Large igneous provinces and organic carbon burial: Controls on global temperature and continental weathering during the Early Cretaceous

    Large igneous provinces and organic carbon burial: Controls on global temperature and continental weathering during the Early Cretaceous St´ephane Bodin, Philipp Meissner, Nico M.M. Janssen, Thomas Steuber, J¨org Mutterlose PII: DOI: Reference:

S0921-8181(15)30020-5 doi: 10.1016/j.gloplacha.2015.09.001 GLOBAL 2322

To appear in:

Global and Planetary Change

Received date: Revised date: Accepted date:

16 October 2014 6 August 2015 1 September 2015

Please cite this article as: Bodin, St´ephane, Meissner, Philipp, Janssen, Nico M.M., Steuber, Thomas, Mutterlose, J¨org, Large igneous provinces and organic carbon burial: Controls on global temperature and continental weathering during the Early Cretaceous, Global and Planetary Change (2015), doi: 10.1016/j.gloplacha.2015.09.001

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ACCEPTED MANUSCRIPT Large igneous provinces and organic carbon burial: Controls on global

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temperature and continental weathering during the Early Cretaceous

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Stéphane Bodin1*, Philipp Meissner1, Nico M.M. Janssen2, Thomas Steuber3, Jörg

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Mutterlose1

Ruhr-Universität Bochum, Institut für Geologie, Mineralogie und Geophysik, D-44870

Emirates

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Petroleum Geosciences, The Petroleum Institute, PO Box 2533, Abu Dhabi, United Arab

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Geertekerkhof 14bis, 3511 XC Utrecht, The Netherlands

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Bochum, Germany

* Corresponding author: [email protected]

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ACCEPTED MANUSCRIPT ABSTRACT There is an abundance of evidence for short intervals of cold climatic conditions during the

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Early Cretaceous. However, the lack of a high-resolution, long-term Early Cretaceous

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paleotemperature record hampers a full-scale synthesis of these putative ―cold snap‖ episodes, as well as a more holistic approach to Early Cretaceous climate changes. We present an extended

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compilation of belemnite-based oxygen, carbon and strontium isotope records covering the

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Berriasian – middle Albian from the Vocontian Basin (SE France). This dataset clearly demonstrates three intervals of cold climatic conditions during the Early Cretaceous (late

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Valanginian – earliest Hauterivian, late early Aptian, latest Aptian – earliest Albian). Each of these intervals is associated with rapid and high amplitude sea-level fluctuations, supporting the

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hypothesis of transient growth of polar ice caps during the Early Cretaceous. As evidenced by positive carbon isotope excursions, each cold episode is associated with enhanced burial of

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organic matter on a global scale. Moreover, there is a relatively good match between the timing and size of large igneous provinces eruptions and the amplitude of Early Cretaceous warming episodes. Altogether, these observations confirm the instrumental role of atmospheric CO2 variations in driving Early Cretaceous climate change. From a long-term perspective, the coupling of global paleotemperature and seawater strontium isotopic ratio during the Early Cretaceous is best explained by temperature-controlled changes of continental crust weathering rates. Keywords Paleotemperature reconstruction; Belemnites; Oceanic Anoxic Events; Late Aptian cold snap 2

ACCEPTED MANUSCRIPT Highlights The Early Cretaceous greenhouse was punctuated by three coldhouse episodes

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Coldhouse episodes are comparable with Maastrichtian and Paleocene cold snaps

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Widespread burial of organic matter may have initiated the cooling episodes

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Warming events are associated with large igneous provinces activity

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Correlation between global temperature and evolution of marine Sr isotope ratio

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1. Introduction

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The Mesozoic climate is traditionally seen as warm and equable, but evidence for more dynamic climate is mounting. Deviations from the normal greenhouse state, either toward an

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coldhouse/icehouse or a hothouse state, have been inferred based on sedimentological,

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paleontological and geochemical observations (e.g. Kemper, 1987; Weissert and Lini, 1991;

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Price, 1999; Miller et al., 2005; Tejada et al., 2009; Suan et al., 2010). Documentation of global paleotemperature changes have been established for the Jurassic and the middle to Late Cretaceous (e. g., Dera et al., 2011; Friedrich et al., 2012). However, a robust and detailed record embracing the entire Early Cretaceous is still missing. Previous high-resolution studies have mainly focused on the Late Cretaceous, clearly documenting that the Cenomanian-Turonian was a phase of super-greenhouse conditions, followed by a long term cooling reaching a minimum in the Maastrichtian (Huber et al., 2002; Pucéat et al., 2003; Jenkyns et al., 2004; Forster et al., 2007; Friedrich et al., 2012; Linnert et al., 2014). The Early Cretaceous record is patchier and only few attempts have proposed long-term paleotemperature reconstructions (Podlaha et al., 1998; Pucéat et al., 2003; Price and Mutterlose, 2004; McArthur et al., 2004, 2007b; Weissert

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ACCEPTED MANUSCRIPT and Erba, 2004; Prokoph et al., 2008; Bodin et al., 2009; Mutterlose et al., 2014b; Bottini et al., 2015).

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Ample (up to 50 m) and rapid (<1 My) global sea-level fluctuations during specific parts of

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the Early Cretaceous have often been reported (Immenhauser and Scott, 2002; Gréselle and Pittet, 2005, 2010; Bover-Arnal et al., 2009, 2014; Rameil et al., 2012; Maurer et al., 2013).

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These studies suggest glacio-eustasy during the late Valanginian, the late early Aptian and the

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latest Aptian – earliest Albian. Although tentative comparison with oxygen-isotope record have been brought forward by some authors to back-up their claim of cold climate and therefore

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glacio-eustasy (e.g., Maurer et al., 2013; Haq, 2014), these latter are nonetheless strongly impaired by the fact that the O-isotope records were derived from bulk-rock analyses. In these

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cases, diagenetic overprints, as well as mixed benthic-planktonic signals, cannot be discounted and precisely quantified. Notable here is the belemnite clumped-isotope study by Price and

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Passey (2013) providing evidence for cooler late Valanginian climate compatible with polar ice. Independent support for intermittent cold climate during the Early Cretaceous is provided by paleontological observations and TEX86 paleothermometry (e.g., Mutterlose et al., 2009; McAnena et al., 2013), and the presence of earliest Cretaceous (Berriasian-Valanginian) tillite deposits in Australia (Alley and Frakes, 2003). Additional cold condition indicators, such as icerafted debris or glendonites (Kemper, 1987; Frakes et al., 1995), have been questioned (e.g., Markwick and Rowley, 1998; Teichert and Luppold, 2013). If the veracity of cold climatic episodes during the Early Cretaceous stands up scrutiny, then it becomes necessary to understand and assess the factors driving Earth’s climate into and out of transient icehouse states during the overall Mesozoic greenhouse. On one hand, enhanced carbon burial has been proposed as a key driver associated for some episodes of global cooling (Barclay 4

ACCEPTED MANUSCRIPT et al., 2010; Jarvis et al., 2011; McAnena et al., 2013; Hollis et al., 2014). It remains, however, uncertain if such systematic causal link can be established throughout the entire Cretaceous (e.g.,

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Heimhofer et al., 2004). Alternatively, vast neritic carbonate factory demise or large volcanic

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aerosol emissions have been proposed as potential triggers for cooling episodes (Donnadieu et al., 2011; Bryan and Ferrari, 2013). On the other hand, Large Igneous Province (LIP) eruptions

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have been suspected to initiate and control global warming events (Kidder and Worsley, 2010;

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Bryan and Ferrari, 2013). Although a strong link between the eruption of the Ontong-Java Plateau and the early Aptian OAE 1a warming has been established (e.g., Méhay et al., 2009;

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Tejada et al., 2009; Bottini et al., 2012), this is however not the case for the other Early Cretaceous LIPs (e.g., Martinez et al., 2013). This observation questions thus the impact of LIP’s

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eruption on global climate.

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Lying at the crossroad of Earth’s thermostat system, continental weathering is one of the key

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processes linking atmosphere, hydrosphere and biosphere (e.g., Berner et al., 1983). Given that chemical weathering is strongly dependent on temperature (e.g., Hay, 1998) and that there is a positive correlation between global temperature and the strength of the hydrological cycle (e.g., Hay et al., 2002), it is expected that Early Cretaceous climate change will be mirrored by a change of continental weathering on a global scale. So far, this link has only been verified for short-term extreme episodes of Oceanic Anoxic Events (OAE) (Blätter et al., 2011; Bodin et al., 2013; Pogge von Strandmann et al., 2013), but it remains yet to be assessed on a longer time scale. In this paper, we present new belemnite stable isotope data (δ18O, δ13C and 87Sr/86Sr) for the uppermost Barremian to middle Albian of the Vocontian Basin, southeast France. These are combined with previously published belemnite records from the same basin (Kennedy et al., 5

ACCEPTED MANUSCRIPT 2000; van de Schootbrugge et al., 2000; Van de Schootbrugge, 2001; McArthur et al., 2007b; Bodin et al., 2009) in order to obtain a continuous record of ca. 30 Myr (late Berriasian – middle

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Albian interval), spanning the main paleoceanographic events of the Early Cretaceous. In concert

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with the compilation of the timing of suspected glacio-eustasy, LIPs emplacement and oceanic crust production, inferences about global paleotemperature changes, enhanced organic carbon

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burial and changes in continental weathering rates are made in the context of Cretaceous

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dynamic climate. Finally, based on the assemblage of the datasets of Zachos et al. (2001), Niebuhr and Joachimski (2002), Cramer et al. (2009), Dera et al. (2011), Friedrich et al. (2012)

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and this study, a tentative 200 Ma record of global paleotemperature change is presented and

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briefly discussed.

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2. Methods and studied sections

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We present an extensive dataset of oxygen, carbon and strontium stable isotope data obtained from Early Cretaceous belemnites of southeastern France (Vocontian Basin, ~30°N paleolatitude; Dercourt et al., 1993; Fig. 1). A total of 203 published isotopic results measured on well-preserved belemnite rostra (Kennedy et al., 2000; Van de Schootbrugge et al., 2000; McArthur et al., 2007b; Bodin et al., 2009) have been compiled and complemented by 79 new analyses covering the late Barremian to middle Albian interval (Table 1 in supplementary material). Seven well-known localities were visited in the Vocontian Basin (Angles – Combe Lambert, Glaise l’Ermitage, Serre Chaitieu, Beaudinard Gaubert, Bellecombe-Tarendol, Col de Palluel – Ravin des Jassines, Col de Pré-Guittard; Figs. 1–2) where a detailed litho-biostratigraphy has been previously established (Bréhéret, 1997; Delanoy, 1998; Vermeulen, 2002; Joly and 6

ACCEPTED MANUSCRIPT Delamette, 2008; Gale et al., 2011). Belemnites were collected in-situ and their exact location with regard to the local lithostratigraphy was documented using published detailed

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sedimentological logs. All analyzed belemnites have later been placed within the Tethyan

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ammonite biostratigraphic scheme (up to the ammonite sub-biozone resolution) using the wellestablished ammonite biozonation of the Vocontian Basin (Fig. 2). This was finally calibrated to

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the numerical ages of the time scale of Gradstein et al. (2012).

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In order to assess the pristine state of the collected belemnites, diagenetic screening was performed by combining visual inspection and chemical analyses. The belemnites showing

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translucent light golden brown calcite, with the presence of a few very thin black rings were considered as optically well-preserved and further analyzed for their major and trace element

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concentrations (Ca, Mg, Sr, Fe, Mn). The analyses were performed with an ICP-OES (iCap 6500 Thermo Electron Corporation) at the Ruhr-University Bochum. Samples (~1.5 mg) were

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prepared by dissolving in 3 M HNO3 (1 ml) and 2 ml H2O. Reproducibility was verified by synchronously analysing internal standards. Belemnites with [Fe] > 200 ppm and [Mn] > 50 ppm were considered as altered and not further analyzed. Carbon- and oxygen-isotope analyses were performed on 79 belemnite samples using a Gasbench II coupled to a Finnigan MAT 253 mass spectrometer at the Ruhr University of Bochum. For each sample, 0.4 mg of powder was weighted in vials and dried for 48 hours in a 105°C preheated oven and subsequently cooled in a refrigerator for 1 hour. The air present in the vials was flushed using helium in order to avoid any contamination. Carbonates were sublimated by adding anhydrous phosphoric acid (104%) using an auto-sampler. The quality of the measurements was controlled by NBS19, NBS18 and RUB internal standards. Isotope data were

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ACCEPTED MANUSCRIPT corrected using CO1 and CO8 carbonate standards. The reproducibility (3
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A total of 46 belemnites (17 in Ruhr University Bochum, 8 in Royal Holloway, University of London and 21 in the CSIRO Radiogenic Isotope Facility, Australia) were analyzed for their

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strontium isotope ratios (87Sr/86Sr). In Bochum, strontium was separated with standard ion-

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exchange methods and loaded onto a rhenium filament, then measured with a thermal ionization

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mass-spectrometer (Finnigan MAT 262) in dynamic mode. Total blanks of strontium were less than 0.09 ng. The long-term mean of ratios for reference materials (USGS EN-1, NIST SRM

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987) measured in 2009–2010 at the stable isotope laboratory in Bochum are 0.709171 (n=23; 2σ mean=7.0*10−6) and 0.710249 (n=23; 2σ mean=6.0*10−6) respectively. The mean of standards

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run together with samples analyzed during the time of data collection for this study is 0.709168

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SRM 987.

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(n=5; 2σ mean=5.0*10−6) for USGS EN-1 and 0.710252 (n=5; 2σ mean=6.0*10−6) for NIST

In Royal Holloway, the picked samples were dissolved in 3 ml of dilute ultrapure nitric acid and the solutions centrifuged. The supernatant was evaporated to dryness with addition of HCl, and taken up in 4 M ultrapure HCl. The Sr was separated using Sr-Spec ion-exchange resin on micro-columns made from 1ml pipette tips. After separation and evaporation to dryness, samples were loaded onto Ta filament and run in dynamic, peak-hopping mode, on a VG 354 TIMS in the Radiogenic Isotope Laboratory at RHUL. External precision of 0.000015 on

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Sr/86Sr was

measured by running multiple loadings of NIST 987 before, during and after the isotopic measurements were made. A similar procedure was used at the CSIRO lab. There, the estimated external precision there (2sem) is based on the analysis of the NBS 987 standard over the period

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ACCEPTED MANUSCRIPT of analysis and was 0.0025% (+/-0.000018). All strontium-isotope ratios presented in this study were adjusted to NIST 987 value of 0.710248.

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3. Results

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3.1. Oxygen isotopes

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A long-term trend in δ18Obel from ca. 0‰ toward more negative values of ca. -0.5‰ throughout the latest Berriasian to late Barremian is followed by a long-term increase of δ18Obel

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values ending in the latest Aptian (ca. 0.5‰). A rapid decrease of δ18Obel follows during the

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Albian (Fig. 3) and reaches ca. 1‰ in the middle Albian. This secular trend is punctuated by short-term excursions toward positive oxygen isotopes values in the late Valanginian and in the

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late early Aptian. Pronounced negative δ18Obel values are recorded in the early Barremian and at

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the Barremian-Aptian boundary. No belemnites have been collected within the Goguel level

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(Oceanic Anoxic Event (OAE) 1a equivalent). 3.2. Carbon isotopes

The secular evolution of belemnite stable carbon isotope (δ13Cbel, Fig. 3) is best described by a long-term rise from the latest Berriasian (ca. -1‰) to the middle Aptian (ca. 3 – 4‰), followed by a long-term decline until the middle Albian (ca. 1‰). This trend is interrupted by three shortlived positive excursions during the middle Valanginian (ca. 1‰), early Aptian (ca. 3 – 4‰) and latest Aptian (ca. 2 – 3‰). This secular trend correlates well with the micrite record in the Vocontian Basin (Reichelt, 2005; Herrle et al., 2004; Föllmi et al., 2006) as well as from other key Tethyan, Atlantic and Pacific localities (e.g., Bralower et al., 1999; Föllmi et al., 2006; McAnena et al., 2013; Fig. 4). Although the coverage of the carbon isotope record from organic matter is less complete than that from carbonates, positive excursions of δ13Corg have also been 9

ACCEPTED MANUSCRIPT reported for the middle Valanginian (Lini et al., 1992), the late early Aptian (Menegatti et al., 1998) and the late Aptian (McAnena et al., 2013; Fig. 4). The δ13Cbel record from the Vocontian

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Basin is therefore tracing global changes within the exogenic carbon cycle. Due to the absence of

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collected belemnites within the Goguel Level, we were unable to observe the negative carbon

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isotope excursion from the base of the OAE 1a (Menegatti et al., 1998; Westermann et al., 2013). 3.3. Stable strontium isotopes 87

Sr/86Sr isotopic curve follows the general pattern recognized for the

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The belemnite-based

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Early Cretaceous by McArthur et al. (2001), but with a higher resolution and accuracy (Fig. 3). Since each belemnite can be precisely placed within the Vocontian Basin lithostratigraphy and

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the Early Cretaceous ammonite zonation (Fig. 5), some stratigraphically important observations,

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independent from any age calibration (and therefore any future revisions of the geological time scale), are noted here:

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a. As already described by McArthur et al. (2004) for the Boreal Realm, the first Cretaceous inflection of the marine

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Sr/86Sr curve (0.707486 ±σ 0.000012; n=9), from rising to declining

trend, occurs during the late early Barremian, and therefore clearly predates the onset of the OAE 1a (by ca. 4 Myr according to the timescale of Gradstein et al., 2012). b. The marine 87Sr/86Sr value characterizing the uppermost part of the earliest Aptian carbon isotope segment C2 (Fig. 6) of Menegatti et al. (1998) is 0.707421 ±σ 0.000007 (n=6). This confirms the results of Huck et al. (2011) derived from rudist shells. c. The 87Sr/86Sr isotope value near the end of the Goguel Level (lower part of carbon isotope segment C7 of Menegatti et al. (1998), according to Westermann et al., 2013; Fig. 6) is 0.707344 ±σ 0.000015 (n=4).

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ACCEPTED MANUSCRIPT d. The early – late Aptian boundary (Fig. 5) is marked by a marine

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Sr/86Sr value of

0.707301 ±σ 0.000010 (n=3). 87

Sr/86Sr curve (0.707196 ±σ 0.000014; n=7), from

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e. The second inflection of the marine

declining to rising trend, occurs during the latest Aptian (Fig. 5), after the deposition of the Jacob

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Level (first sub-level of OAE 1b) and before the onset of the Kilian Level (2nd sub-level of OAE

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1b), that marks the Aptian-Albian boundary according to Petrizzo et al. (2012).

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Within the broad Early Cretaceous sine curve described by

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Sr/86Sr values, three

noteworthy changes of slope steepness can be observed. Firstly, an accelerated rate of

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Sr/86Sr

the marine

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increase occurs during the early Hauterivian. Secondly, during the Barremian – Aptian transition, 87

Sr/86Sr values seems to be stagnant, before showing slightly accelerated decline

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rates coeval to the OAE 1a and its aftermath. Finally, during the early late Aptian, a strong reduction in the rate of decrease is observed.

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4. Interpretation – discussion

4.1. Secular temperature changes The stable position of the Vocontian Basin around 30° North throughout the Early Cretaceous (Fig. 1b) excludes paleolatitudinal changes as potential causes of the observed carbon and oxygen isotopic shifts. Given that all the belemnites originate from a single basin, potential biases linked to interbasinal correlation are also avoided. Vital effects are also minimized since the isotopic data have been retrieved from a single taxon (i.e., belemnite), although intergeneric or interspecific variations in biofractionation are possible (e.g., McArthur et al., 2007a; Ullmann et al., 2014).

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ACCEPTED MANUSCRIPT Since all the presented belemnites have passed through diagenetic screening, we interpret the δ18Obel signal as being primarily driven by paleotemperature and δ18Oseawater changes. The two

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short-lived negative excursions in the Barremian have also been observed in the Boreal Realm

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(Mutterlose et al., 2010) and therefore seem to be rather related to paleoenvironmental conditions than to diagenetic processes. However, a comparison with TEX86 palaeothemometry data

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(Mutterlose et al., 2014b) highlights that they cannot be explained by short-lived warming

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episodes. These short-lived negative oxygen-isotope excursions might therefore be rather linked to changes in seawater isotopic budget (labeled ―δ18Osw events‖ in Fig. 3), either due to enhanced

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vertical mixing of water masses (Bodin et al., 2009) or to massive inflow of continental freshwater. Interestingly, both events coincide with increased kaolinite content in the Vocontian

Mutterlose et al., 2014a).

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Basin, interpreted by Godet et al. (2008) as reflecting wetter climatic conditions (see also

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There is a very good correspondence between the intervals of positive δ18Obel values and the purported cool climatic (icehouse) intervals of the Early Cretaceous (Figs. 3 and 4), as deduced by sedimentological, paleontological and geochemical observations (Hochuli et al., 1999; BoverArnal et al., 2009; 2014; Gréselle & Pittet, 2010; Maurer et al., 2013; McAnena et al., 2013; Price and Passey, 2013). This strengthens our interpretation that the secular δ18Obel trend in the Vocontian Basin belemnites is primarily driven by sea-water paleotemperature. It confirms moreover the assertions of dynamic climate change during the Early Cretaceous, which has alternated between a normal greenhouse mode and episodic coldhouse phases. For the late Aptian cooling, the amplitude of the δ18Obel shift is in the order of 1‰ which could translate into a ca. 4°C cooling if no changes in δ18Oseawater is taken into account (Fig. 4). This compares well with the amplitude of the sea surface temperature (SST) changes calculated 12

ACCEPTED MANUSCRIPT by McAnena et al. (2013) from their TEX86 data and would then be contradictory to the hypothesis that transient ice-sheets have grown during the late Aptian cooling. However, as it

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appears that δ18Obel values are likely capturing a deep-water δ18O signal (see below), it is

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possible that only part of this 1‰ amplitude shift is linked to temperature change given that change in SST are not necessarily of same amplitude as in the deep-water. According to Maurer

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et al. (2013), the late Aptian sea-level drop was at least 50m. If this is entirely linked to glacio-

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eustasy, given the fact that total melting of present polar icecaps and glaciers would lower the δ18Oseawater value to -1‰ (SMOW) and that this would raise the sea-level by 70m, one can

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calculate that only 30% of the late Aptian δ18Obel shift is linked to temperature, representing a ca. 1.2°C cooling of deep-water during the late Aptian. The Valanginian cooling is only recorded by

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a 0.5‰ positive shift of the δ18Obel values. This is half the amplitude of the Aptian cooling. Two hypotheses can thus be formulated. On the one hand, the Valanginian cooling could have been

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less ample than the Aptian one. On the other hand, one could also argue that local temperature conditions did not change significantly in the Vocontian Basin during the Valanginian, and that δ18Obel values are only recording the change in δ18Oseawater signal. Further studies are needed here to disentangle the temperature from the δ18Oseawater signal in order to assess the veracity and true extent of polar ice sheet during the Valanginian and the late Aptian, as well as to disentangle the regional from the global signal recorded here. The absence of belemnites within the Goguel Level (OAE 1a equivalent) does not allow comparing its peak temperature to the rest of the record. However, based on TEX86 data from Germany, Mutterlose et al. (2014b) have documented that it corresponds to a ca. 4°C increase compared to pre-event temperatures, which would translate into a ca. 1‰ negative shift in the oxygen isotope record (excluding changes in δ18Oseawater). This would thus give a hypothetical 13

ACCEPTED MANUSCRIPT 1.5‰ signature, much lower than any Early Cretaceous belemnite record in the Vocontian Basin (excluding the δ18Osw events of the Barremian), highlighting here the extreme nature of the OAE

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1a. According to the classification scheme of Kidder and Worsley (2010), we speculate that the

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OAE 1a is the only time interval of the Early Cretaceous having experienced the development of

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a hothouse climatic state.

4.2. Global carbon burial and Large Igneous Provinces

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Due to their influence on atmospheric carbon budget, LIPs and variations of organic carbon

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burial are often invoked as driving forces behind past climatic changes (e.g., Barclay et al., 2010; Jarvis et al., 2011; Kidder and Worsley, 2010; Hollis et al., 2014). While the role of the Ontong-

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Java LIP during the early Aptian OAE 1a seems to be well-constrained (Méhay et al., 2009;

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Tejada et al., 2009; Bottini et al., 2012), the same cannot be said for the other LIP events in the Early Cretaceous. For instance, it has long been postulated that the Paraná-Etendeka LIP was

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responsible for the middle Valanginian Weissert Event (e.g., Erba et al., 2004). However, the refinement in the dating of the LIP emplacement (Thiede and Vasconcelos, 2010; Janasi et al., 2011), combined with the Valanginian chronostratigraphy proposed in Gradstein et al. (2012), indicate that it postdates the carbon isotope perturbation (Martinez et al., 2013). Nonetheless, a recent refinement of Valanginian – Hauterivian astrochronology, suggests that the emplacement of the Paraná-Etendeka LIP coincides with the start of the Weissert Event (Martinez et al., 2015). Difficulties in tying LIP eruptions and environmental changes during the Early Cretaceous arise mostly from the scarcity of radio-isotopic dates within biostratigraphically well-dated sections, where those environmental changes are deduced from. Correlation between LIP eruptions

and

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changes

relies

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integrated

biostratigraphy,

magnetostratigraphy, chemostratiraphy and astrochronology, which can be flawed due to the 14

ACCEPTED MANUSCRIPT presence of hiatus, different interpretations or methodology accuracy. Fingerprints of LIP volcanism, such as Os or Pb isotopic records, are presently the best evidence for a link between

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the Ontong-Java LIP and OAE 1a (Tejada et al., 2009; Kuroda et al., 2011; Bottini et al., 2012),

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but similar evidences are currently lacking for the other Early Cretaceous events. Following Martinez et al. (2015), the emplacement of the Paraná-Etendeka LIP coincides

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with the onset of the Weissert Event, which is characterized by a cooling trend according to our

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long-term δ18Obel compilation (Fig 3). As such, it appears that the Paraná-Etendeka LIP did not have the same environmental impact as the early Aptian Ontong-Java LIP. This might be related

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to its relative small size and protracted activity (Dodd et al., 2015). In the Aptian – Albian, there seems to be a synchronicity of the peak activity of the LIPs activity and warming events (Fig. 3),

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supporting the claim that LIP eruptions were responsible for reinforced greenhouse condition through volcanic CO2 emissions (Bryan and Ferrari, 2013). There appears also to be a link

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between the amplitude of the warming and the areal extent (and volume) of emitted magma. Thus, the most severe episode of Early Cretaceous climate change, i.e. the Early Aptian OAE 1a hyperthermal, is associated with the Ontong-Java LIP activity (Tejada et al., 2009), which is the world largest LIP (Neal et al., 1997). Second on the list, the South Kerguelen plateau activity around 112-110 Ma (Coffin et al., 2002; Duncan, 2002; Frey et al., 2003), aided by the NauruMariana LIP (Eldhom and Coffin, 2000), is associated with the early Albian global warming. At the other end of the spatial extent spectrum, the relatively small Rajmahal LIP (Kent et al., 2002), associated with the 119-118 Ma activity of the South Kerguelen plateau, has left almost no clear imprints on the middle late Aptian global temperatures, although a transient warming event might be inferred from the few belemnite data points available. Improving the resolution of the belemnite paleotemperature record is needed here to better understand the middle Aptian 15

ACCEPTED MANUSCRIPT environmental changes. As noted by Erba et al. (2015), further revision of the available time scales is nevertheless needed to improve the temporal link between LIP and environmental

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changes. Increased organic carbon burial on a global scale has been documented during the middle –

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late Valanginian Weissert Event, the early Aptian OAE 1a and the Aptian – Albian transition

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(OAE 1b). These three events are best characterized by their associated positive carbon isotope

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excursion in both carbonate and organic matter phases (Menegatti et al., 1998; Gröcke, 1998; Bralower et al., 1999; Herrle et al., 2004; Westermann et al. (2010); McAnena et al., 2013; Figs.

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3 and 4), clearly documenting the global carbon isotope fractionation due to enhanced organic matter burial in marine and/or continental settings. For the three events, this has resulted in

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augmented sequestration of CO2 and climatic cooling (Hochuli et al., 1999; McAnena et al.,

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2013), as reflected by the coeval positive shift of δ18Obel and the inferred glacio-eustasy during

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the late Valanginian, the late early Aptian and the latest Aptian (Gréselle and Pittet, 2010; BoverArnal et al., 2009; 2014; Maurer et al., 2013; Fig. 3). Enhanced carbon burial on a global scale is therefore systematically associated with the initiation of cooling events, leading to transient icehouse states during the Early Cretaceous. 4.3. Controls on global weathering rates An important feature of the current dataset is the long-term (10 Myr resolution) coupled oxygen- and strontium-isotope records (Fig. 3). During periods of long-term temperature rise (Berriasian – Barremian, Albian), the marine

87

Sr/86Sr isotope ratio is increasing, while it is

decreasing during the long-term Aptian temperature decrease. Superimposed on this secular trend are three short-term perturbations that appear also to be correlated with short-term temperature variations. Firstly, during the late Valanginian, a slight slowdown of the 16

87

Sr/86Sr

ACCEPTED MANUSCRIPT increase (Fig. 3) appears to be correlated to the Valanginian transient cooling event. The subsequent abrupt increase of the 87Sr/86Sr values coincides with the early Hauterivian warming.

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Secondly, within the overall declining 87Sr/86Sr trend in the late Barremian – Aptian, two events

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can be noticed. During the Barremian – Aptian transition, relatively unchanging 87Sr/86Sr values are followed by a rapid decrease coeval to the OAE 1a timing. Thirdly, the early late Aptian 87

Sr/86Sr values is correlated with a relative warming before the onset of

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pseudo-plateau of the

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the latest Aptian cold climate.

Owing to the long-term residence time of strontium in seawater (~ 2–5 Myr), rapid 87

Sr/86Sr values cannot be expected (Veizer, 1989). Previous

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variations in seawater

interpretations of the seawater 87Sr/86Sr change during the Early Cretaceous attributed a leading

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role to changes in hydrothermal flux to the oceans. Thus, Larson and Erba (1999) have attributed

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the late Barremian – Aptian declining marine

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Sr/86Sr trend to the activity of the Ontong-Java

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LIP. Although such mechanism may have partly contributed to the decline of seawater 87Sr/86Sr (see below), it is unlikely to be its main cause due to timing issues (McArthur et al., 2004). Indeed, the onset of the

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Sr/86Sr decline predates the Ontong-Java LIP by ca. 4 Myr, while

another 5 Myr separates the end of the LIP activity and the end of the declining (Fig. 3).

Disentangling the mechanisms behind the evolution of seawater

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Sr/86Sr trend

Sr/86Sr has always

remained a challenge given that numerous factors are at work (Veizer, 1989; McArthur, 1994). On a long-term scale, a first-order correlation between seawater

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Sr/86Sr and global

temperatures is observed during the Early Cretaceous (Fig. 3). We interpret this long-term feature as the record of the mechanistic link between global climate and weathering rates. On the considered time-scale (107 years), changes in global weathering rates have already been invoked 17

ACCEPTED MANUSCRIPT as a driving mechanism for seawater 87Sr/86Sr (Veizer, 1989; Korte et al., 2006; Halverson et al., 2007). Because continental crust has a higher

87

Sr/86Sr value than oceanic crust, a climatically-

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driven decrease in continental weathering rates will result in a decrease of the flux of heavy Sr

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isotope to the ocean. Since the net effect of climate cooling is a decrease of both precipitation and runoff, and therefore a slowdown of weathering rates (Hay et al., 2002; Theiling et al., 2012;

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Maher and Chamberlain, 2014), we speculate that the long-term Early Cretaceous marine Sr/86Sr record is primarily driven by global paleotemperature variations. An increased

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87

contribution of the marine hydrothermal Sr flux to the oceans may have possibly aided the

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decrease of this ratio during the Aptian, but it should be noted that the emplacement of LIPs are not in tune with variation in seawater 87Sr/86Sr. For example, the Ontong-Java LIP emplacement

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coincides with a decreasing 87Sr/86Sr trend, while the late Aptian to early Albian emplacement of the Nauru-Mariana-South Kerguelen LIP complex goes along with an increasing seawater Sr/86Sr trend. The same reasoning applies for the role of oceanic crust production. Although the

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late Aptian has experienced the highest production of oceanic crust for the last 150 Myr (Larson, 1991), roughly corresponding to the Early Cretaceous

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Sr/86Sr minimum, there is otherwise no

correlation between these two parameters. A further argument to this discussion is also the recent understanding that oceanic crust hydrothermal fluids may not be the main contributor for mantlederived

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Sr/86Sr into the ocean (Allègre et al., 2010). Approximately 60% of this contribution

may rather come from the weathering of volcanic islands. Nevertheless, one can notice a small lag between the decrease of marine 87Sr/86Sr values (middle Barremian) and the decrease of longterm global T°, which starts around the Barremian – Aptian boundary. This implies that changes in global weathering rates are also not the primary driver behind the initiation of the marine

18

ACCEPTED MANUSCRIPT 87

Sr/86Sr values decline. There is currently no satisfactory explanation to account for the

initiation of this trend inversion.

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Sr/86Sr trend is even more challenging than the longer-term

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decelerating rate) of the marine

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Firmly establishing the significance of the short-term perturbations (accelerating or

changes (e.g., McArthur et al., 2007b). Adjustments in the calibration of the geological time

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scale might change the rate of Sr isotope trend. For instance, the validity of the early Hauterivian

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pulse in part rests on the short duration attributed to the early Hauterivian sub-stage (Gradstein et al., 2012). A future revision of the Cretaceous time scale may affect rate estimates. If it

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corresponds to a genuine short-term rise in the rate of increase in marine 87Sr/86Sr through time, enhanced continental weathering rates could be postulated as a driving mechanism. It should be

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noted that this Hauterivian 87Sr/86Sr pulse coincides with a sharp rise in global temperature (Fig.

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3). However, a calibration of marine Sr isotope ratio to the recently revised Valanginian –

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Hauterivian astrochronology (Martinez et al., 2015) shows no peculiar acceleration during the early Hauterivian, but confirms a pause of the rising trend during the late Valanginian, coincident with the transient coldhouse climate. Nevertheless, Weissert (1990) did observe that both late Valanginian and early Hauterivian correspond to enhanced influx of siliciclastics in the North Atlantic and Tethyan realms, which was interpreted as a consequence of enhanced continental weathering. Making the assumption that Weissert’s observations are representative for global weathering rates, this contradicts the inference made above from the short-term marine 87Sr/86Sr trend perturbation, and further highlights the need of complementary independent proxy for global weathering. The OAE 1a and its early Aptian aftermath seem to be associated with an acceleration of the marine

87

Sr/86Sr decline, after relatively steady values characterizing the Barremian – Aptian 19

ACCEPTED MANUSCRIPT transition (Fig. 5). Such acceleration of the marine 87Sr/86Sr decline was also noted by Bralower et al. (1997) and might be linked to the weathering of the Ontong-Java Plateau, as suggested by

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Larson and Erba (1999), superimposed on the long-term decrease of global weathering. Equally

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noteworthy is the sharp turnaround of the marine 87Sr/86Sr trend in the latest Aptian, followed by very rapid rise until the middle Albian (rate of ca. 0,000055 units per Myr). For comparison, the

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rate of change during the late Berriasian – early Barremian is less than half of this value (ca.

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0,000021 units per Myr). Potential explanation might point at an underestimation of the duration of the early Albian by Gradstein et al. (2012) or a shorter residence time of strontium in seawater

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during the late Early Cretaceous, linked for instance to a lowering of the concentration of strontium in seawater (for instance due to enhanced burial flux of Sr) or to a significantly

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increase of the global river discharge. Firmly constraining the Albian time scale is however necessary before further inference about marine chemistry can be made.

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4.4. A 200 Ma record of global temperature changes Combining the results presented here with δ18O from benthic foraminifera (Zachos et al., 2001; Cramer et al., 2009; Friedrich et al., 2012; and references therein), Jurassic δ18Obel data (Dera et al., 2011; and references therein), and Campanian δ18Obel data (Niebuhr & Joachimski, 2002) yields a 200 Myr compilation of δ18O change (Fig. 7). Despite the differences between the taxonomic groups of foraminifera and belemnites in terms of calcification and ecology, there is a very good match between the two datasets. The overlap is nearly perfect in the Campanian, whereas Albian δ18Obel data plot on the negative end of the benthic foraminifera δ18O dataset established by Friedrich et al. (2012). This shows that belemnite rostra are likely capturing a deep-water δ18O signal. This could in part be attributed to the fact the belemnite had a nekto-

20

ACCEPTED MANUSCRIPT benthic lifestyle (e.g., Bodin et al., 2009), and/or to post-mortem early diagenetic processes in belemnite rostra unnoticed so far (see for instance Sørensen et al., 2015).

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Placing the Early Cretaceous data recorded here in a broader context underlines the similarity between the δ18Obel of the late Valanginian, the late Aptian and the latest Cretaceous

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cool episodes. It highlights moreover the similarities of these positive δ18O shifts and the one

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observed for the earliest Miocene, when partial or ephemeral ice-sheets developed on Antarctica

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(Zachos et al., 2001). This reinforces the hypothesis that transient glaciations have occurred during specific parts of the Cretaceous.

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The δ18Obel spread is larger for the Jurassic than for the Cretaceous dataset. This is perhaps due to the fact that the compilation of Dera et al. (2011) includes belemnites from several basins

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around the western Tethys and the Boreal Realm, which probably introduce biases in δ18O signal (see also Ullmann et al., 2014). As the connection between the Tethys Ocean and the Boreal

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Realm was only intermittent during the Jurassic (Dera et al., 2009), mixing of deep-water masses is therefore uncertain. Nonetheless, the late Pliensbachian, the late middle Toarcian and the middle Jurassic coldhouse episodes (Price, 1999; Korte and Hesselbo, 2011; Suan et al., 2010; Dera et al., 2011; Krencker et al., 2014) are confirmed by this compilation and compare to the δ18O values of the Early Neogene. Due to unconstrained biofractionation between seawater and belemnite rostra calcite, as well as the potential bias in the Jurassic belemnites dataset, great care should however be employed to not overestimate the meaning of this comparison. 5. Conclusions The Early Cretaceous greenhouse is punctuated by three episodes of cool climatic conditions that have likely caused intermittent polar glaciations. These brief coldhouse states occurred 21

ACCEPTED MANUSCRIPT during the late Valanginian-earliest Hauterivian, the late early Aptian and the late Aptian. Each of these episodes was likely triggered by enhanced organic-carbon burial on a global scale, as

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reflected by coeval short-term positive δ13C excursions in belemnite rostra, micrite, and organic carbon.

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The emplacement of LIPs during the early Aptian (Ontong-Java) and the early – middle

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Albian (Nauru-Mariana-South Kerguelen) is associated with global warming episodes. Although

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the emplacement of the Ontong-Java Plateau is responsible for the switch of Earth’s climatic state into a hothouse phase, this is however not the case for other LIP events. The Paraná-

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Etendeka is coeval to a cooling episode, whereas the Nauru-Mariana-South Kerguelen is likely responsible for the end of late Aptian coldhouse phases and the restoration of the normal

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greenhouse state. There is a general correlation between the size of the LIP and the amplitude of the associated climatic perturbation, which can ultimately be linked to the amount of

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volcanogenic-greenhouse gases emitted into the atmosphere. The Early Cretaceous secular trend in seawater

87

Sr/86Sr ratio is best explained by a

dominance of long-term global temperature change and its mechanistic influence on continental runoff and weathering rates. A first-order Early Cretaceous warming peak during the Barremian – earliest Aptian is mirrored by the highest Sr-isotope value that we link to long-term peak continental weathering. On the other hand, the late Aptian cooling corresponds to low

87

Sr/86Sr

values that we interpret as being primarily driven by long-term decreased continental weathering. Enhanced oceanic hydrothermal fluxes have only played a secondary role in shaping the marine Early Cretaceous 87Sr/86Sr curve.

22

ACCEPTED MANUSCRIPT 6. Acknowledgments Laurenz Fähnrich is thanked for the belemnite preparation. The assistance of John McArthur

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regarding strontium isotope analyses at RHUL, as well as numerous fruitful discussions and

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comments on a draft version of this paper is greatly acknowledged. This investigation was supported by the German Research Foundation (DFG; project MU 667/40-1). We are grateful to

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Mark Leckie and an anonymous reviewer for their constructive comments on this manuscript.

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7. References

MA

Allègre, C.J., Louvat, P., Gaillardet, J., Meynadier, L., Rad, S., Capmas, F., 2010. The fundamental role of island arc weathering in the oceanic Sr isotope budget. Earth and

D

Planetary Science Letters 292, 51-56.

TE

Alley, N.F., Frakes, L.A., 2003. First known Cretaceous glaciation: Livingston Tillite Member of

144.

AC CE P

the Cadna-owie Formation, South Australia. Australian Journal of Earth Sciences 50, 139-

Barclay, R.S., McElwain, J.C., Sageman, B.B., 2010. Carbon sequestration activated by a volcanic CO2 pulse during Ocean Anoxic Event 2. Nature Geoscience 3, 205-208. Berner, R.A., Lasaga, A.C., Garrels, R.M., 1983. The carbonate-silicate geochemical cycle and its effect on atmospheric carbon dioxide over the past 100 million years. American Journal of Science 283, 641-683. Blättler, C.L., Jenkyns, H.C., Reynard, L.M., Henderson, G.M., 2011. Significant increases in global weathering during Oceanic Anoxic Events 1a and 2 indicated by calcium isotopes. Earth and Planetary Science Letters 309, 77-88.

23

ACCEPTED MANUSCRIPT Bodin, S., Fiet, N., Godet, A., Matera, V., Westermann, S., Clément, A., Janssen, N.M.M., Stille, P., Föllmi, K.B., 2009. Early Cretaceous (latest Berriasian to earliest Aptian)

PT

palaeoceanographic change along the northwestern Tethyan margin (Vocontian trough, SE

RI

France): δ13C, δ18O and Sr-isotope belemnite and whole-rock records. Cretaceous Research 30, 1247-1262.

SC

Bodin, S., Godet, A., Westermann, S., Föllmi, K.B., 2013. Secular change in northwestern

Planetary Science Letters 374, 121-131.

NU

Tethyan water-mass oxygenation during the late Hauterivian-early Aptian. Earth and

MA

Bottini, C., Cohen, A.S., Erba, E., Jenkyns, H.C., Coe, A.L., 2012. Osmium-isotope evidence for volcanism, weathering, and ocean mixing during the early Aptian OAE 1a. Geology 40,

TE

D

583-586.

Bottini, C., Erba, E., Tiraboschi, D., Jenkyns, H.C., Schouten, S., Sinninghe Damsté, J.S., 2015.

402.

AC CE P

Climate variability and ocean fertility during the Aptian Stage. Climate of the Past 11, 383-

Bover-Arnal, T., Salas, R., Guimerà, J., Moreno-Bedmar, J.A., 2014. Deep incision in an Aptian carbonate succession indicates major sea-level fall in the Cretaceous. Sedimentology 61, 1558-1593.

Bover-Arnal, T., Salas, R., Moreno-Bedmar, J.A., Bitzer, K., 2009. Sequence stratigraphy and architecture of a late Early–Middle Aptian carbonate platform succession from the western Maestrat Basin (Iberian Chain, Spain). Sedimentary Geology 219, 280-301. Bralower, T.J., Fullagar, P.D., Paull, C.K., Dwyer, G.S., Leckie, R.M., 1997. Mid-Cretaceous strontium-isotope stratigraphy of deep-sea sections. Geological Society of America Bulletin 109, 1421–1442. 24

ACCEPTED MANUSCRIPT Bralower, T.J., CoBabe, E., Clement, B., Sliter, W.V., Osburn, C.L., Longoria, J., 1999. The record of global change in mid-Cretaceous (Barremian-Albian) sections from the Sierra

PT

Madre, northeastern Mexico. Journal of Foraminiferal Research 29, 418-137.

RI

Bréhéret, J.-G., 1997. L'Aptien et l'Albien de la fosse vocontienne (des bordures au bassin). Evolution de la sédimentation et enseignements sur les événements anoxiques. 614 pp.

SC

Bryan, S.E., Ferrari, L., 2013. Large igneous provinces and silicic large igneous provinces:

NU

Progress in our understanding over the last 25 years. Geological Society of America Bulletin 125, 1053-1078.

MA

Coffin, M.F., Pringle, M.S., Duncan, R.A., Gladczenko, T.P., Storey, M., Müller, R.D., Gahagan, L.A., 2002. Kerguelen Hotspot Magma Output since 130 Ma. Journal of Petrology 43, 1121-

TE

D

1137.

Cramer, B.S., Toggweiler, J.R., Wright, J.D., Katz, M.E., Miller, K.G., 2009. Ocean overturning

AC CE P

since the Late Cretaceous: Inferences from a new benthic foraminiferal isotope compilation. Paleoceanography 24, PA4216. Delanoy, G., 1998. Biostratigraphie des faunes d'ammonites à la limite Barrémien-Aptien dans la région d'Angles-Barrême-Castellane. Etude particulière de la famille des Heteroceratina Spath, 1922 (Ancyloceratina, Ammonoidea). Annales du Muséum d'Histoire Naturelle de Nice (Nice) tome XII, 1-270. Dera, G., Brigaud, B., Monna, F., Laffont, R., Pucéat, E., Deconinck, J.-F., Pellenard, P., Joachimski, M., Durlet, C., 2011. Climatic ups and downs in a disturbed Jurassic world. Geology 39, 215-218. Dera, G., Pucéat, E., Pellenard, P., Neige, P., Delsate, D., Joachimski, M.M., Reisberg, L., Martinez, M., 2009. Water mass exchange and variations in seawater temperature in the NW 25

ACCEPTED MANUSCRIPT Tethys during the Early Jurassic: Evidence from neodymium and oxygen isotopes of fish teeth and belemnites. Earth and Planetary Science Letters 286, 198-207.

PT

Dercourt, J., Ricou, L.E., Vrielynck, B., (Eds), Atlas, Tethys, Palaeoenvironmental Maps,

RI

Gauthier-Villars, Paris, 1993, 307 pp.

Dodd, S.C., Mac Niocaill, C., Muxworthy, A.R., 2015. Long duration (>4 Ma) and steady-state

SC

volcanic activity in the early Cretaceous Paraná-Etendeka Large Igneous Province: New

NU

palaeomagnetic data from Namibia. Earth and Planetary Science Letters 414, 16-29. Donnadieu, Y., Dromart, G., Godderis, Y., Pucéat, E., Brigaud, B., Dera, G., Dumas, C., Olivier,

MA

N., 2011. A mechanism for brief glacial episodes in the Mesozoic greenhouse. Paleoceanography 26, PA3212.

TE

D

Duncan, R.A., 2002. A Time Frame for Construction of the Kerguelen Plateau and Broken Ridge. Journal of Petrology 43, 1109-1119.

AC CE P

Eldhom, O., Coffin, M.F., 2000. Large igneous provinces and plate tectonics, in: Richards, M.A., Gordon, R.G., Van der Hilst, D., (Eds.), The history and dynamics of global plate motions, pp. 309-326.

Eldrett, J.S., Harding, I.C., Wilson, P.A., Butler, E., Roberts, A.P., 2007. Continental ice in Greenland during the Eocene and Oligocene. Nature 446, 176-179. Erba, E., Bartolini, A., Larson, R.L., 2004. Valanginian Weissert oceanic anoxic event. Geology 32, 149-152. Erba, E., Duncan, R.A., Bottini, C., Tiraboschi, D., Weissert, H., Jenkyns, H.C., Malinverno, A., 2015. Environmental consequences of Ontong Java Plateau and Kerguelen Plateau volcanism. Geological Society of America Special Papers 511, 271-303.

26

ACCEPTED MANUSCRIPT Föllmi, K.B., Godet, A., Bodin, S., Linder, P., 2006. Interactions between environmental change and shallow-water carbonate build-up along the northern Tethyan margin and their impact

PT

on the early Cretaceous carbon-isotope record. Paleoceanography 21, PA4211.

RI

Forster, A., Schouten, S., Moriya, K., Wilson, P.A., Sinninghe Damste, J.S., 2007. Tropical warming and intermittent cooling during the Cenomanian/Turonian oceanic anoxic event 2:

SC

Sea surface temperature records from the equatorial Atlantic. Paleoceanography 22,

NU

PA1219.

Frakes, L.A., Alley, N.F., Deynoux, M., 1995. Early Cretaceous ice rafting and climate zonation

MA

in Australia. International Geology Review 37, 567-583. Frey, F.A., Coffin, M.F., Wallace, P.J., Weis, D., 2003. Leg 183 synthesis: Kerguelen Plateau–

TE

D

Broken Ridge — a large igneous province, in: Frey, F.A., Coffin, M.F., Wallace, P.J., Quilty, P.G., (Eds.), Proceedings of the Ocean Drilling Program, Scientific Results 183, pp.

AC CE P

1-48.

Friedrich, O., Norris, R.D., Erbacher, J., 2012. Evolution of middle to Late Cretaceous oceans -A 55 m.y. record of Earth's temperature and carbon cycle. Geology 40, 107-110. Gale, A.S., Bown, P., Caron, M., Crampton, J., Crowhurst, S.J., Kennedy, W.J., Petrizzo, M.R., Wray, D.S., 2011. The uppermost Middle and Upper Albian succession at the Col de Palluel, Hautes-Alpes, France: An integrated study (ammonites, inoceramid bivalves, planktonic foraminifera, nannofossils, geochemistry, stable oxygen and carbon isotopes, cyclostratigraphy). Cretaceous Research 32, 59–130. Godet, A., Bodin, S., Föllmi, K.B., Vermeulen, J., Gardin, S., Fiet, N., Adatte, T., Berner, Z., Stüben, D., Van de Schootbrugge, B., 2006. Evolution of the marine stable carbon-isotope

27

ACCEPTED MANUSCRIPT record during the early Cretaceous: A focus on the late Hauterivian and Barremian in the Tethyan realm. Earth and Planetary Science Letters 242, 254-271.

PT

Godet, A., Bodin, S., Adatte, T., Föllmi, K.B., 2008. Platform-induced clay-mineral fractionation

RI

along a northern Tethyan basin-platform transect: implications for the interpretation of Early Cretaceous climate change (Late Hauterivian-Early Aptian). Cretaceous Research 29, 830-

SC

847.

NU

Gradstein, F.M., Ogg, J.G., Schmitz, M.D., Ogg, G.M., 2012. The Geologic Time Scale 2012. 1144 pp.

MA

Gréselle, B., Pittet, B., 2005. Fringing carbonate platforms at the Arabian Plate margin in northern Oman during the Late Aptian-Middle Albian: Evidence for high.amplitude sea-

TE

D

level changes. Sedimentary Geology 175, 367-390. Gréselle, B., Pittet, B., 2010. Sea-level reconstruction from the Peri-Vocontian Zone (South-east

AC CE P

France) point to Valanginian glacio-eustasy. Sedimentology 57, 1640–1684. Gröcke, D., 1998. Carbon-isotope analyses of fossil plants as a chemostratigraphic and palaeoenvironmental tool. Lethaia 31, 1-13. Halverson, G.P., Dudás, F.Ö., Maloof, A.C., Bowring, S.A., 2007. Evolution of the composition

of

Neoproterozoic

seawater.

Palaeogeography,

87

Sr/86Sr

Palaeoclimatology,

Palaeoecology 256, 103-129. Hammer, Ø., Harper, D.A.T., Ryan, P.D., 2001. PAST: Paleontological statistics software package for education and data analysis. Palaeontologia Electronica 4, 1-9. Haq, B.U., 2014. Cretaceous eustasy revisited. Global and Planetary Change 113, 44-58. Hay, W.W., 1998. Detrital sediment fluxes from continents to oceans. Chemical Geology 145, 287-323. 28

ACCEPTED MANUSCRIPT Hay, W.W., Soeding, E., DeConto, R.M., Wold, C.N., 2002. The Late Cenozoic uplift - climate change paradox. International Journal of Earth Sciences 91, 746-774.

PT

Heimhofer, U., Hochuli, P.A., Herrle, J.O., Andersen, N., Weissert, H., 2004. Absence of major

RI

vegetation and palaeoatmospheric pCO2 changes associated with oceanic anoxic event 1a (Early aptian, SE France). Earth and Planetary Science Letters 223, 303-318.

SC

Herrle, J.O., Kössler, P., Friedrich, O., Erlenkeuser, H., Hemleben, C., 2004. High-resolution

NU

carbon isotope records of the Aptian to Lower Albian from SE France and the Mazagan Plateau (DSDP Site 545): a stratigraphic tool for paleoceanographic and paleobiologic

MA

reconstruction. Earth and Planetary Science Letters 218, 149-161. Hochuli, P.A., Menegatti, A.P., Weissert, H., Riva, A., Erba, E., Premoli-Silva, I., 1999.

657-660.

TE

D

Episodes of high productivity and cooling in the early Aptian Alpine Tethys. Geology 27,

AC CE P

Hollis, C.J., Tayler, M.J.S., Andrew, B., Taylor, K.W., Lurcock, P., Bijl, P.K., Kulhanek, D.K., Crouch, E.M., Nelson, C.S., Pancost, R.D., Huber, M., Wilson, G.S., Ventura, G.T., Crampton, J.S., Schioler, P., Phillips, A., 2014. Organic-rich sedimentation in the South Pacific Ocean associated with Late Paleocene climatic cooling. Earth-Science Reviews 134, 81-97.

Huber, B.T., Norris, R.D., MacLeod, K.G., 2002. Deep-sea paleotemperature record of extreme warmth during the Cretaceous. Geology 30, 123-126. Huck, S., Heimhofer, U., Rameil, N., Bodin, S., Immenhauser, A., 2011. Strontium and carbonisotope chronostratigraphy of Barremian-Aptian shoal-water carbonates: Northern Tethyan platform drowning predates OAE 1a. Earth and Planetary Science Letters 304, 547-558.

29

ACCEPTED MANUSCRIPT Immenhauser, A., Scott, R.W., 2002. An estimate of Albian sea-level amplitudes and its implication for the duration of stratigraphic hiatuses. Sedimentary Geology 152, 19-28.

PT

Janasi, V.d.A., de Freitas, V.A., Heaman, L.H., 2011. The onset of flood basalt volcanism,

RI

Northern Parana Basin, Brazil: A precise U-Pb baddeleyite/zircon age for a Chapeco-type dacite. Earth and Planetary Science Letters 302, 147–153.

SC

Jarvis, I., Lignum, J.S., Gröcke, D.R., Jenkyns, H.C., Pearce, M.A., 2011. Black shale

NU

deposition, atmospheric CO2 drawdown, and cooling during the Cenomanian-Turonian Oceanic Anoxic Event. Paleoceanography 26, PA3201.

MA

Jenkyns, H.C., Forster, A., Schouten, S., Sinninghe Damste, J.S., 2004. High temperatures in the Late Cretaceous Arctic Ocean. Nature 432, 888-892.

TE

D

Joly, B., Delamette, M., 2008. Les Phylloceratoidea (Ammonoidea) aptiens et albiens du bassin vocontien (Sud-Est de la France). Notebooks on Geology CG2008_M04, 1-60.

AC CE P

Jones, C.E., Jenkyns, H.C., 2001. Seawater strontium isotopes, oceanic anoxic events, and seafloor hydrothermal activity in the Jurassic and Cretaceous. American Journal of Science 301, 112-149.

Kemper, E., 1987. Das klima der Kreide-zeit. Geologisches Jahrbuch, Reihe A 96, 5-185. Kennedy, W.J., Gale, A.S., Bown, P.R., Caron, M., Davey, R.J., Gröcke, D., Wray, D.S., 2000. Integrated stratigraphy across the Aptian-Albian boundary in the Marnes Bleues, at the Col de Pré-Guittard, Arnayon (Drôme), and at Tartonne (Alpes-de-Haute-Provence), France: a candidate Global Boundary Stratotype Section and Boundary Point for the base of the Albian Stage. Cretaceous Research 21, 591–720.

30

ACCEPTED MANUSCRIPT Kent, R.W., Pringle, M.S., Müller, R.D., Saunders, A.D., Ghose, N.C., 2002.

40

Ar/39Ar

Geochronology of the Rajmahal Basalts, India, and their Relationship to the Kerguelen

PT

Plateau. Journal of Petrology 43, 1141-1153.

RI

Kidder, D.L., Worsley, T.R., 2010. Phanerozoic Large Igneous Provinces (LIPs), HEATT (Haline Euxinic Acidic Thermal Transgression) episodes, and mass extinctions.

SC

Palaeogeography, Palaeoclimatology, Palaeoecology 295, 162–191.

NU

Korte, C., Hesselbo, S.P., 2011. Shallow marine carbon and oxygen isotope and elemental records indicate icehouse-greenhouse cycles during the Early Jurassic. Paleoceanography

MA

26, PA4219.

Korte, C., Jasper, T., Kozur, H.W., Veizer, J., 2006.

87

Sr/86Sr record of Permian seawater.

TE

D

Palaeogeography, Palaeoclimatology, Palaeoecology 240, 89-107. Krencker, F.-N., Bodin, S., Hoffmann, R., Suan, G., Mattioli, E., Kabiri, L., Föllmi, K.B.,

AC CE P

Immenhauser, A., 2014. The middle Toarcian cold snap: trigger of mass extinction and carbonate factory demise. Global and Planetary Change 117, 64-78. Kuroda, J., Tanimizu, M., Hori, R.S., Suzuki, K., Ogawa, N.O., Tejada, M.L.G., Coffin, M.F., Coccioni, R., Erba, E., Ohkouchi, N., 2011. Lead isotopic record of Barremian-Aptian marine sediments: Implications for large igneous provinces and the Aptian climatic crisis. Earth and Planetary Science Letters 307, 126-134. Larson, R.L., 1991. Geological consequences of superplumes. Geology 19, 963-966. Larson, R.L., Erba, E., 1999. Onset of the mid-Cretaceous greenhouse in the Barremian-Aptian : Igneous

events

and

the

biological,

sedimentary

Paleoceanography 14, 663-678.

31

and

geochemical

responses.

ACCEPTED MANUSCRIPT Lini, A., Weissert, H., Erba, E., 1992. The Valanginian carbon isotope event: a first episode of greenhouse climate conditions during the Cretaceous. Terra Nova 4, 374-384.

PT

Linnert, C., Robinson, S.A., Lees, J.A., Bown, P.R., Pérez-Rodríguez, I., Petrizzo, M.R., Falzoni,

RI

F., Littler, K., Arz, J.A., Russell, E.E., 2014. Evidence for global cooling in the Late Cretaceous. Nature Communications 5, 4194.

NU

geologic carbon cycle. Science 343, 1502-1504.

SC

Maher, K., Chamberlain, C.P., 2014. Hydrologic regulation of chemical weathering and the

Markwick, P.J., Rowley, D.B., 1998. The geological evidence for Triassic to Pleistocene

MA

glaciations: Implications for eustasy, in: Pindell, J., Drake, C.L., (Eds.), Paleogeographic Evolution and Non-Glacial Eustasy, Northern South America, SEPM Special Publication 58,

TE

D

pp. 17-43.

Martinez, M., Deconinck, J.-F., Pellenard, P., Reboulet, S., Riquier, L., 2013. Astrochronology

AC CE P

of the Valanginian Stage from reference sections (Vocontian Basin, France) and palaeoenvironmental

implications

for

the

Weissert

Event.

Palaeogeography,

Palaeoclimatology, Palaeoecology 376, 91-102. Martinez, M., Deconinck, J.-F., Pellenard, P., Riquier, L., Company, M., Reboulet, S., Moiroud, M., 2015. Astrochronology of the Valanginian-Hauterivian stages (Early Cretaceous): Chronological relationships between the Paraná-Etendeka large igneous province and the Weissert and the Faraoni events. Global and Planetary Change 131, 158-173. Masse, J.-P., 1993. Valanginian-Early Aptian Carbonate Platforms from Provence, Southeastern France, in: Simo J.A.T., Scott R.W., Masse J.-P., (Eds.), Cretaceous carbonates platforms, AAPG Memoir 56, American Association of Petroleum Geologists. Tulsa, OK, United States., pp. 363-374. 32

ACCEPTED MANUSCRIPT Maurer, F., van Buchem, F.S.P., Eberli, G.P., Pierson, B.J., Raven, M.J., Larsen, P.-H., AlHusseini, M.I., Vincent, B., 2013. Late Aptian long-lived glacio-eustatic lowstand recorded

PT

on the Arabian Plate. Terra Nova 25, 87-94.

RI

McAnena, A., Flögel, S., Hofmann, P., Herrle, J.O., Griesand, A., Pross, J., Talbot, H.M., Rethemeyer, J., Wallmann, K., Wagner, T., 2013. Atlantic cooling associated with a marine

SC

biotic crisis during the mid-Cretaceous period. Nature Geoscience 6, 558-561.

NU

McArthur, J.M., 1994. Recent trends in strontium isotope stratigraphy. Terra Nova 6, 331–358. McArthur, J.M., Doyle, P., Leng, M.J., Reeves, K., Williams, C.T., Garcia-Sanchez, R.,

MA

Howarth, R.J., 2007. Testing palaeo-environmental proxies in Jurassic belemnites: Mg/Ca, Sr/Ca, Na/Ca, δ18O and δ13C. Palaeogeography, Palaeoclimatology, Palaeoecology 252, 464-

TE

D

480.

McArthur, J.M., Howarth, R.J., Bailey, T.R., 2001. Strontium isotope stratigraphy: LOWESS

AC CE P

version 3: best fit to the marine Sr-isotope curve for 0-509 Ma and accompanying look-up table for deriving numerical age. The Journal of Geology 109, 155–170. McArthur, J.M., Janssen, N.M.M., Reboulet, S., Leng, M.J., Thirlwall, M.F., Van de Schootbrugge, B., 2007. Palaeo-temperatures, polar ice-volume, and isotope stratigraphy (Mg/Ca, δ18O, δ13C, 87Sr/86Sr): the Early Cretaceous (Berriasian, Valanginian, Hauterivian). Palaeogeography, Palaeoclimatology, Palaeoecology 248, 391-430. McArthur, J.M., Mutterlose, J., Price, G.D., Rawson, P.F., Ruffell, A., Thirlwall, M.F., 2004. Belemnites of Valanginian, Hauterivian and Barremian age: Sr-isotope stratigraphy, composition

(87Sr/86Sr,

δ13C,

δ18O,

Na,

Sr,

Mg),

and

Palaeogeography, Palaeoclimatology, Palaeoecology 202, 253-272.

33

palaeo-oceanography.

ACCEPTED MANUSCRIPT Méhay, S., Keller, C.E., Bernasconi, S.M., Weissert, H., Erba, E., Bottini, C., Hochuli, P.A., 2009. A volcanic CO2 pulse triggered the Cretaceous Oceanic Anoxic Event 1a and a

PT

biocalcification crisis. Geology 37, 819–822. Menegatti, A.P., Weissert, H., Brown, R.S., Tyson, R.V., Farrimond, P., Strasser, A., Caron, M.,

SC

Alpine Tethys. Paleoceanography 13, 530-545.

RI

1998. High-resolution δ13C stratigraphy through the early Aptian "Livello Selli" of the

NU

Miller, K.G., Wright, J.D., Browning, J.V., 2005. Visions of ice sheets in a greenhouse world. Marine Geology 217, 215-231.

MA

Mutterlose, J., Bodin, S., Fähnrich, L., 2014. Strontium-isotope stratigraphy of the Early Cretaceous (Valanginian-Barremian): Implications for Boreal-Tethys correlation and

TE

D

paleoclimate. Cretaceous Research 50, 252-263. Mutterlose, J., Bornemann, A., Herrle, J., 2009. The Aptian - Albian cold snap: Evidence for

AC CE P

"mid" Cretaceous icehouse interludes. N. Jb. Geol. Päläont. Abh. 252, 217-225. Mutterlose, J., Bottini, C., Schouten, S., Sinninghe Damsté, J.S., 2014. High sea-surface temperatures during the early Aptian Oceanic Anoxic Event 1a in the Boreal Realm. Geology 42, 439-442.

Mutterlose, J., Malkoč, M., Schouten, S., Sinninghe Damsté, J.S., Forster, A., 2010. TEX86 and stable δ18O paleothermometry of early Cretaceous sediments: Implications for belemnite ecology and paleotemperature proxy application. Earth and Planetary Science Letters 298, 286–298. Neal, C.R., Mahoney, J.J., Kroenke, L.W., Duncan, R.A., Petterson, M.G., 1997. The Ontong Java Plateau, in: Mahoney, J.J., Coffin, M.F., (Eds.), Large Igneous Provinces: Continental, Oceanic, and Planetary Flood Volcanism, American Geophysical Union, pp. 183-216. 34

ACCEPTED MANUSCRIPT Niebuhr, B., Joachimski, M.M., 2002. Stable isotope and trace element geochemistry of Upper Cretaceous carbonates and belemnite rostra (Middle Campanian, north Germany). Geobios

PT

35, 51-64.

RI

Petrizzo, M.R., Huber, B.T., Gale, A.S., Barchetta, A., Jenkyns, H.C., 2012. Abrupt planktic foraminiferal turnover across the Niveau Kilian at Col de Pré-Guittard (Vocontian Basin,

SC

southeast France): new criteria for defining the Aptian/Albian boundary. Newsletter on

NU

Stratigraphy 45, 55-74.

Podlaha, O.G., Mutterlose, J., Veizer, J., 1998. Preservation of δ18O and δ13C in belemnite rostra

MA

from the Jurassic/Early Cretaceous successions. American Journal of Science 298, 324-347. Pogge von Strandmann, P.A.E., Jenkyns, H.C., Woodfine, R.G., 2013. Lithium isotope evidence

TE

D

for enhanced weathering during Oceanic Anoxic Event 2. Nature Geoscience 6, 668-672. Price, G.D., 1999. The evidence and implications of polar ice during the Mesozoic. Earth-

AC CE P

Science Reviews 48, 183-210.

Price, G.D., Mutterlose, J., 2004. Isotopic signals from late Jurassic-early Cretaceous (VolgianValanginian) sub-Arctic belemnites, Yatria River, Western Siberia. Journal of Geological Society of London 161, 959-968. Price, G.D., Passey, B.H., 2013. Dynamic polar climates in a greenhouse world: Evidence from clumped isotope thermometry of Early Cretaceous belemnites. Geology 41, 923-926. Prokoph, A., Shields, G.A., Veizer, J., 2008. Compilation and time-series analysis of a marine carbonate δ18O, δ13C,

87

Sr/86Sr and δ34S database through Earth history. Earth-Science

Reviews 87, 113-133.

35

ACCEPTED MANUSCRIPT Pucéat, E., Lécuyer, C., Sheppard, S.M.F., Dromart, G., Reboulet, S., Grandjean, P., 2003. Thermal evolution of Cretaceous Tethyan marine waters inferred from oxygen isotope

PT

composition of fish tooth enamels. Paleoceanography 18, PA1029. Rameil, N., Immenhauser, A., Csoma, A.É., Warrlich, G.M.D., 2012. Surfaces with a long

RI

history: the Aptian top Shu’aiba Formation unconformity, Sultanate of Oman.

SC

Sedimentology 59, 212-248.

NU

Reichelt, K., Late Aptian-Albian of the Vocontian Basin (SE-France) and Albian of NE-Texas: Biostratigraphic and paleoceanographic implications by planktic foraminifera faunas, PhD,

MA

Geowissenschaftlichen Fakultät, Eberhard-Karls-Universität Tübingen, 2005. Sørensen, A.M., Ullmann, C.V., Thibault, N., Korte, C., 2015. Geochemical signatures of the

TE

D

early Campanian belemnite Belemnellocamax mammillatus from the Kristianstad Basin in Scania, Sweden. Palaeogeography, Palaeoclimatology, Palaeoecology 433, 191-200.

AC CE P

Suan, G., Mattioli, E., Pittet, B., Lécuyer, C., Suchéras-Marx, B., Duarte, L.V., Philippe, M., Reggiani, L., Martineau, F., 2010. Secular environmental precursors to Early Toarcian (Jurassic) extreme climate changes. Earth and Planetary Science Letters 290, 448–458. Teichert, B.M.A., Luppold, F.W., 2013. Glendonites from an Early Jurassic methane seep -Climate or methane indicators? Palaeogeography, Palaeoclimatology, Palaeoecology 390, 81-93. Tejada, M.L.G., Suzuki, K., Kuroda, J., Coccioni, R., Mahoney, J.J., Ohkouchi, N., Sakamoto, T., Tatsumi, Y., 2009. Ontong Java Plateau eruption as a trigger for the early Aptian oceanic anoxic event. Geology 37, 855-858. Theiling, B.P., Elrick, M., Asmerom, Y., 2012. Increased continental weathering flux during orbital-scale sea-level highstands: Evidence from Nd and O isotope trends in Middle 36

ACCEPTED MANUSCRIPT Pennsylvanian cyclic carbonates. Palaeogeography, Palaeoclimatology, Palaeoecology 342343, 17-26.

PT

Thiede, D.S., Vasconcelos, P.M., 2010. Parana flood basalts: Rapid extrusion hypothesis

RI

confirmed by new 40Ar/39Ar results. Geology 38, 747–750.

Ullmann, C.V., Thibault, N., Ruhl, M., Hesselbo, S.P., Korte, C., 2014. Effect of a Jurassic

SC

oceanic anoxic event on belemnite ecology and evolution. Proceedings of the National

NU

Academy of Sciences 111, 10073-10076.

van de Schootbrugge, B., 2001. Influence of paleo-environmental changes during the

MA

Hauterivian (Early Cretaceous) on carbonate deposition along the northern margin of the Tethys: Evidence from geochimical records (C, O, and Sr-isotopes, P, Fe, Mn), Thèse de

Switzerland.

TE

D

Doctorat ès Sciences, spécialité Géologie, Institut de Géologie, Université de Neuchâtel,

AC CE P

van de Schootbrugge, B., Föllmi, K.B., Bulot, L.G., Burns, S.J., 2000. Paleoceanographic changes during the early Cretaceous (Valanginian-Hauterivian): evidence from oxygen and carbon stable isotopes. Earth and Planetary Science Letters 181, 15-31. Veizer, J., 1989. Strontium isotopes in seawater through time. Annual Review of Earth and Planetary Sciences 17, 141-167. Vermeulen, J., 2002. Etude stratigraphique et paléontologique de la famille des Pulchelliidae (ammonoidea, Ammonitina, Endemocerataceae). Grenoble, France, 333 pp. Weissert, H., 1990. Siliciclastics in the Early Cretaceous Tethys and North Atlantic oceans: Documents of periodic greenhouse climate conditions. Mem. Soc. Geol. It. 44, 59–69.

37

ACCEPTED MANUSCRIPT Weissert, H., Lini, A., 1991. Ice age interludes during the time of Cretaceous greenhouse climate, in: Müller, D.W., McKenzie, J.A., Weissert, H., (Eds.), Controversies in modern

PT

geology, Academic Press, London, pp. 173-191.

RI

Weissert, H., Erba, E., 2004. Volcanism, CO2 and palaeoclimate; a Late Jurassic-Early Cretaceous carbon and oxygen isotope record. Journal of the Geological Society of London

SC

161, 695-702.

NU

Westermann, S., Föllmi, K.B., Adatte, T., Matera, V., Schnyder, J., Fleitmann, D., Fiet, N., Ploch, I., Duchamp-Alphonse, S., 2010. The Valanginian δ13C excursion may not be an

MA

expression of a global oceanic anoxic event. Earth and Planetary Science Letters 290, 118131.

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Westermann, S., Stein, M., Matera, V., Fiet, N., Fleitmann, D., Adatte, T., Föllmi, K.B., 2013. Rapid changes in the redox conditions of the western Tethys Ocean during the early Aptian

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oceanic anoxic event. Geochimica et Cosmochimica Acta 121, 467-486. Zachos, J.C., Pagani, M., Sloan, L., Thomas, E., Billups, K., 2001. Trends, rhythms, and aberrations in global climate 65 Ma to Present. Science 292, 686-693.

Figure captions: Fig. 1: (A) Map of France showing the present-day location of the Vocontian Basin in southeast France. (B) Early Aptian palaeogeographic map of western Tethys (redrawn from Masse et al., 1993) showing the original location of the Vocontian Basin in the northwestern corner of the Tethys Ocean. (C) Outline of the southeastern France deep-water domain (Pre-Vocontian and

38

ACCEPTED MANUSCRIPT Vocontian Basin) and surrounding shallow-water areas during the Early Cretaceous. The location

PT

of the Barremian – Albian studied sections is marked with a star.

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Fig. 2: Composite lithostratigraphic section of the Aptian – upper Albian p.p. ―Marnes Bleues‖ Fm (Vocontian Basin, SE France) with key marker beds (modified from Joly and Delamette,

SC

2008). The interval covered by each sections studied here is indicated. Due to variable

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sedimentation rate within the Vocontian Basin, no scale is given.

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Fig. 3: Evolution of Early Cretaceous δ18Obel, δ13Cbel and marine 87Sr/86Sr ratio as recorded in the Vocontian Basin (data from this study, complemented with data from Kennedy et al., 2000; van

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de Schootbrugge et al., 2000; van de Schootbrugge, 2001; McArthur et al., 2007b; Bodin et al., 2009) plotted against the timescale of Gradstein et al. (2012). Periods of suspected glacio-eustasy

AC CE P

after Bover-Arnal et al. (2009, 2014), Gréselle and Pittet (2005, 2010) and Maurer et al. (2013). Anchoring of large igneous provinces activity against the Early Cretaceous chronostratigraphy follows the conclusions of Martinez et al. (2015) for the Paraná-Etendeka LIP and the Os and Pb isotopes fingerprints of Ontong-Java LIP activity coeval to the unfolding of OAE 1a (Tejada et al., 2009; Kuroda et al., 2011; Bottini et al., 2012). Radio-isotopic age of the Rajmahal Basalt after Kent et al. (2002), of the Nauru-Mariana LIP after Eldhom and Coffin (2000), and of the three ―episodes‖ of South Kerguelen LIP activity (a – c) after Coffin et al. (2002), Duncan (2002) and Frey et al. (2003). Relative oceanic-crust production after Larson (1991). Grey dots picture δ18Obel values that are suspected to be strongly influenced by anomalous seawater δ18O values in the Vocontian Basin (see text for discussion). The trend lines (red curve) and its 95%

39

ACCEPTED MANUSCRIPT confidence intervals (dashed blue lines) are calculated using a LOWESS smoothing (α = 0.1)

PT

with the PAST software package (Hammer et al., 2001).

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Fig. 4: Comparison of Vocontian Basin carbon and oxygen isotope trends with the western Tethyan (Italy) and Pacific Ocean temperature index (Bottini et al., 2015), and the North Atlantic

SC

record (δ13Ccarb, δ13Corg and sea surface temperature [SST] derived from TEX86 data after

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McAnena et al., 2013). Compilation of bulk carbonate δ13Ccarb data in the Vocontian Basin after data from Herrle et al. (2004), Reichelt (2005), Godet et al. (2006), Bodin et al. (2009) and

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Westermann et al. (2013). Similar paleotemperature and carbon isotope trends can be observed

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within these different localities during the latest Barremian – middle Albian.

Fig. 5: Evolution of Early Cretaceous marine

87

Sr/86Sr ratio (as recorded by belemnite rostrum

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from the Vocontian Basin) plotted within the chronologic framework based on Tethyan ammonite biostratigraphy and Vocontian Basin lithostratigraphy (see also Fig. 2).

Fig. 6: Lower Aptian of the Angles - Combe Lambert - Glaise composite section showing the position of belemnite strontium isotope data and the Goguel level. Bulk carbonate and organic matter δ13C data after Bodin et al. (2009) and Westermann et al. (2013). C2 to C7 indicate the position of the different carbon isotope segments characterizing the early Aptian (Menegatti et al., 1998).

Fig. 7: Early Jurassic to present-day long-term variation of benthic sea-water δ18O signal (as recorded by benthic foraminifera and belemnites). Data after the compilation of Zachos et al. 40

ACCEPTED MANUSCRIPT (2001), Niebuhr and Joachimski (2002), Cramer et al. (2009), Dera et al. (2011), Friedrich et al. (2012) and this study. Potential occurrences of Mesozoic ice-sheet and their qualitative

PT

representation of ice volume are represented as vertical pink and yellow bars. Cenozoic ice-sheet

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occurrences after Zachos et al. (2001), Eldrett et al. (2007) and Hollis et al. (2014).

JAS 330

Middle Albian

JAS 352

JAS 354

Middle Albian Middle Albian

JAS 356

Middle Albian

JAS 360

Middle Albian

PAL 145

Middle Albian

PAL 135 PAL 119

Middle Albian Middle

87/8 6 Sr

MA

JAS 324

Middle Albian

lautus

lautus

AC CE P

JAS 316

Middle Albian

ammonite zone

D

Stage

TE

Sample

NU

SC

Table. 1: Belemnite isotopic data from Berriasian to middle Albian strata of the Vocontian Basin.

loricatus

loricatus

loricatus

loricatus

loricatus

dentatus

dentatus dentatus

d1 d1 3C 8O

0.70 0.8 0.5 7426 1 9 0.6 1.0 0 9 0.70 1.2 1.1 7430 6 7 0.70 0.9 0.6 7418 6 8 0.70 0.0 0.4 7420 1 9 1.5 1.1 1 8 0.70 0.8 1.0 7407 5 7 0.70 1.5 0.4 7407 1 4 0.5 0.8 9 6 0.70 0.5 41

Age (Grad stein et al. 2012) 107.6 2 107.8 5 108.0 3 108.6 7 108.7 3 108.7 8 108.9 0 109.6 5 109.7 6 109.9

Source

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ACCEPTED MANUSCRIPT 2

mammillat um

0.70 1.2 7408 2

GUI 130

Middle Albian

mammillat um

0.70 0.2 7419 8

Kennedy K10

Lower Albian

0.70 tardefurcat 0.8 7339 a 5

Kennedy K12

Upper Aptian

germanica

0.70 1.0 7327 5

Kennedy K8

Upper Aptian

germanica

0.70 1.3 7343 2

Kennedy K9

Upper Aptian

germanica

0.70 0.8 7311 7

Kennedy K5

Upper Aptian

FER 27-30 FER 27 FER 22 FER 18 FER 17.5 (Kennedy K1) FER 17.5 (Kennedy K2) FER 17.5 (Kennedy K3) FER 17

NU

MA

D TE

germanica

0.70 0.6 7329 9

jacobi

0.70 0.8 7361 8 2.8 2 0.70 1.8 7218 5 0.70 3.0 7173 7 0.70 2.4 7203 0

Upper Aptian

Jacobi

0.70 72

Upper Aptian

Jacobi

Upper Aptian Upper Aptian Upper Aptian Upper Aptian Upper Aptian

AC CE P

Kennedy K6

SC

GUI 135

Middle Albian

Upper Aptian Upper Aptian

germanica jacobi jacobi jacobi

Jacobi

0.9 8 1.2 6 0.7 5 0.0 9 0.4 9 0.2 9 0.2 3 0.6 3 0.9 6 0.1 0 0.3 9 0.2 2 0.4 4 0.1 0

0.70 72

jacobi 42

2.5 2

5 110.6 0

PT

7400

110.7 0

RI

Albian

3.0 0.2 0 9 1.8 0.1 6 2 2.7 0.5 0 7

111.2 5 111.3 0 111.3 0 111.3 0 111.5 1 111.5 1 113.6 6 113.7 4 114.0 0 114.2 1

This study

This study Kennedy et al. (2000) Kennedy et al. (2000) Kennedy et al. (2000) Kennedy et al. (2000) Kennedy et al. (2000) Kennedy et al. (2000) This study This study This study This study

114.2 4

Kennedy et al. (2000)

114.2 4

Kennedy et al. (2000)

114.2 4 114.2 7

Kennedy et al. (2000) This study

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FER 7 FER 2 GAU 234

jacobi jacobi

MA

CHA 121

Upper Aptian

1.4 4 1.8 0

melchioris

0.70 1.1 7235 7

melchioris

0.70 1.0 7244 2

melchioris

1.0 4

melchioris

2.4 5

melchioris

0.70 1.1 7258 2

Nolani Nolani

AC CE P

CHA 137

Nolani

Upper Aptian Upper Aptian

Pey 110

Upper Aptian

CHA 103

Upper Aptian

CHA 100 COM141-144 COM140140b COM139d-e

Upper Aptian Upper Aptian Upper Aptian Upper

0.70 2.0 7211 4 1.8 0

D

CHA 131

Upper Aptian Upper Aptian

Nolani

TE

CHA 148

Pey 115

jacobi

Upper Aptian Upper Aptian

GAU 229

CHA 115

jacobi

melchioris Martini Martini Martini

0.70 1.4 7261 5 2.6 9 1.8 9 0.70 0.8 43

PT

FER 10

jacobi

114.2 9 114.4 8 114.6 3 114.7 9 115.0 5 115.5 1

RI

FER 13

jacobi

0.4 8 0.9 7 0.1 1 0.5 7 0.8 0 0.5 1 0.3 0 0.4 3 0.2 1 0.2 6 0.2 1 0.3 1 0.3 8 2.2 0 0.7 0 0.7 2 0.4 4 0.2 1 0.0

SC

FER 16.6

1.8 6 0.70 3.0 7187 2 1.5 3 0.70 3.0 7191 7 3.6 2 2.4 8

NU

Upper Aptian Upper Aptian Upper Aptian Upper Aptian Upper Aptian Upper Aptian

115.6 2 115.6 4 116.2 6 116.6 0 117.0 9 117.3 6 117.5 1 117.6 8 117.8 9 118.0 2 118.2 9 118.7 0 119.5

This study This study This study This study This study This study

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ACCEPTED MANUSCRIPT

Martini

0.70 2.2 7266 5

CHA 73

Upper Aptian

Martini

0.70 1.5 7305 8

COM139c-d (low)

Upper Aptian

Martini

0.70 1.8 7283 1

COM139b)(c) (low)

Upper Aptian

Martini

COM138a139 (high)

Upper Aptian

Martini

CHA 54 COM137-138 base

Upper Aptian Upper Aptian

CHA 49

Lower Aptian

TE

D

Martini

Furcata

NU

0.70 1.7 7305 9

Furcata

3.5 0

Furcata

0.70 3.4 7340 7

Furcata

3.7 6

AC CE P

Furcata

2.3 7

CLUPN.b

GL +0.5

Lower Aptian

CHA 35

Lower Aptian

GL -0.5

Lower Aptian

CHA 37

0.70 2.4 7290 3 0.70 2.5 7309 1

Furcata

Lower Aptian

CHA 40

0.9 9

0.70 3.5 7331 3 0.70 4.0 7334 5 0.70 2.2 7355 8 0.70 3.1 7322 8

CHA 37-1

CHA 44

1.5 4

MA

Martini

Furcata Furcata Furcata

8 0.4 8 0.6 2 0.1 5 0.2 9 0.2 6 0.3 8 0.1 3 0.0 3 0.0 3 0.1 8 0.0 1 0.1 4 0.7 1 0.2 0 0.0 1 0.3 6

44

2 120.4 5 120.7 4

PT

CHA 76

Upper Aptian

Lower Aptian Lower Aptian Lower Aptian Lower Aptian

9

RI

7275

SC

Aptian

This study

This study

121.0 2

This study

121.8 4

This study

122.2 4

This study

122.5 9 122.7 9 123.0 2 123.2 1 123.3 6 123.4 7 123.4 7 123.5 1 123.5 2 123.5 4 123.5 6

This study This study

This study

This study This study This study This study

This study

This study

This study

This study

ACCEPTED MANUSCRIPT

CHA 23

Lower Aptian

Deshayesi

COM129-a

Lower Aptian

Deshayesi

An 230 top

An 230 base

Forbesi

Forbesi Forbesi

AC CE P

AN 228 Mid

Lower Aptian Lower Aptian

Forbesi

MA

AN 231

Deshayesi

D

Lower Aptian Lower Aptian

Deshayesi

TE

CHA 25

AN 226-227

Lower Aptian

AN 225 top

Lower Aptian

Forbesi

Forbesi

Lower Aptian

Forbesi

AN 209

Lower Aptian Lower Aptian

Oglanlensi s Oglanlensi s

AN 206 mid

Lower Aptian

Oglanlensi s

AN 205 top AN 203a

Lower Aptian Lower

Oglanlensi s Oglanlensi

COM 109b

AN 212

123.9 2

PT

COM130-a

Lower Aptian Lower Aptian

123.7 3

123.9 3

RI

Furcata

SC

CHA 30

NU

Lower Aptian

0.70 3.8 0.0 7344 4 2 0.70 2.7 0.3 7334 1 1 0.70 4.0 0.0 7335 6 0 0.70 3.0 0.8 7340 7 2 0.70 2.8 0.8 7366 5 2 0.70 1.7 0.7 7418 1 2 0.70 7417 0.70 1.9 1.4 7413 2 1 0.70 7425 1.4 0.3 5 4 1.6 0.2 8 7 0.9 0.70 0.7 3 7433 4 1.4 1.9 8 1 0.70 7417 1.6 1.6 5 7 0.70 1.2 0.2 7429 1 5 0.70 45

123.9 9 124.1 3 125.7 8 125.8 0 125.8 1 125.8 3

This study

This study This study

This study

This study

This study This study

This study This study

125.8 5

This study

125.8 6

This study

125.9 7 126.0 2 126.0 6

Bodin et al. (2009)

This study This study

126.1 1

This study

126.1 4 126.1

This study This study

ACCEPTED MANUSCRIPT

Lower Aptian

Oglanlensi s

AN 200 top

Lower Aptian

Oglanlensi s

AN 197 mid

Upper Barremian

Giraudi

AN 194 base

Upper Barremian

Giraudi

AN 192base

Upper Barremian

Giraudi

AN 188 top

Upper Barremian

Giraudi

AN 187.2

Upper Barremian

AN 184-185 SDL 373b

D

TE

AC CE P

AN 185b

Giraudi

Upper Barremian Upper Barremian Upper Barremian

Giraudi

Giraudi

Giraudi

AN 177.1 base

Upper Barremian

Giraudi

SDL 366b

Upper Barremian

Giraudi

AN 175.2176.1 SDL 365

Upper Barremian Upper Barremian

Giraudi Giraudi

126.2 1

PT

AN 203B base

0.70 0.1 0.6 7433 9 7 0.5 1.8 5 2 0.6 2.4 7 7 0.3 0.8 7 9 1.2 2.1 0 9 0.7 0.5 5 5 0.70 0.6 0.9 7424 0 8 0.9 0.5 2 4 1.5 0.70 1.8 2 7425 0 0.4 0.0 9 8 0.70 0.1 0.6 7418 1 5 0.70 1.0 1.0 7440 1 1 0.70 1.2 0.3 7448 4 1 0.70 0.2 1.7 7444 0 4 1.9 7 1.8

126.2 2

RI

Oglanlensi s

8

SC

Lower Aptian

AN 202

7423

NU

s

MA

Aptian

46

Bodin et al. (2009)

This study

126.2 8

This study

126.4 1

This study

126.5 7

This study

126.6 2

This study

126.7 2

This study

126.7 8

This study

126.8 5 126.8 8 126.9 5

Bodin et al. (2009)

This study

Bodin et al. (2009)

127.1 5

This study

127.1 7

Bodin et al. (2009)

127.1 9 127.2 2

This study Bodin et al. (2009)

ACCEPTED MANUSCRIPT

AN 165b

AN 165b

AN 162b

AN 161.3b

AN 161.3b

AN 161.2b

AN 161.1b

AN 160.3b

AN 158b

AN 158

Upper Barremian Upper Barremian Upper Barremian Upper Barremian Upper Barremian

0.7 2

Giraudi G. sartousian a G. sartousian a G. sartousian a G. sartousian a G. sartousian a G. sartousian a G. sartousian a G. sartousian a G. sartousian a

1.6 9

0.70 7460 0.70 7457

Upper Barremian Upper Barremian Upper Barremian Upper Barremian Upper Barremian

H. sayni

Upper Barremian

H. sayni

1.6 6 1.3 2 0.4 4 0.1 7

AC CE P

AN 165b

Giraudi

1.2 4 1.2 3 0.70 7475

0.6 1 0.5 3

0.70 7475

1.0 7 0.4 4

47

127.2 9

PT

1.2 8

127.2 5

127.3 2

RI

AN 172.2b

Upper Barremian

0.70 7457

SC

Upper Barremian

Giraudi

NU

SDL 362b

1.2 9

MA

Upper Barremian

D

AN 173b

1.0 9

Giraudi

TE

AN 174.1-2

Upper Barremian

3 1.0 3 0.5 8 0.2 3 0.0 2 0.4 1 0.5 1 0.6 2 0.3 2 0.5 3 0.2 4 0.2 6 0.7 0 0.5 9 0.6 2 0.2 7

127.3 4 127.7 4 127.7 4 127.7 4 128.1 7 128.2 4 128.2 4 128.3 0 128.3 8 128.4 2 128.6 6 128.6 6

This study

Bodin et al. (2009)

Bodin et al. (2009) Bodin et al. (2009)

Bodin et al. (2009)

Bodin et al. (2009)

Bodin et al. (2009)

Bodin et al. (2009)

Bodin et al. (2009)

Bodin et al. (2009)

Bodin et al. (2009)

Bodin et al. (2009)

Bodin et al. (2009)

Bodin et al. (2009)

Bodin et al. (2009)

ACCEPTED MANUSCRIPT

AN 136b

AN 125b

AN 125

AN 121b

AN 119b

AN 112.7b

AN 112

AN 111.4b

AN 111.1b

AN 110.4b

Lower Barremian

C. darsi

Lower Barremian

C. darsi

Lower Barremian

C. darsi

Lower Barremian Lower Barremian Lower Barremian Lower Barremian

0.70 7496 0.70 7479

C. darsi

K. compressi ssima K. compressi ssima K. compressi ssima

Lower Barremian

N. pulchella

Lower Barremian

N. pulchella

Lower Barremian

N. pulchella

Lower Barremian

N. pulchella

0.70 7483 0.70 7478

0.70 7498

48

128.9 8

PT

H. uhligi

128.8 5

129.2 4

RI

Upper Barremian

0.70 7485

SC

H. uhligi

0.5 0.8 5 5 0.3 0.5 7 4 0.3 0.1 1 9 1.9 2.4 6 1 0.1 0.6 1 0 0.0 0.3 8 1 0.6 0.2 5 6 0.2 0.3 9 4 0.3 0.7 1 1 0.6 2.6 1 8 0.5 0.3 3 5 0.1 1.6 7 4 0.6 0.5 9 2 0.3 1.2 4 8 0.5 0.4 5 0

NU

AN 139.1

Upper Barremian

0.70 7486

MA

AN 143b

H. sayni

D

AN 144b

Upper Barremian

TE

AN 151.3b

H. sayni

AC CE P

AN 155.2b

Upper Barremian

129.2 9 129.4 3 129.4 6 129.5 9 129.6 0 129.6 4 129.6 6 129.7 4 129.7 9 129.8 2 129.8 5 129.8 6

Bodin et al. (2009)

Bodin et al. (2009)

Bodin et al. (2009)

Bodin et al. (2009)

Bodin et al. (2009)

Bodin et al. (2009)

Bodin et al. (2009)

Bodin et al. (2009)

Bodin et al. (2009)

Bodin et al. (2009)

Bodin et al. (2009)

Bodin et al. (2009)

Bodin et al. (2009)

Bodin et al. (2009)

Bodin et al. (2009)

ACCEPTED MANUSCRIPT

AN 94b

AN 92b

AN 89b

AN 88b

AN 87b

AN 85b

AN 84b

AN 80b

AN 79b

AN 78b

Lower Barremian

K. nicklesi

Lower Barremian

K. nicklesi

Lower Barremian

T. hugii

Lower Barremian Lower Barremian

T. hugii

T. hugii

Lower Barremian

T. hugii

Lower Barremian

T. hugii

Lower Barremian

T. hugii

Lower Barremian

T. hugii

Lower Barremian

T. hugii

Lower Barremian

T. hugii

130.0 8

PT

K. nicklesi

129.9 2

130.1 1

RI

Lower Barremian

SC

K. nicklesi

NU

AN 102b

Lower Barremian

0.3 0.7 8 0 0.5 0.7 2 8 0.1 0.5 0 3 0.6 0.70 0.4 0 7500 4 0.4 0.6 6 8 0.7 0.5 0 0 0.4 0.3 3 4 0.1 0.3 8 9 0.5 0.5 0 5 0.0 0.6 2 3 0.4 0.70 0.5 1 7473 1 0.0 0.3 4 3 0.3 0.2 1 9 0.2 0.5 8 0 0.3 0.4 5 4

MA

AN 103b

K. nicklesi

D

AN 103b2

Lower Barremian

TE

AN 104b

N. pulchella

AC CE P

AN 110.1b

Lower Barremian

49

130.1 1 130.1 4 130.3 4 130.4 1 130.5 0 130.5 1 130.5 3 130.5 6 130.5 8 130.6 4 130.6 5 130.6 6

Bodin et al. (2009)

Bodin et al. (2009)

Bodin et al. (2009)

Bodin et al. (2009)

Bodin et al. (2009)

Bodin et al. (2009)

Bodin et al. (2009)

Bodin et al. (2009)

Bodin et al. (2009)

Bodin et al. (2009)

Bodin et al. (2009)

Bodin et al. (2009)

Bodin et al. (2009)

Bodin et al. (2009)

Bodin et al. (2009)

ACCEPTED MANUSCRIPT

AN 73b

AN 71b

VG 197c

B 1a-2 AN 54.2b

AN 54.1b

AN 53.2b

AN 50c

VG 181c AN 43b

Lower Barremian

T. hugii

Lower Barremian

T. hugii

Upper Hauterivia n Upper Hauterivia n Upper Hauterivia n Upper Hauterivia n Upper Hauterivia n Upper Hauterivia n Upper Hauterivia n Upper Hauterivia n Upper Hauterivia n

P. ohmi

Angulicost ata

Ohmi

0.70 7470 0.70 7479 0.70 7458

P. ohmi

0.0 0.0 9 8

P. ohmi

P. ohmi

0.70 7466

0.0 9

Angulicost ata

0.5 6

Angulicost ata

0.70 0.4 7441 9 0.3 2

P. ohmi 50

130.6 9

PT

T. hugii

130.6 9

130.7 0

RI

Lower Barremian

0.70 7495

SC

T. hugii

0.3 0.2 8 2 0.5 0.2 4 3 0.4 0.7 6 5 0.4 0.2 0 1 0.4 0.2 0 8 0.5 0.0 2 4 0.1 0.4 8 8 0.8 0.6 3 3 0.6 0.3 5 0 0.8 0.2 0 3

NU

AN 74b

Lower Barremian

MA

AN 75b

T. hugii

D

AN 76b

Lower Barremian

TE

AN 77b

T. hugii

AC CE P

AN 77.2b

Lower Barremian

0.0 3 0.2 5 1.0 2 0.2 4

130.7 2 130.7 3 130.7 4 130.7 8

Bodin et al. (2009)

Bodin et al. (2009)

Bodin et al. (2009)

Bodin et al. (2009)

Bodin et al. (2009)

Bodin et al. (2009)

130.9 7

Bodin et al. (2009) Van de Schootbrugge et al. (2000)

131.1 7

McArthur et al. (2007b)

131.2 2 131.2 3 131.2 6 131.3 7 131.5 3 131.5 5

Bodin et al. (2009)

Bodin et al. (2009)

Bodin et al. (2009) Van de Schootbrugge et al. (2000) Van de Schootbrugge et al. (2000)

Bodin et al. (2009)

ACCEPTED MANUSCRIPT

AN 18b

AN 11c

AN 9c

AN 8c AN 7b

AN 2b

AN 1b

VG 133c

VG 128c CB J117– J117a

B. balearis

B. balearis

B. balearis

B. balearis

0.70 7442 0.70 7443

B. balearis

B. balearis

Ligatus

Ligatus

0.70 7466 0.70 7436

Ligatus

Ligatus

0.70 7457 51

131.5 5

PT

131.5 8 131.6 4

RI

SC

B. balearis

0.70 7473

0.4 0.2 2 0 0.1 0.1 2 5 0.3 0.5 7 6 0.3 0.1 4 9 0.3 0.3 9 9 0.0 0.0 6 2 0.5 0.2 9 3 0.7 0.2 3 8 0.1 0.4 7 0 0.4 0.4 2 0 0.2 0.4 8 2 0.0 0.2 4 6 0.5 0.1 9 6 0.0 0.4 7 7 0.2 0.1 4 4

NU

AN 22b

B. balearis

MA

AN 34c

B. balearis

D

AN 37b

B. balearis

TE

AN 41b

P. ohmi

AC CE P

AN 43b

Upper Hauterivia n Upper Hauterivia n Upper Hauterivia n Upper Hauterivia n Upper Hauterivia n Upper Hauterivia n Upper Hauterivia n Upper Hauterivia n Upper Hauterivia n Upper Hauterivia n Upper Hauterivia n Upper Hauterivia n Upper Hauterivia n Upper Hauterivia n Upper Hauterivia n

131.6 9 131.9 3 131.9 9 132.1 5 132.1 9 132.2 1 132.2 4 132.3 2 132.3 8

Bodin et al. (2009)

Bodin et al. (2009)

Bodin et al. (2009) Van de Schootbrugge et al. (2000)

Bodin et al. (2009)

Bodin et al. (2009) Van de Schootbrugge et al. (2000) Van de Schootbrugge et al. (2000) Van de Schootbrugge et al. (2000)

Bodin et al. (2009)

Bodin et al. (2009)

132.4 9

Bodin et al. (2009) Van de Schootbrugge et al. (2000) Van de Schootbrugge et al. (2000)

132.5 3

McArthur et al. (2007b)

132.4 7

ACCEPTED MANUSCRIPT

VG 82c CB J106– J107

VG 79c

VG 69c

TM 150c

TM 147c

Sayni

Sayni

Sayni

Sayni

AC CE P

VG 76c

TM 146c

TM 144c

LC 315c

CB J99–J100

Sayni

Nodosopli catum

0.70 0.0 7440 2 0.70 0.0 7451 1 0.70 0.3 7437 8 0.4 1 0.3 0

Nodosopli catum

0.0 0 0.2 3 0.0 1

Nodosopli catum Nodosopli catum Nodosopli catum Nodosopli catum

0.70 0.1 0.0 7419 1 2 0.70 0.1 0.3 7424 5 2 52

132.5 6

PT

132.6 8 132.8 4

RI

0.3 8 0.6 3 0.1 0 0.3 1 0.5 3 0.3 8 0.1 5 0.2 0 0.2 1 0.5 4 0.5 5 1.3 5 0.8 1

SC

Sayni

NU

LC 339c

Sayni

0.70 0.5 7444 9 0.70 0.5 7450 3 0.1 8 0.5 8 0.70 0.3 7436 2

MA

LC 342c

Ligatus

D

VG 99c

Ligatus

TE

VG 117c

Upper Hauterivia n Upper Hauterivia n Upper Hauterivia n Upper Hauterivia n Upper Hauterivia n Upper Hauterivia n Upper Hauterivia n Upper Hauterivia n Upper Hauterivia n Lower Hauterivia n Lower Hauterivia n Lower Hauterivia n Lower Hauterivia n Lower Hauterivia n Lower Hauterivia n

132.8 6 132.8 8 132.8 9

Van de Schootbrugge et al. (2000) Van de Schootbrugge et al. (2000) Van de Schootbrugge et al. (2000) Van de Schootbrugge et al. (2000) Van de Schootbrugge et al. (2000)

133.1 6

McArthur et al. (2007b) Van de Schootbrugge et al. (2000) Van de Schootbrugge et al. (2000) Van de Schootbrugge et al. (2000) Van de Schootbrugge et al. (2000) Van de Schootbrugge et al. (2000) Van de Schootbrugge et al. (2000) Van de Schootbrugge et al. (2000) Van de Schootbrugge et al. (2000)

133.2 2

McArthur et al. (2007b)

132.9 4 133.0 2 133.0 9 133.0 9 133.1 1 133.1 3 133.1 5

ACCEPTED MANUSCRIPT

TM 121c

CL g1/g2

LC 284c

LC 276c

TM 113c

LC 272c

384

LC 258c-1

LC 257c

LC 256c

Loryi

Loryi

Loryi

Loryi

Radiatus

Radiatus

Radiatus

PT 133.3 4 133.3 5 133.3 5

133.4 133.4 7 133.5 1

0.3 0.3 2 6 0.4 0.4 3 7

133.5 6

Loryi

Radiatus

133.3 3

0.70 0.0 0.5 7406 5 9

Loryi

Radiatus

133.3

RI

SC

NU

TM 125c-2

Loryi

0.70 0.3 0.0 7390 3 2 0.3 0.0 0 9 0.2 0.6 2 9 0.4 0.4 1 8 0.70 0.3 0.3 7407 5 7

MA

LC 293c

Nodosopli catum

D

LC 294c

Nodosopli catum

TE

TM 129c

0.7 1.3 8 1 0.4 0.3 1 0

Nodosopli catum

AC CE P

TM 133c

Lower Hauterivia n Lower Hauterivia n Lower Hauterivia n Lower Hauterivia n Lower Hauterivia n Lower Hauterivia n Lower Hauterivia n Lower Hauterivia n Lower Hauterivia n Lower Hauterivia n Lower Hauterivia n Lower Hauterivia n Lower Hauterivia n Lower Hauterivia n Lower Hauterivia n

0.1 0.0 6 9 0.70 0.3 0.5 7386 4 0 0.70 0.1 0.1 7395 4 5 0.9 0.0 7 8 0.0 0.3 5 0 53

133.5 7

133.6 133.7 4 133.8 3 133.8 4 133.8 6

Van de Schootbrugge et al. (2000) Van de Schootbrugge et al. (2000) Van de Schootbrugge et al. (2000) Van de Schootbrugge et al. (2000) Van de Schootbrugge et al. (2000) Van de Schootbrugge et al. (2000) McArthur et al. (2007b) Van de Schootbrugge et al. (2000) Van de Schootbrugge et al. (2000) Van de Schootbrugge et al. (2000) Van de Schootbrugge et al. (2000) McArthur et al. (2007b) Van de Schootbrugge et al. (2000) Van de Schootbrugge et al. (2000) Van de Schootbrugge et al. (2000)

ACCEPTED MANUSCRIPT

166–167

162

160-a

154-a–b

148–149

144–145

138–139 131a1 – 131a2

129–130

Furcillata

0.70 1.4 0.3 7377 2 4

134.3 4

McArthur et al. (2007b)

Furcillata

0.70 0.6 0.0 7375 1 2

134.4 5

McArthur et al. (2007b)

Furcillata

0.70 0.1 0.0 7368 7 1

134.5 3

McArthur et al. (2007b)

0.70 0.3 0.1 7373 9 9 0.70 0.0 0.1 7377 0 0 0.70 0.5 0.1 7372 9 5

134.5 7

McArthur et al. (2007b)

134.9 7

McArthur et al. (2007b)

134.9 9

McArthur et al. (2007b)

0.70 0.5 0.0 7369 3 3 0.70 0.8 0.1 7367 6 2 0.70 0.4 0.3 7368 8 1

135.0 7

McArthur et al. (2007b)

135.1 0

McArthur et al. (2007b)

135.2 0

McArthur et al. (2007b)

135.3 2

McArthur et al. (2007b)

Peregrinu s

0.70 0.6 0.0 7367 5 9 0.70 0.8 0.0 7360 6 4

135.3 9

McArthur et al. (2007b)

Peregrinu s

0.70 0.8 0.0 7368 8 2

135.4 4

McArthur et al. (2007b)

Peregrinu s

0.70 0.5 0.0 7370 3 8

135.5 7

McArthur et al. (2007b)

Peregrinu s

0.70 1.1 0.0 7369 1 2

135.6 1

McArthur et al. (2007b)

RI

SC

NU

Furcillata

Furcillata

Peregrinu s Peregrinu s Peregrinu s Peregrinu s Peregrinu s

PT

McArthur et al. (2007b)

MA

167-168

134.1 1

D

172-172a

0.70 0.9 0.4 7379 9 2

TE

173

Furcillata

AC CE P

175 mid

Upper Valanginia n Upper Valanginia n Upper Valanginia n Upper Valanginia n Upper Valanginia n Upper Valanginia n Upper Valanginia n Upper Valanginia n Upper Valanginia n Upper Valanginia n Upper Valanginia n Upper Valanginia n Upper Valanginia n Upper Valanginia n Upper Valanginia n

54

ACCEPTED MANUSCRIPT

121–122

120–121

120

119–120

118–119

117–118

116–117

114

113–114

135.7 4

McArthur et al. (2007b)

135.7 8

McArthur et al. (2007b) McArthur et al. (2007b)

PT

McArthur et al. (2007b)

135.8 3

Verrucosu m

0.70 0.7 0.1 7364 0 1

135.8 6

McArthur et al. (2007b)

Verrucosu m

0.70 1.5 0.3 7364 3 5 0.70 0.3 0.0 7350 2 5

135.8 8

McArthur et al. (2007b)

135.9 1

McArthur et al. (2007b)

0.70 0.5 0.0 7354 6 0

135.9 3

McArthur et al. (2007b)

Verrucosu m

0.70 0.0 0.1 7361 0 4

135.9 5

McArthur et al. (2007b)

Verrucosu m

0.70 0.5 0.0 7354 6 1

135.9 6

McArthur et al. (2007b)

Verrucosu m

0.70 0.0 0.0 7366 0 5

135.9 6

McArthur et al. (2007b)

Verrucosu m

0.70 0.7 0.0 7364 7 9

135.9 9

McArthur et al. (2007b)

Verrucosu m

136.0 1

McArthur et al. (2007b)

Verrucosu m

0.70 1.5 0.2 7366 2 0 0.70 1.1 0.0 7362 5 4

136.0 3

McArthur et al. (2007b)

Verrucosu m

0.70 0.6 0.2 7353 6 2

136.0 3

McArthur et al. (2007b)

RI

Verrucosu m

SC

122–122a

135.6 9

0.70 0.3 0.0 7364 2 1 0.70 0.4 0.4 7369 6 9

NU

118–123

0.70 0.3 0.0 7365 1 2 0.70 1.0 0.0 7367 4 9

MA

320–324

Peregrinu s

Verrucosu m

D

123–123a

Peregrinu s

TE

123c–124

Peregrinu s

Verrucosu m

AC CE P

126 base

Upper Valanginia n Upper Valanginia n Upper Valanginia n Upper Valanginia n Upper Valanginia n Upper Valanginia n Upper Valanginia n Upper Valanginia n Upper Valanginia n Upper Valanginia n Upper Valanginia n Upper Valanginia n Upper Valanginia n Upper Valanginia n Upper Valanginia n

55

ACCEPTED MANUSCRIPT

311–311a

109–110

310a–311

105b–106 306b1– 306b2

105–105a

104–105

LZ 104T

103–104

McArthur et al. (2007b)

0.70 1.7 7358 7

136.0 9

McArthur et al. (2007b)

Verrucosu m

0.70 1.2 7364 6

136.0 9

McArthur et al. (2007b)

Verrucosu m

0.70 1.0 7363 0

136.1 0

McArthur et al. (2007b)

Verrucosu m

0.70 0.6 7367 8

136.1 3

McArthur et al. (2007b)

Verrucosu m

0.70 0.6 7365 9

136.1 3

McArthur et al. (2007b)

0.70 0.2 0.0 7365 2 0

136.1 4

McArthur et al. (2007b)

Verrucosu m

0.70 1.5 0.1 7358 3 3

136.2 2

McArthur et al. (2007b)

Verrucosu m

0.70 1.5 0.2 7359 6 3 0.8 0.0 2 7 0.70 0.0 0.3 7359 4 8 0.70 1.1 0.4 7359 6 4

136.2 4

McArthur et al. (2007b)

136.3 0

McArthur et al. (2007b)

136.3 3

McArthur et al. (2007b)

136.3 4

McArthur et al. (2007b)

0.70 1.4 0.0 7358 3 9 0.70 0.2 0.3 7352 8 4

136.3 6

McArthur et al. (2007b)

136.3 7

McArthur et al. (2007b)

Verrucosu m

Verrucosu m Verrucosu m Verrucosu m Verrucosu m Verrucosu m

RI

Verrucosu m

56

PT

136.0 7

SC

0.70 0.9 7365 7

NU

110–110a

McArthur et al. (2007b)

MA

312a–312c

Verrucosu m

0.2 8 0.0 2 0.1 5 0.2 2 0.0 3 0.2 6 0.0 1

136.0 7

D

312a–c

0.70 0.0 7357 0

TE

312c–312d

Verrucosu m

AC CE P

(110c)–111

Upper Valanginia n Upper Valanginia n Upper Valanginia n Upper Valanginia n Upper Valanginia n Upper Valanginia n Upper Valanginia n Upper Valanginia n Upper Valanginia n Upper Valanginia n Upper Valanginia n Upper Valanginia n Upper Valanginia n Upper Valanginia n Upper Valanginia n

ACCEPTED MANUSCRIPT

96e–97

96c–96d

95–96

93–94

89–90

87–88

80

LC 92 top

74–75

LC 86–(87)

Campyloto xus Campyloto xus Campyloto xus Campyloto xus Campyloto xus Campyloto xus Campyloto xus Campyloto xus Campyloto xus Campyloto xus

McArthur et al. (2007b)

136.3 9

McArthur et al. (2007b)

136.4 0

McArthur et al. (2007b)

136.4 2

McArthur et al. (2007b)

136.5 7

McArthur et al. (2007b)

136.6 0

McArthur et al. (2007b)

136.6 5

McArthur et al. (2007b)

136.6 9

McArthur et al. (2007b)

136.7 6

McArthur et al. (2007b)

136.8 7

McArthur et al. (2007b)

136.9 4

McArthur et al. (2007b)

137.1 5

McArthur et al. (2007b)

137.1 7

McArthur et al. (2007b)

137.3 2

McArthur et al. (2007b)

137.3 4

McArthur et al. (2007b)

PT

136.3 8

RI

SC

Campyloto xus

0.70 1.5 0.0 7343 3 0 0.70 1.1 0.6 7360 5 3 0.70 0.0 0.4 7355 9 8 0.70 0.4 0.1 7343 3 4 0.70 0.4 0.2 7358 0 5 0.70 1.3 0.2 7344 9 6 0.70 0.3 0.0 7351 6 5 0.70 0.4 0.4 7340 2 3 0.70 1.5 0.5 7354 0 4 0.70 0.8 0.2 7343 1 5 0.70 2.0 0.2 7351 6 7 0.70 0.5 0.1 7324 8 3 0.70 0.0 0.4 7321 1 0

NU

Campyloto xus

0.70 1.0 0.0 7358 0 7 0.70 0.2 0.1 7356 1 6

MA

97–97a

Verrucosu m

D

100–101

Verrucosu m

TE

102–103

Verrucosu m

AC CE P

top 103

Upper Valanginia n Upper Valanginia n Upper Valanginia n Lower Valanginia n Lower Valanginia n Lower Valanginia n Lower Valanginia n Lower Valanginia n Lower Valanginia n Lower Valanginia n Lower Valanginia n Lower Valanginia n Lower Valanginia n Lower Valanginia n Lower Valanginia n

57

ACCEPTED MANUSCRIPT

SC 55–56

53–54

46–47

43–44

V 55–56

V 54–55

V 50

V 44(–46)

V 32–33

McArthur et al. (2007b)

137.5 8

McArthur et al. (2007b)

137.6 1

McArthur et al. (2007b)

137.7 1

McArthur et al. (2007b)

137.8 1

McArthur et al. (2007b)

137.8 7

McArthur et al. (2007b)

138.0 1

McArthur et al. (2007b)

138.0 4

McArthur et al. (2007b)

138.0 9

McArthur et al. (2007b)

138.1 6

McArthur et al. (2007b)

138.4 6

McArthur et al. (2007b)

138.4 9

McArthur et al. (2007b)

138.6 4

McArthur et al. (2007b)

138.7 7

McArthur et al. (2007b)

138.9 9

McArthur et al. (2007b)

PT

137.4 5

RI

AC CE P

TE

49a

SC

59–60

NU

63–65

MA

66–67

D

70–71

Lower Campyloto Valanginia xus 0.70 2.8 0.4 n 7333 9 0 Lower Campyloto Valanginia xus 0.70 1.2 0.3 n 7331 3 2 Lower Campyloto Valanginia xus 0.70 1.1 0.0 n 7333 7 3 Lower Valanginia Pertransie 1.1 0.1 n ns 9 5 Lower Valanginia Pertransie 0.70 0.6 0.3 n ns 7334 8 9 Lower Valanginia Pertransie 0.70 1.0 0.0 n ns 7335 9 1 Lower Valanginia Pertransie 0.70 1.9 0.1 n ns 7330 2 8 Lower Valanginia Pertransie 0.70 2.9 0.2 n ns 7320 5 2 Lower Valanginia Pertransie 0.70 1.0 0.2 n ns 7310 8 1 Lower Valanginia Pertransie 0.70 0.6 0.1 n ns 7322 4 1 Lower Valanginia Pertransie 0.70 1.1 0.2 n ns 7314 1 5 Lower Valanginia Pertransie 0.70 1.0 0.3 n ns 7322 5 8 Lower Valanginia Pertransie 0.70 1.6 0.3 n ns 7322 4 8 Lower Valanginia Pertransie 0.70 0.6 0.2 n ns 7318 1 3 Lower Valanginia Pertransie 0.70 0.1 0.0 n ns 7310 5 9 58

ACCEPTED MANUSCRIPT

W 89

W 81-82

W 53-54

0.70 7293

Boissieri

0.70 7293

Boissieri

Lower Berriasian

0.70 0.2 7279 1 0.70 1.2 7278 5 0.70 1.5 7275 5 0.70 0.9 7205 4

Boissieri

Boissieri

Jacobi

59

McArthur et al. (2007b)

139.1 1

McArthur et al. (2007b)

139.1 9

McArthur et al. (2007b)

139.3 8

McArthur et al. (2007b)

139.4 4

McArthur et al. (2007b)

139.5 1

McArthur et al. (2007b)

139.8 1

McArthur et al. (2007b)

140.0 5

McArthur et al. (2007b)

144.7 6

McArthur et al. (2007b)

PT

Pertransie ns

139.1 0

RI

0.70 7293

0.4 4 0.2 1 0.0 3 0.4 5 0.3 2

SC

Pertransie ns

AC CE P

Mir 113-115

0.70 7319

1.2 6 0.7 2 0.0 2 1.2 7 1.0 3

NU

V 14b–16

Pertransie ns

MA

V 24 – 24a

0.70 7306

D

V 28a

Pertransie ns

TE

V (28a–)29

Lower Valanginia n Lower Valanginia n Lower Valanginia n Lower Valanginia n Upper Berriassia n Upper Berriassia n Upper Berriassia n Upper Berriassia n

0.1 2 0.0 7 0.5 2 0.4 1

AC CE P

TE

D

MA

NU

SC

RI

PT

ACCEPTED MANUSCRIPT

Figure 1

60

AC CE P

TE

D

MA

NU

SC

RI

PT

ACCEPTED MANUSCRIPT

Figure 2

61

Figure 3

AC CE P

TE

D

MA

NU

SC

RI

PT

ACCEPTED MANUSCRIPT

62

NU

SC

RI

PT

ACCEPTED MANUSCRIPT

AC CE P

TE

D

MA

Figure 4

63

AC CE P

TE

D

MA

NU

SC

RI

PT

ACCEPTED MANUSCRIPT

Figure 5

64

MA

NU

SC

RI

PT

ACCEPTED MANUSCRIPT

AC CE P

TE

D

Figure 6

65

AC CE P

TE

D

MA

NU

SC

RI

PT

ACCEPTED MANUSCRIPT

Figure 7 66