.A., 1999. Estimating the global thermal state from Cretaceous sea surfaceand continental temperature data. Geological Society of America Special Paper332, 4957.

Fllmi, K.B., Godet, A., Bodin, S. and Linder, P., 2006. Interactions betweenenvironmental change and shallow-water carbonate build-up along the northernTethyan margin and their impact on the early Cretaceous carbon-isotope record.Paleoceanography, 21, PA4211.


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