Eocene Thermal Maximum 2

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Eocene Thermal Maximum 2 (ETM-2), also called H-1 or the Elmo event, was a transient period of global warming that occurred approximately 53.7 million years ago (Ma).[1][2][3][4] It appears to be the second major hyperthermal that punctuated the long-term warming trend from the Late Paleocene through the early Eocene (58 to 50 Ma).[5]

The hyperthermals were geologically brief time intervals (<200,000 years) of global warming and massive carbon input. The most extreme and best-studied event, the Paleocene-Eocene Thermal Maximum (PETM or ETM-1), occurred about 1.8 million years before ETM-2, at approximately 55.5 Ma. Other hyperthermals likely followed ETM-2 at nominally 53.6 Ma (H-2), 53.3 (I-1), 53.2 (I-2) and 52.8 Ma (informally called K, X or ETM-3). The number, nomenclature, absolute ages and relative global impact of the Eocene hyperthermals are the source of much current research.[6][7] In any case, the hyperthermals appear to have ushered in the Early Eocene Climatic Optimum, the warmest interval of the Cenozoic Era. They also definitely precede the Azolla event at about 49 Ma.

ETM-2 is clearly recognized in sediment sequences by analyzing the stable carbon isotope composition of carbon-bearing material.[1][2][4][6][7] The 13C/12C ratio of calcium carbonate or organic matter drops significantly across the event. This is similar to what happens when one examines sediment across the PETM, although the magnitude of the negative carbon isotope excursion is not as large. The timing of Earth system perturbations during ETM-2 and the PETM also appear different.[4] Specifically, the onset of ETM-2 may have been longer (perhaps 30,000 years) while the recovery seems to have been shorter (perhaps <50,000 years).[4] (Note, however, that the timing of short-term carbon cycle perturbations during both events remains difficult to constrain).

A thin clay-rich horizon marks ETM-2 in marine sediment from widely separated locations. In sections recovered from the deep-sea (for example those recovered by Ocean Drilling Program Leg 208 on Walvis Ridge), this layer is caused by dissolution of calcium carbonate.[4] However, in sections deposited along continental margins (for example those now exposed along the Clarence River, New Zealand), the clay-rich horizon represents dilution by excess accumulation of terrestrial material entering into the ocean.[2] Similar changes in sediment accumulation are found across the PETM.[2] In sediment from Lomonosov Ridge in the Arctic Ocean, intervals across both ETM-2 and the PETM shows signs of higher temperature, lower salinity and lower dissolved oxygen.[3]

The PETM and ETM-2 are thought to have a similar generic origin,[2][3][4] although this idea is at the edge of current research. During both events, a tremendous amount of 13C-depleted carbon rapidly entered the ocean and atmosphere. This decreased the 13C/12C ratio of carbon-bearing sedimentary components, and dissolved carbonate in the deep ocean. Somehow the carbon input was coupled to an increase in Earth surface temperature and a greater seasonality in precipitation, which explains the excess terrestrial sediment discharge along continental margins. Possible explanations for changes during ETM-2 are the same as those for the PETM, and are discussed under the latter entry.

The H-2 event appears to be a "minor" hyperthermal that follows ETM-2 (H-1) by about 100,000 years. This has led to speculation that the two events are somehow coupled and paced by changes in orbital eccentricity.[2][4]

As in the case of the PETM, reversible dwarfing of mammals has been noted during the ETM-2.[8]

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References[edit]

  1. ^ a b Lourens, L.J.; Sluijs, A.; Kroon, D.; Zachos, J.C.; Thomas, E.; Röhl, U.; Bowles, J.; Raffi, I. (2005). "Astronomical pacing of late Palaeocene to early Eocene global warming events". Nature 435 (7045): 1083–1087. Bibcode:2005Natur.435.1083L. doi:10.1038/nature03814. PMID 15944716. 
  2. ^ a b c d e f Nicolo, M.J.; Dickens, G.R.; Hollis, C.J.; Zachos, J.C. (2007). "Multiple early Eocene hyperthermals: Their sedimentary expression on the New Zealand continental margin and in the deep sea". Geology 35 (8): 699–702. doi:10.1130/G23648A.1. 
  3. ^ a b c Sluijs, A.; Schouten, S.; Donders, T.H.; Schoon. P.L.; Röhl, U.; Reichart, G.-J.; Sangiorgi, F.; Kim, J.-H.; Sinninghe Damsté, J.S.; Brinkhuis, H. (2009). "Warm and wet conditions in the Arctic region during Eocene Thermal Maximum 2". Nature Geoscience 2 (11): 777–780. Bibcode:2009NatGe...2..777S. doi:10.1038/ngeo668. 
  4. ^ a b c d e f g Stap, L.; Lourens, L.J.; Thomas, E.; Sluijs, A.; Bohaty, S.; Zachos, J.C. (2010). "High-resolution deep-sea carbon and oxygen isotope records of Eocene Thermal Maximum 2 and H2". Geology 38 (7): 607–610. doi:10.1130/G30777.1. 
  5. ^ Zachos, J.C.; Dickens, G.R.; Zeebe, R.E. (2008). "An early Cenozoic perspective on greenhouse warming and carbon-cycle dynamics". Nature 451 (7176): 279–283. Bibcode:2008Natur.451..279Z. doi:10.1038/nature06588. PMID 18202643. 
  6. ^ a b Slotnick, B.S.; Dickens. G.R.; Nicolo, M.J.; Hollis, C.J.; Crampton, J.S.; Zachos, J.C.; Sluijs, A. (2012). "Large amplitude variations in carbon cycling and terrestrial weathering during the latest Paleocene and earliest Eocene: The record at Mead Stream, New Zealand". Journal of Geology 120: 487–505. Bibcode:2012JG....120..487S. doi:10.1086/666743. 
  7. ^ a b Abels, H.A..; Clyde, H.C.; Gingerich, P.D.; Hilgen, F.J.,; Fricke, H.C.; Bowen, G.J.; Lourens, L.J. (2012). "Terrestrial carbon isotope excursions and biotic change during Palaeogene hyperthermals". Nature Geoscience 5 (8): 326–329. doi:10.1038/NGEO1427. 
  8. ^ Erickson, J. (2013-11-01). "Global warming led to dwarfism in mammals — twice". University of Michigan. Retrieved 2013-11-12. 

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