Late Eocene Asian Climate Seasonality inferred from δ18O of Tarim Basin Oyster Shell Laurie Bougeois
Internship supervised by Guillaume DupontNivet in the Paleomagnetic Laboratory, University of Utrecht
Introduction
Eocene – Oligocene World
Blackey, NAU
Localisation
Tarim Basin We st Ku n
lun
Tibetan Plateau
Hi ma
lay a
maps.google.com
Bosboom 2008
Our study : localisation
Oyster
Bosboom 2008
Geological background
Bashibulake Formation
Yin et al., 2002
MARINE
CONTINENTAL
Stratigraphy Early Priabonian Red mudstones + siltstones
Around 36Ma
Limestones + green calcareous siltstones Green marls
Oyster 60,6 m Massive calcareous green sandstones + limestones
Bosboom 2008
Determination of oyster
16 cm Xiu, 1997 and personal communication
Problem : Sokolowia buhsii assigned to Wulagen Formation
➔
Material This oyster provides an unique record of seasonality ● ● ●
Direct record of water chemistry Continuous record Very high resolution
4 cm
Material How? ● ●
Oxygen isotopes analysis Study along a perpendicular transect of growth lines in the ligamental area
Section
4 cm
Isotopes analysis
The MicromillTM
Isotopes analysis
93 lines drilled perpendicularly to the growth direction.
Length = between 0,2 and 0,4 cm Width = 30 µm Space between each lines = 120 µm
Methods – Notions of geochemistry What is δ18O ?
18
0 16 sample 0 18 O ‰= 18 − 1×1000 0 16 ref 0
Reference : ● PDB for calcite ● SMOW for seawater
Fractionation between 16O and 18O during phase transitions
→ δ O depending on temperature and chemistry 18
δ18O = Climatic Indicator
Methods
precipitations??
δ18Op= 20‰
Mountains elevation?? δ18Op= 3‰
Connexion??
Open ocean
Paratethys δ18Ow = ???
δ18Ow = 1‰
T(°C) = 16 – 4.14 * (δ18Oc – δ18Ow) => ΔT = 4,14 * Δδ18Oc ???
calculated
???
Expected results Result from Buick and Ivany on the fossil bivalve Cuculaea raea, from the Eocene of Antartica
Buick and Ivany, 2004
Expected results 3 possible cases
Big range of temperature variations between winter and summer ➔ Arid climate Small range of temperature variations between winter and summer ➔ Temperate climate No temperature variations ➔ No record because of a secondary effect (diagenesis, chemical reactions...)
Results
Unfortunately, we are still waiting for results....
Conclusion and prospects What kind of climate during Late Eocene in West Kunlun Shan? ➔
arid/semi arid area humid area
Consistent with proxies data?
Zang et al., 2007
Conclusion and prospects What kind of climate during Late Eocene in West Kunlun Shan? ➔
Consistent with climate models?
Eldrett et al. 2009
Conclusion and prospects
For my study: ●
●
Study of δ13C correlated with δ18O → fractionation with the growth rate? Possibility to study the Sr which is an indicator of open sea
After: ● ● ●
Extend the study troughout time and space Other isotopes methods → absolute T Comparison with other global data
Thanks for your attention ~~~~ Questions?
References Anderson T.F. and Arthur M.A. 1983. Stable isotopes of oxygen and carbon and their application to sedimentologie and paleoenvironnmental problems. In Stable Isotopes in Sedimentary Geology (ed. M.A. Arthur, T.F. Anderson, I.R. Kaplan, J. Veizer, and L. Land). Society of Ecomo;ic Paleontologists and mineralogists, Short Course, p 1151 Bosboom, R.E. 2008. The retreat of the Paratethys from the Tarim Basin (West China) linked to the EoceneOligocene climate transition and the IndoAsia collision. p117 Charlier B.L.A., Ginibre C., Morgan D., Nowell G.M., Pearson D.G., Davidson J.P., Ottley C.J. 2006. Methods for the microsampling and highprecision analysis of strontium and rubidium isotopes at single crystal scale for petrological and geochronolical applications. Chemical Geology 232. p 114133 Craig H. 1965. Mesurment of oxygen isotope paleotemperatures. In Stable Isotopes in Oceanographic Studies and Paleotemperatures (ed. E. Tongiorgi), Consiglio Nazionale Delle Richerche Laboratorio Di Geologica Nucleare. P 9130 DeConto, R.M., and Pollard, D., 2003, Rapid Cenozoic glaciation of Antarctica induced by declining atmospheric CO2: Nature, v. 421, p. 245249. DupontNivet, G., Krijgsman, C.G., Abels, H.A., Dai, S., Fang, X., 2007. Tibetan Plateau aridification linked to global cooling at the EoceneOligocene transition. Nature 445, p 635638 Epstein S., Buchsbaum R., Lowenstam H.A., Urey H.C. !(%! Carbonatewater isotopic temperature scale. Bulletin of the Geological Society of America 64, p 13151326 Graham S.A., Chamberlain C., Yue Y. Ritts B., Hanson A.D., Horton T.W., Walldbauer J.R., Poage M.A., Feng X. 2005. Stable isotope records of Cenozoic climate and topography, Tibetan Plateau and Tarim Basin. American Journal of Science vol. 305. p101–118 Jin X., Wang J., Chen B., Ren L. 2003 Cenozoic depositional sequences in the piedmont of the west Kunlun and their paleogeographic and tectonic implications . Journal of Asian Earth Sciences 21. p755–765 Kaandorp, Vonhof, Wesselinghb, Romero Pittmand, Kroona, van Hinte. 2005. Seasonal Amazonian rainfall variation in the Miocene Climate Optimum . Palaeogeography, Palaeoclimatology, Palaeoecology 221. p16 Kaandorp, Wesselingh, Vonhof. 2006. Ecological implications from geochemical records of Miocene Western Amazonian bivalves . Journal of South American Earth Sciences 21. p5474 Katz, M.E., Miller, K.G., Wright, J.D., Wade, B.S., Browning, J.V., Cramer, B.S., and Rosenthal, Y., 2008, Stepwise transition from the Eocene greenhouse to the Oligocene icehouse: Nature Geosciences, v. 1, p. 329334.
Kennett, J.P., 1977, Cenozoic evolution of Antarctic glaciation, the circumAntarctic oceans and their impact on global paleoceanography: J. Geophys. Res., v. 82, p. 38433859. Langlet D. 2002. Enregistrement haute fréquence des conditions environnementales par les tests de bivalves. Application des techniques de marquage, cathodoluminescence, et chimie à l'huître Crassostrea gigas de l'étang de Tha (Hérault, France). Thèse doctorale de l'université Pierre et Marie Curie Paris VI. Langlet D., AlunnoBruscia M., Rafelis M., Renard M., Roux M., Schein E., Buestel D. 2006. Experimental and natural manganese induced cathodoluminescence in the shell of the Japanese oyster Crassostrea gigas (Thunberg, 1793) from Thau Lagoon (Hérault, France) : ecological and environment implications. Marine Ecology Progress Series 317. p 143156 Lartaud F. 2007. Les fluctuations haute fréquence de l'environnement au cours des temps géologiques. Mise au point d'une modèle de référence actuel sur l'enregistrement des contrastes saisonniers dans l'Atlantique Nord. Thèse doctorale de l'université Pierre et Marie Curie Paris VI. Meehl, G.A., 1992, Effect of tropical topography on global climate: Annual review of Earth and Planetary Sciences, v. 20, p. 85112 Popov, S., Rögl, F., Rozanov, A.Y., Steininger, F.F., Shcherba, I.G., and Kovac, M., 2004, LithologicalPaleogeographic maps of Paratethys 10 Maps Late Eocene to Pliocene: Courier Forschungsinstitut Senckenberg, v. 250, p. 142. Ramstein G., Fluteau F., Besse J., Joussaume S. 1997. Effect of orogeny, plate motion and landsea distribution on Eurasian climate change over the past 30 million years. Nature vol 386 p 788795 Raymo, M.E., Ruddiman, W.F., and Froelich, P.N., 1988, Influence of late Cenozoic mountain building on ocean geochemical cycles: Geology, v. 16, p. 649653. Ritts B., Yue Y., GRAHAM S., Sobel E., Abbink O.A., Stockli D. 2008. From sea leveal to high elevation in 15 million years : uplift history of the northern Tibetan Plateau margin in the Altun Shan. American Journal of Science vol. 308. 657– 678 Schmidt G.A. 1999 Forward modelling of carbonate proxy data from planktonic foraminifera using oxygen isotope tracers in a global ocean model. Paleoceanography> 14 p 482498 Xiu L. 1997 Paleogene bivalve communities in the Tarim Basin and their paleoenvironmental implications. Paleowords Number 7. p137157 Yin A., P.E. Rumelhart, R. Butler, E. Cowgill, T.M. Harrison. 2002. Tectonic history of the Altyn Tagh fault system in northern Tibet inferred from Cenozoic sedimentation . GSA bulletin vol. 114. p1257–1295 Zhang, Z., Wang, H., Guo, Z., and Jiang, D., 2007, What triggers the transition of palaeoenvironmental patterns in China, the Tibetan Plateau uplift or the Paratethys Sea retreat?: Palaeogeography, Palaeoclimatology, Palaeoecology, v. 245, p. 317331.
Acknowledgments
Guillaume DupontNivet GertJan Reichart Miriam Shutter Arnold van Dijk
Methods – Notions of geochemistery What is δ18O ?
18
0 16 sample 0 18 O ‰= 18 − 1×1000 0 16 ref 0
●
●
Reference : ● PDB for calcite ● SMOW for seawater
In water : 160 is heavier than 180 → so during a phase transition, 160 goes in the more volatile phase In calcite : role of temperature ➔ For 2 cases : FRACTIONATION
δ18O of sea water is a proxie of the ice volume
Methods Relationship between temperature of seawater T(°C), δ18Oc of calcite shell (‰, PDB) and δ18Ow of surrounding water (‰, SMOW) (Epstein et al., 1951 Craig,1965 Anderson and Arthur, 1983)
T(°C) = 16 – 4.14 * (δ18O – δ18O ) + 0.13 * (δ18O – δ18O )² c w c w ???
calculated
???
According to Zachos et al. (2004) : average for seawater during Eocene is δ18Ow (SMOW) = 1‰ (Earth without ice)
BUT ➔
large fluctuations (until 5‰ (Schmitt, 1999)) ➔ not applicable for an epicontinental sea
Methods
precipitations??
δ18Op= 20‰
Mountains elevation?? δ18Op= 3‰
Connexion??
Open ocean δ18Ow = 1‰
Paratethys δ18Ow = ???
Method T(°C) = 16 – 4.14 * (δ18O – δ18O ) + 0.13 * (δ18O – δ18O )² c w c w ???
calculated
???
δ18Ow unknown → absolute T unknown
BUT we can reconstitute the variations of temperature
➔
ΔT ≈ 4,14 * (Δδ18Oc – Δδ18Ow)
End: sea water oxygen isotope composition remains constant throughout the year → Δδ18Ow = 0
So: ΔT ≈ 4,14 * Δδ18Oc