Earth:Eemian

From HandWiki
Short description: Interglacial period which began 130,000 years ago
Two ice core temperature records; the Eemian is at a depth of about 1500–1800 meters in the lower graph
CO
2 concentrations over the last 400,000 years.

The Eemian (also called the last interglacial,[1] Sangamonian Stage, Ipswichian, Mikulin, Kaydaky, penultimate interglacial,[2] Valdivia or Riss-Würm) was the interglacial period which began about 130,000 years ago at the end of the Penultimate Glacial Period and ended about 115,000 years ago at the beginning of the Last Glacial Period.[3] It corresponds to Marine Isotope Stage 5e.[4] Although sometimes referred to as the "last interglacial" (in the "most recent previous" sense of "last"), it was the second-to-latest interglacial period of the current Ice Age, the most recent being the Holocene which extends to the present day (having followed the last glacial period). The prevailing Eemian climate was, on average, around 1 to 2 degrees Celsius (1.8 to 3.6 Fahrenheit) warmer than that of the Holocene.[5] During the Eemian, the proportion of CO
2 in the atmosphere was about 280 parts per million.[6]

The Eemian is known as the Ipswichian in the United Kingdom , the Mikulin interglacial in Russia , the Valdivia interglacial in Chile and the Riss-Würm interglacial in the Alps. Depending on how a specific publication defines the Sangamonian Stage of North America, the Eemian is equivalent to either all or part of it.

The period falls into the Middle Paleolithic and is of some interest for the evolution of anatomically modern humans, who were present in Western Asia (Skhul and Qafzeh hominins) as well as in Southern Africa by this time, representing the earliest split of modern human populations that persists to the present time (associated with mitochondrial haplogroup L0).[7]

Climate

View of the Eemian-aged coastal terraces of Niebla near Valdivia, Chile .

Global temperatures

The Eemian climate is believed to have been warmer than the current Holocene.[8][9] Changes in the Earth's orbital parameters from today (greater obliquity and eccentricity, and perihelion), known as Milankovitch cycles, probably led to greater seasonal temperature variations in the Northern Hemisphere.[citation needed] As the Eemian cooled, pCO2 remained stable.[10]

During the northern summer, temperatures in the Arctic region were about 2–4 °C higher than in 2011.[11] The Arctic Eemian climate was highly unstable, with pronounced temperature swings revealed by δ18O fluctuations in Greenlandic ice cores,[12] though some of the instability inferred from Greenland ice core project records may be a result of mixing of Eemian ice with ice from the preceding or succeeding glacial intervals.[13]

The warmest peak of the Eemian was around 125,000 years ago, when forests reached as far north as North Cape, Norway (which is now tundra) well above the Arctic Circle at [ ⚑ ] 71°10′21″N 25°47′40″E / 71.1725°N 25.79444°E / 71.1725; 25.79444. Hardwood trees such as hazel and oak grew as far north as Oulu, Finland. At the peak of the Eemian, the Northern Hemisphere winters were generally warmer and wetter than now, though some areas were actually slightly cooler than today. The hippopotamus was distributed as far north as the rivers Rhine and Thames.[14] A 2018 study based on soil samples from Sokli in northern Finland identified abrupt cold spells ca. 120,000 years ago caused by shifts in the North Atlantic Current, lasting hundreds of years and causing temperature drops of a few degrees and vegetation changes in these regions. In Northern Europe, winter temperatures rose over the course of the Eemian while summer temperatures fell.[15] During an insolation maximum from 133,000 to 130,000 BP, meltwater from the Dnieper and Volga caused the Black and Caspian Seas to connect.[16] During the mid-Eemian, a weakened Atlantic Meridional Overturning Circulation (AMOC) began to cool the eastern Mediterranean region.[17] The period closed as temperatures steadily fell to conditions cooler and drier than the present, with a 468-year-long aridity pulse in central Europe at about 116,000 BC,[18] and by 112,000 BC, ice caps began to form in southern Norway, marking the start of a new glacial period.[19] Kaspar et al. (GRL, 2005) performed a comparison of a coupled general circulation model (GCM) with reconstructed Eemian temperatures for Europe. Central Europe (north of the Alps) was found to be 1–2 °C (1.8–3.6 °F) warmer than present; south of the Alps, conditions were 1–2 °C cooler than today. The model (generated using observed greenhouse gas concentrations and Eemian orbital parameters) generally reproduces these observations, leading them to conclude that these factors are enough to explain the Eemian temperatures.[20]

Meltwater pulse 2B, approximately 133,000 BP, substantially weakened the Indian Summer Monsoon (ISM).[21]

Trees grew as far north as southern Baffin Island in the Canada Arctic Archipelago: currently, the northern limit is further south at Kuujjuaq in northern Quebec. Coastal Alaska was warm enough during the summer due to reduced sea ice in the Arctic Ocean to allow Saint Lawrence Island (now tundra) to have boreal forest, although inadequate precipitation caused a reduction in the forest cover in interior Alaska and Yukon Territory despite warmer conditions.[22] The prairie-forest boundary in the Great Plains of the United States lay further west near Lubbock, Texas, whereas the current boundary is near Dallas.

Interglacial conditions ended on Antarctica while the Northern Hemisphere was still experiencing warmth.[23]

All palaeotemps.svg

Sea level

Eemian erosion surface in a fossil coral reef on Great Inagua, The Bahamas. Foreground shows corals truncated by erosion; behind the geologist is a post-erosion coral pillar which grew on the surface after sea level rose again.[24]

Sea level at peak was probably 6 to 9 metres (20 to 30 feet) higher than today,[25][26] with Greenland contributing 0.6 to 3.5 m (2.0 to 11.5 ft),[27] thermal expansion and mountain glaciers contributing up to 1 m (3.3 ft),[28] and an uncertain contribution from Antarctica.[29] A 2007 study found evidence that the Greenland ice core site Dye 3 was glaciated during the Eemian,[30] which implies that Greenland could have contributed at most 2 m (6.6 ft) to sea level rise.[31][32] Recent research on marine sediment cores offshore of the West Antarctic Ice Sheet suggest that the sheet melted during the Eemian, and that ocean waters rose as fast as 2.5 meters per century.[33] Global mean sea surface temperatures are thought to have been higher than in the Holocene, but not by enough to explain the rise in sea level through thermal expansion alone, and so melting of polar ice caps must also have occurred.

Because of the sea level drop since the Eemian, exposed fossil coral reefs are common in the tropics, especially in the Caribbean and along the Red Sea coastlines. These reefs often contain internal erosion surfaces showing significant sea level instability during the Eemian.[34]

Along the Central Mediterranean Spanish coast, sea levels were comparable to those of the present.[35] Scandinavia was an island. Vast areas of northwestern Europe and the West Siberian Plain were inundated.[36]

Definition of the Eemian

Bittium reticulatum Picture from Pieter Harting (1886) assigned by him as 'Index fossil' for the Eemian.

The Eemian Stage was first recognized from boreholes in the area of the city of Amersfoort, Netherlands, by Pieter Harting (1875). He named the beds "Système Eémien", after the river Eem on which Amersfoort is located. Harting noticed the marine molluscan assemblages to be very different from the modern fauna of the North Sea. Many species from the Eemian layers nowadays show a much more southern distribution, ranging from South of the Strait of Dover to Portugal (Lusitanian faunal province) and even into the Mediterranean (Mediterranean faunal province). More information on the molluscan assemblages is given by Lorié (1887), and Spaink (1958). Since their discovery, Eemian beds in the Netherlands have mainly been recognized by their marine molluscan content combined with their stratigraphical position and other palaeontology. The marine beds there are often underlain by tills that are considered to date from the Saalian, and overlain by local fresh water or wind-blown deposits from the Weichselian. In contrast to e.g. the deposits in Denmark, the Eemian deposits in the type area have never been found overlain by tills, nor in ice-pushed positions.

Van Voorthuysen (1958) described the foraminifera from the type site, whereas Zagwijn (1961) published the palynology, providing a subdivision of this stage into pollen stages. At the end of the 20th century, the type site was re-investigated using old and new data in a multi-disciplinary approach (Cleveringa et al., 2000). At the same time a parastratotype was selected in the Amsterdam glacial basin in the Amsterdam-Terminal borehole and was the subject of a multidisciplinary investigation (Van Leeuwen, et al., 2000). These authors also published a U/Th age for late Eemian deposits from this borehole of 118,200 ± 6,300 years ago. A historical review of Dutch Eemian research is provided by Bosch, Cleveringa and Meijer, 2000.

See also

References

  1. ↑ Adams, Jonathan; Maslin, Mark; Thomas, Ellen. "Sudden climate transitions during the Quaternary". Oak Ridge National Laboratory. http://www.esd.ornl.gov/projects/qen/transit.html. 
  2. ↑ NOAA - Penultimate Interglacial Period http://www.ncdc.noaa.gov/global-warming/penultimate-interglacial-period
  3. ↑ Dahl-Jensen, D.; Albert, M. R.; Aldahan, A.; Azuma, N.; Balslev-Clausen, D.; Baumgartner, M.; Berggren, A. -M.; Bigler, M. et al. (2013). "Eemian interglacial reconstructed from a Greenland folded ice core". Nature 493 (7433): 489–94. doi:10.1038/nature11789. PMID 23344358. Bibcode: 2013Natur.493..489N. http://nora.nerc.ac.uk/id/eprint/500331/1/2012-07-09846-NEEM_revised.pdf. 
  4. ↑ Shackleton, Nicholas J.; Sánchez-Goñi, Maria Fernanda; Pailler, Delphine; Lancelot, Yves (2003). "Marine Isotope Substage 5e and the Eemian Interglacial". Global and Planetary Change 36 (3): 151–155. doi:10.1016/S0921-8181(02)00181-9. Bibcode: 2003GPC....36..151S. http://www.colorado.edu/geography/class_homepages/geog_5241_f09/media/Readings/shackletonetal.pdf. Retrieved 2014-08-07. 
  5. ↑ "Current & Historical Global Temperature Graph". https://www.temperaturerecord.org/. 
  6. ↑ "Earth is the warmest it's been in 120,000 years". Mashable. 2018. https://mashable.com/2018/08/27/earth-warmest-temperatures-climate-change. 
  7. ↑ M Richards et al. in: Bandelt et al. (eds.), Human Mitochondrial DNA and the Evolution of Homo sapiens, Springer (2006), p. 233.
  8. ↑ "Current & Historical Global Temperature Graph". https://www.temperaturerecord.org/. 
  9. ↑ Arctic Council, Impacts of a Warming Climate: Arctic Climate Impact Assessment, Cambridge U. Press, Cambridge, 2004
  10. ↑ Brovkin, Victor; Brücher, Tim; Kleinen, Thomas; Zaehle, Sönke; Joos, Fortunat; Roth, Raphael; Spahni, Renato; Schmitt, Jochen et al. (1 April 2016). "Comparative carbon cycle dynamics of the present and last interglacial". Quaternary Science Reviews 137: 15–32. doi:10.1016/j.quascirev.2016.01.028. ISSN 0277-3791. https://www.sciencedirect.com/science/article/pii/S0277379116300300. Retrieved 1 January 2024. 
  11. ↑ Nathaelle Bouttes (2011). "Warm past climates: is our future in the past?". The National Centre for Atmospheric Science. https://www.ncas.ac.uk/en/climate-blog/397-warm-past-climates-is-our-future-in-the-past. 
  12. ↑ Johnsen, Sigfús J.; Clausen, Henrik B.; Dansgaard, Willi; Gundestrup, Niels S.; Hammer, Claus U.; Andersen, Uffe; Andersen, Katrine K.; Hvidberg, Christine S. et al. (30 November 1997). "The δ 18 O record along the Greenland Ice Core Project deep ice core and the problem of possible Eemian climatic instability" (in en). Journal of Geophysical Research: Oceans 102 (C12): 26397–26410. doi:10.1029/97JC00167. 
  13. ↑ Chappellaz, Jérôme; Brook, Ed; Blunier, Thomas; Malaizé, Bruno (30 November 1997). "CH 4 and δ 18 O of O 2 records from Antarctic and Greenland ice: A clue for stratigraphic disturbance in the bottom part of the Greenland Ice Core Project and the Greenland Ice Sheet Project 2 ice cores" (in en). Journal of Geophysical Research: Oceans 102 (C12): 26547–26557. doi:10.1029/97JC00164. ISSN 0148-0227. 
  14. ↑ van Kolfschoten, Th. (2000). "The Eemian mammal fauna of central Europe". Netherlands Journal of Geosciences 79 (2/3): 269–281. doi:10.1017/S0016774600021752. 
  15. ↑ Salonen, J. Sakari; Helmens, Karin F.; Brendryen, Jo; Kuosmanen, Niina; Väliranta, Minna; Goring, Simon; Korpela, Mikko; Kylander, Malin et al. (20 July 2018). "Abrupt high-latitude climate events and decoupled seasonal trends during the Eemian" (in en). Nature Communications 9 (1): 2851. doi:10.1038/s41467-018-05314-1. ISSN 2041-1723. PMC 6054633. https://www.nature.com/articles/s41467-018-05314-1. Retrieved 1 January 2024. 
  16. ↑ Wegwerth, Antje; Dellwig, Olaf; Wulf, Sabine; Plessen, Birgit; Kleinhanns, Ilka C.; Nowaczyk, Norbert R.; Jiabo, Liu; Arz, Helge W. (1 September 2019). "Major hydrological shifts in the Black Sea "Lake" in response to ice sheet collapses during MIS 6 (130–184 ka BP)". Quaternary Science Reviews 219: 126–144. doi:10.1016/j.quascirev.2019.07.008. ISSN 0277-3791. https://www.sciencedirect.com/science/article/pii/S0277379119304548. Retrieved 21 September 2023. 
  17. ↑ Levy, Elan J.; Vonhof, Hubert B.; Bar-Matthews, Miryam; Martínez-García, Alfredo; Ayalon, Avner; Matthews, Alan; Silverman, Vered; Raveh-Rubin, Shira et al. (25 August 2023). "Weakened AMOC related to cooling and atmospheric circulation shifts in the last interglacial Eastern Mediterranean" (in en). Nature Communications 14 (1): 5180. doi:10.1038/s41467-023-40880-z. ISSN 2041-1723. PMID 37620353. 
  18. ↑ Sirocko, F.; Seelos, K.; Schaber, K.; Rein, B.; Dreher, F.; Diehl, M.; Lehne, R.; Jäger, K. et al. (11 August 2005). "A late Eemian aridity pulse in central Europe during the last glacial inception". Nature 436 (7052): 833–6. doi:10.1038/nature03905. PMID 16094365. Bibcode: 2005Natur.436..833S. https://www.nature.com/articles/nature03905#citeas. Retrieved 17 September 2023. 
  19. ↑ Holmlund, P.; Fastook, J. (1995). "A time dependent glaciological model of the Weichselian Ice Sheet" (in en). Quaternary International 27: 53–58. doi:10.1016/1040-6182(94)00060-I. https://linkinghub.elsevier.com/retrieve/pii/104061829400060I. Retrieved 17 September 2023. 
  20. ↑ Kaspar, F.; Kühl, Norbert; Cubasch, Ulrich; Litt, Thomas (2005). "A model-data comparison of European temperatures in the Eemian interglacial". Geophysical Research Letters 32 (11): L11703. doi:10.1029/2005GL022456. Bibcode: 2005GeoRL..3211703K. http://edoc.mpg.de/256350. 
  21. ↑ Wassenburg, Jasper A.; Vonhof, Hubert B.; Cheng, Hai; Martínez-García, Alfredo; Ebner, Pia-Rebecca; Li, Xianglei; Zhang, Haiwei; Sha, Lijuan et al. (18 November 2021). "Penultimate deglaciation Asian monsoon response to North Atlantic circulation collapse" (in en). Nature Geoscience 14 (12): 937–941. doi:10.1038/s41561-021-00851-9. ISSN 1752-0908. 
  22. ↑ Vegetation and paleoclimate of the last interglacial period, central Alaska. USGS
  23. ↑ Landais, Amaelle (16 September 2003). "A tentative reconstruction of the last interglacial and glacial inception in Greenland based on new gas measurements in the Greenland Ice Core Project (GRIP) ice core" (in en). Journal of Geophysical Research 108 (D18): 1–10. doi:10.1029/2002JD003147. ISSN 0148-0227. 
  24. ↑ Wilson, M. A.; Curran, H. A.; White, B. (2007). "Paleontological evidence of a brief global sea-level event during the last interglacial". Lethaia 31 (3): 241–250. doi:10.1111/j.1502-3931.1998.tb00513.x. 
  25. ↑ Dutton, A; Lambeck, K (13 July 2012). "Ice volume and sea level during the last interglacial.". Science 337 (6091): 216–9. doi:10.1126/science.1205749. PMID 22798610. Bibcode: 2012Sci...337..216D. https://www.science.org/doi/10.1126/science.1205749#:~:text=References%20and%20Notes-,More%20Melting,10%20meters%20above%20current%20levels.. Retrieved 17 September 2023. 
  26. ↑ Kopp, RE; Simons, FJ; Mitrovica, JX; Maloof, AC; Oppenheimer, M (17 December 2009). "Probabilistic assessment of sea level during the last interglacial stage.". Nature 462 (7275): 863–7. doi:10.1038/nature08686. PMID 20016591. Bibcode: 2009Natur.462..863K. https://www.nature.com/articles/nature08686. Retrieved 17 September 2023. 
  27. ↑ Stone, E.J; Lundt, D.J; Annan, J.D.; Hargreaves, J.C. (2013). "Quantification of Greenland ice-sheet contribution to Last Interglacial sea-level rise". Climate of the Past 9 (2): 621–639. doi:10.5194/cp-9-621-2013. Bibcode: 2013CliPa...9..621S. https://cp.copernicus.org/articles/9/621/2013/cp-9-621-2013.html. Retrieved 17 September 2023. 
  28. ↑ McKay, Nicholas P.; Overpeck, Jonathan T.; Otto-Bliesner, Bette L. (July 2011). "The role of ocean thermal expansion in Last Interglacial sea level rise". Geophysical Research Letters 38 (14): n/a. doi:10.1029/2011GL048280. Bibcode: 2011GeoRL..3814605M. 
  29. ↑ Scherer, RP; Aldahan, A; Tulaczyk, S; Possnert, G; Engelhardt, H; Kamb, B (3 July 1998). "Pleistocene collapse of the west antarctic ice sheet". Science 281 (5373): 82–5. doi:10.1126/science.281.5373.82. PMID 9651249. Bibcode: 1998Sci...281...82S. 
  30. ↑ Willerslev, E.; Cappellini, E.; Boomsma, W.; Nielsen, R.; Hebsgaard, M. B.; Brand, T. B.; Hofreiter, M.; Bunce, M. et al. (2007). "Ancient Biomolecules from Deep Ice Cores Reveal a Forested Southern Greenland". Science 317 (5834): 111–4. doi:10.1126/science.1141758. PMID 17615355. PMC 2694912. Bibcode: 2007Sci...317..111W. http://researchrepository.murdoch.edu.au/id/eprint/5130/. 
  31. ↑ Cuffey, K. M.; Marshall, S. J. (2000). "Substantial contribution to sea-level rise during the last interglacial from the Greenland ice sheet". Nature 404 (6778): 591–4. doi:10.1038/35007053. PMID 10766239. Bibcode: 2000Natur.404..591C. 
  32. ↑ Otto-Bliesner, B. L.; Marshall, Shawn J.; Overpeck, Jonathan T.; Miller, Gifford H.; Hu, Aixue (2006). "Simulating Arctic Climate Warmth and Icefield Retreat in the Last Interglaciation". Science 311 (5768): 1751–3. doi:10.1126/science.1120808. PMID 16556838. Bibcode: 2006Sci...311.1751O. 
  33. ↑ Voosen, Paul (20 December 2018). "Antarctic ice melt 125,000 years ago offers warning". Science 362 (6421): 1339. doi:10.1126/science.362.6421.1339. ISSN 0036-8075. PMID 30573605. Bibcode: 2018Sci...362.1339V. 
  34. ↑ Hamed, Basher; Bussert, Robert; Dominik, Wilhelm (1 February 2016). "Stratigraphy and evolution of emerged Pleistocene reefs at the Red Sea coast of Sudan". Journal of African Earth Sciences 114: 133–142. doi:10.1016/j.jafrearsci.2015.11.011. ISSN 1464-343X. https://www.sciencedirect.com/science/article/pii/S1464343X15301072. Retrieved 1 January 2024. 
  35. ↑ Viñals, María José; Fumanal, María Pilar (January 1995). "Quaternary development and evolution of the sedimentary environments in the Central Mediterranean Spanish coast" (in en). Quaternary International 29-30: 119–128. doi:10.1016/1040-6182(95)00014-A. https://linkinghub.elsevier.com/retrieve/pii/104061829500014A. Retrieved 17 September 2023. 
  36. ↑ Gornitz, Vivien (2013). Rising Seas: Past, Present, Future. New York: Columbia University Press. p. 101. ISBN 978-0-231-14739-2. https://books.google.com/books?id=78CrAgAAQBAJ&dq=eemian+scandinavia+island+inpublisher:university+inpublisher:press&pg=PA101. Retrieved August 9, 2021. 

Further reading

External links



Retrieved from "https://handwiki.org/wiki/index.php?title=Earth:Eemian&oldid=3294565"