The Impacts of the Paleocene-Eocene Thermal Maximum (PETM) Event on Earth Surface Cycles and Its Trigger Mechanism
Received date: 2006-11-07
Revised date: 2007-02-06
Online published: 2007-04-10
The Paleocene-Eocene Thermal Maximum (PETM) event is an abrupt climate change event that occurred at the Paleocene-Eocene boundary. The event led to a sudden reversal in ocean overturning along with an abrupt rise in sea surface salinity (SSSs) and atmospheric humidity. An unusual proliferation of biodiversity and productivity during the PETM is indicative of massive fertility increasing in both oceanic and terrestrial ecosystems. Global warming enabled the dispersal of low-latitude populations into mid-and high-latitude. Biological evolution also exhibited a dramatic pulse of change, including the first appearance of many important groups of “modern” mammals (such as primates, artiodactyls, and perissodactyls) and the mass extinction of benthic foraminifera. Massive input of 12C enriched carbon into the oceanic-atmospheric system induced a prominent negative carbon isotope excursion (CIE) and rapid perturbation of global carbon cycle. The trigger mechanism of PETM remains obscure. One plausible explanation involves abrupt release of marine methane hydrate. Magma activity and bolide effect are also announced accounting for the occurrence of PETM. As for the gas hydrate hypothesis, there are still a lot of different theories explaining how the thermal or depressure dissociation of gas hydrate happened.
ZHAO Yu-long, LIU Zhi-fei
. The Impacts of the Paleocene-Eocene Thermal Maximum (PETM) Event on Earth Surface Cycles and Its Trigger Mechanism
[1]Integrated Ocean Drilling Program (IODP) Planning Sub-Committee (IPSC). Earth, Oceans and Life, IODP Initial Science Plan: 2003-2013[R].Translated by Marine Geology Key Laboratory of MOE, Tongji University. Shanghai: Tongji University Press, 2003.[IODP科学规划委员会.地球、海洋与生命,IODP初始科学计划:2003-2013[R].同济大学海洋地质教育部重点实验室译.上海:同济大学出版社,2003.]
[2]Kennett J, Scott L. Abrupt deep sea warming, paleoceanographic changes and benthic extinctions at the end of the Paleocene[J].Nature,1991,353:319-322.
[3]Liu Zhifei, Hu Xiumian. Extreme climates events in the Cretaceous and Paleogene[J].Advances in Earth Science,2003,18 (5):681-690.[刘志飞,胡修棉.白垩纪至早第三纪的极端气候事件[J].地球科学进展, 2003,18(5):681-690.]
[4]Gingerich P. Environment and evolution through the Paleocene-Eocene thermal maximum[J].Trends in Ecology and Evolution,2006,21(5):246-253.
[5]Cramer B, Kent D. Bolide summer: The Paleocene/Eocene thermal maximum as a response to an extraterrestrial trigger[J].Palaeogeography, Palaeoclimatology, Palaeoecology,2005, 224: 144-166.
[6]Moran K, Backman J, Brinkhuis H, et al. The Cenozoic palaeoenvironment of the Arctic Ocean[J]. Nature,2006,441:601-605.
[7]Zachos J, Wara M, Bohaty S, et al. A transient rise in tropical sea surface temperature during the Paleocene-Eocene thermal maximum[J].Science,2003,302(28):1 551-1 554.
[8]Nunes F, Norris R. Abrupt reversal in ocean overturning during the Paleocene/Eocene warm period [J].Nature,2006, 439: 60-63.
[9]Bowen G, Beerling D, Koch P, et al. A humid climate state during the Palaeocene/Eocene Thermal Maximum[J].Nature,2004, 432:495-499.
[10]Crouch E,Heilmann-Clausen C, Brinkhuis H, et al. Global dinoflagellate event associated with the late Paleocene thermal maximum[J].Geology,2001,29:315-318.
[11]Gibbs S, Bralower T, Bowen P, et al. Shelf and open-ocean calcareous phytoplankton assemblages across the Paleocene-Eocene Thermal Maximum: Implications for global productivity gradients[J].Geology,2006,34(4):233-236.
[12]Lu G, Keller G. Ecological stasis and saltation: species richness change in planktic foraminifera during the late Paleocene to early Eocene, DSDP Site 577[J].Palaeogeography, Palaeoclimatology, Palaeoecology,1995,117:211-227.
[13]Bains S, Norris R, Corfield R, et al. Termination of global warmth at the Palaeocene/Eocene boundary through productivity feedback[J].Nature,2000,407:171-174.
[14]Kelly D, Bralower T, Zachos J, et al. Rapid diversification of planktonic foraminifera in the tropical Pacific (ODP Site 865) during the late Paleocene thermal maximum[J].Geology,1996,24(5):423-426.
[15]Beerling D. Increased terrestrial carbon storage across the Palaeocene-Eocene boundary[J].Palaeogeography, Palaeoclimatology, Palaeoecology,2000,161:395-405.
[16]Wing S, Harrigton G, Smith F, et al. Transient floral change and rapid global warming at the Paleocene-Eocene boundary[J].Science,2005,310:993-996.
[17]Bowen G, Clyde W, Koch P, et al. Mammalian dispersal at the Paleocene/Eocene boundary [J].Science,2002,295:2 062-2 065.
[18]Clyde W, Khan I, Gingerich P. Stratigraphic response and mammalian dispersal during initial India Asia collision: Evidence from the Ghazij Formation, Baluchistan, Pakistan [J].Geology, 2003,31(12):1 097-1 100.
[19]Clyde W, Gingerich P. Mammalian community response to the latest Paleocene thermal maximum: An isotaphonomic study in the northern Bighorn basin, Wyoming [J].Geology,1998, 26(11):1 011-1 014.
[20]Bains S, Corfield R, Norris R. Mechanisms of climate warming at the end of the Paleocene[J].Science,1999,285:724-727.
[21]Dickens G, O'Neil J, Rea D, et al. Dissociation of oceanic methane hydrate as a cause of the carbon isotope excursion at the end of the Paleocene [J].Paleoceanography,1995,10:965-971.
[22]Thomas D, Zachos J, Bralower T, et al. Warming the fuel for the fire: Evidence for the thermal dissociation of methane hydrate during the Paleocene-Eocene thermal maximum [J].Geology,2002,30(12):1 067-1 070.
[23]Zachos J, Röhl U, Schellenberg S, et al. Rapid acidification of the ocean during the Paleocene-Eocene thermal maximum[J]. Science, 2005,308:1 611-1 615.
[24]Eldholm O, Thomas E. Environmental impact of volcanic margin formation[J]. Earth and Planetary Science Letters,1993,117:319-329.
[25]Bice K, Marotzke J. Numerical evidence against reversed thermohaline circulation in the warm Paleocene/Eocene ocean[J].Journal of Geophysical Research,2001,106:11 529-11 542.
[26]Thomas D, Bralower T, Jones C. Neodymium isotopic reconstruction of late Paleocene-early Eocene thermohaline circulation[J].Earth and Planetary Science Letters,2003,209:309-322.
[27]Bralower T, Thomas D, Zachos J, et al. High-resolution records of the late Paleocene thermal maximum and circum-Caribbean volcanism: Is there a causal link[J].Geology,1997,25(11):963-966.
[28]Svensen H,Planke S, Malthe-S renssen A, et al. Release of methane from a volcanic basin as a mechanism for initial Eocene global warming[J].Nature,2004,429:542-545.
[29]Lourens L, Sluijs A, Kroon D, et al. Astronomical pacing of late Palaeocene to early Eocene global warming events[J].Nature,2005, 435: 1 083-1 087.
[30]Katz M, Cramer B, Mountain G, et al. Uncorking the bottle: What triggered the Paleocene/Eocene thermal maximum methane release[J].Paleocenography,2001,16(6):549-562.
[31]Maclennan J, Jones S. Regional uplift, gas hydrate dissociation and the origins of the Paleocene-Eocene thermal maximum[J].Earth and Planetary Science Letters,2006, 245:65-80.
[32]Kent D, Cramer B, Lanci L, et al. A case for a comet impact trigger for the Paleocene/Eocene thermal maximum and carbon isotope excursion[J].Earth and Planetary Science Letters, 2003, 211:13-26.
[33]Higgins J, Schrag D. Beyond methane: Towards a theory for the Paleocene-Eocene thermal maximum[J].Earth and Planetary Science Letters,2006, 245:523-537.
[34]Kurtz A, Kump L, Arthur M, et al. Early Cenozoic decoupling of the global carbon and sulfur cycles[J].Paleoceanography,2003, 18(4):1 090, doi: 10.1029/2003PA000908.
/
| 〈 |
|
〉 |