Global sea-level fluctuations during the Last Interglaciation (MIS 5e) |
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| Institution: | 1. School of Earth and Environmental Sciences, University of Wollongong, Wollongong, NSW 2522, Australia;2. Institute of Arctic and Alpine Research, University of Colorado, Boulder, CO 80309, USA;3. Marine Sciences Department, University of North Carolina, Chapel Hill, NC 27599-3300, USA;4. Department of Environmental and Geographical Sciences, Manchester Metropolitan University, Manchester M1 5GD, UK;5. Research School of Earth Sciences, The Australian University, Canberra, ACT 0000, Australia;1. Department of Earth and Planetary Sciences, Birkbeck, University of London, Malet Street, Bloomsbury, London WC1E 7HX, UK;2. Department of Earth Sciences, Oxford University, South Parks Road, Oxford OX1 3AN, UK;3. School of Geoscience, University of Edinburgh, Grant Institute, The King''s Buildings, West Mains Road, Edinburgh EH9 3JW, UK;1. Department of Physical Geography and the Bolin Centre for Climate Research, Stockholm University, 106 91 Stockholm, Sweden;2. Department of Geosciences and Geography, P.O. Box 64, 00014 University of Helsinki, Finland;3. Institute for Biodiversity and Ecosystem Dynamics (IBED), University of Amsterdam, Science Park 904, 1098 XH Amsterdam, The Netherlands;4. Department of Environmental Sciences, P.O. Box 65, 00014 University of Helsinki, Finland;5. Department of Geological Sciences and the Bolin Centre for Climate Research, Stockholm University, 106 91 Stockholm, Sweden;6. Department of Earth Science and Bjerknes Centre for Climate Research, University of Bergen. P.O. 7803, N-5007 Bergen, Norway;7. Department of Earth Sciences, VU University Amsterdam, De Boelelaan 1085, 1081 HV Amsterdam, The Netherlands;1. MARUM – Center for Marine Environmental Sciences, University of Bremen, Leobener Strasse, 28359 Bremen, Germany;2. British Antarctic Survey, High Cross, Madingley Road, CB3 0ET Cambridge, UK;3. Environmental Change Research Centre, Department of Geography, University College London, London WC1E 6BT, UK;4. Royal Belgian Institute of Natural Sciences, Jennerstraat 13, B-1000 Brussels, Belgium;5. GEOTOP, Université du Québec à Montréal, Montréal, H3C 3P8, Canada;6. Institut des sciences de la mer de Rimouski (ISMER), Canada Research Chair in Marine Geology, Université du Québec à Rimouski, Rimouski, Canada;7. GEOTOP Research Center, Canada;8. College of Earth, Ocean, and Atmospheric Sciences, Oregon State University, 104 CEOAS Admin Bldg., Corvallis, Oregon 97331-5503, USA;9. Institut Pierre-Simon Laplace/Laboratoire des Sciences du Climat et de l''Environnement, UMR 8212, CEA-CNRS-UVSQ, 91190 Gif-sur-Yvette, France;10. Centre for Ice and Climate, Niels Bohr Institute, University of Copenhagen, Denmark;11. UMR 7194 CNRS “Histoire Naturelle de l''Homme Préhistorique”, Département de Préhistoire, Muséum national d''histoire naturelle, Institut de Paléontologie Humaine, 75013 Paris, France;12. Department of Environmental Chemistry, Institute of Environmental Assessment and Water Research (IDÆA), Spanish Council for Scientific Research (CSIC), 08034 Barcelona, Spain;13. Alfred Wegener Institute Helmholtz Centre for Polar and Marine Research, Am Handelshafen 12, D-27570 Bremerhaven, Germany;14. Institute of Environmental Science and Technology and Department of Geography, Universitat Autònoma de Barcelona, 08193 Bellaterra, Spain;15. Laboratoire de Glaciologie et Géophysique de l''Environnement, UJF, CNRS, 54 rue Molière, 38402 St Martin d’Hères, France;p. Centre for Past Climate Studies, Department of Geoscience, Aarhus University, Høegh-Guldsbergs Gade 2, Aarhus C DK-8000, Denmark;q. Institució Catalana de Recerca i Estudis Avançats (ICREA) and Institut de Ciència i Tecnologia Ambientals (ICTA), Departament de Física, Universitat Autònoma de Barcelona, 08193 Bellaterra, Spain;1. British Antarctic Survey, High Cross, Madingley Road, Cambridge, CB3 0ET, UK;2. Ocean and Earth Science, National Oceanography Centre, University of Southampton Waterfront Campus, European Way, Southampton, SO14 3ZH, UK;1. Marine Geoscience Unit, Council for Geoscience, PO Box 572, Bellville 7535, South Africa;2. Centre for Coastal Palaeoscience, Nelson Mandela University, Port Elizabeth, Eastern Cape 6031, South Africa;3. ARC Centre of Excellence for Australian Biodiversity and Heritage, Centre for Archaeological Science, School of Earth and Environmental Sciences, University of Wollongong, New South Wales 2522, Australia;4. Department of Geological Sciences, University of Cape Town, University Avenue, Rondebosch 7700, South Africa;5. Institute of Human Origins, School of Human Evolution and Social Change, Arizona State University, Tempe, AZ 85287-2402, USA;6. Evolutionary Studies Institute, University of the Witwatersrand, Private Bag 3, WITS, Johannesburg 2050, South Africa;7. Malcolm H. Wiener Laboratory for Archaeological Science, American School of Classical Studies, Souidias 54, 10676 Athens, Greece;1. Institute for Geological and Geochemical Research, Research Centre for Astronomy and Earth Sciences, Hungarian Academy of Sciences, Budapest, Budaörsi út 45, H-1112, Hungary;2. Department of Physical and Applied Geology, Eötvös University, Budapest, Pázmány Péter sétány 1/C, H-1117, Hungary;3. High-Precision Mass Spectrometry and Environment Change Laboratory (HISPEC), Department of Geosciences, National Taiwan University, Taipei 10617, Taiwan;4. University of Lausanne, Institute of Earth Surface Dynamics, CH-1015 Lausanne, Switzerland;5. Hungarian Meteorological Service, Budapest, Kitaibel Pál u. 1, H-1024, Hungary;6. Geodetic and Geophysical Institute, Research Centre for Astronomy and Earth Sciences, Hungarian Academy of Sciences, Sopron, Csatkai E. u. 6-8, H-9400, Hungary |
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| Abstract: | The geomorphology and morphostratigraphy of numerous worldwide sites reveal the relative movements of sea level during the peak of the Last Interglaciation (Marine Isotope Stage (MIS) 5e, assumed average duration between 130±2 and 119±2 ka). Because sea level was higher than present, deposits are emergent, exposed, and widespread on many stable coastlines. Correlation with MIS 5e is facilitated by similar morphostratigraphic relationships, a low degree of diagenesis, uranium–thorium (U/Th) ages, and a global set of amino-acid racemization (AAR) data. This study integrates information from a large number of sites from tectonically stable areas including Bermuda, Bahamas, and Western Australia, and some that have experienced minor uplift (～2.5 m/100 ka), including selected sites from the Mediterranean and Hawaii. Significant fluctuations during the highstand are evident at many MIS 5e sites, revealed from morphological, stratigraphic, and sedimentological evidence. Rounded and flat-topped curves derived only from reef tracts are incomplete and not representative of the entire interglacial story. Despite predictions of much different sea-level histories in Bermuda, the Bahamas, and Western Australia due to glacio- and hydro-isostatic effects, the rocks from these sites reveal a nearly identical record during the Last Interglaciation.The Last Interglacial highstand is characterized by several defined sea-level intervals (SLIs) that include: (SLI#1) post-glacial (MIS 6/5e Termination II) rise to above present before 130 ka; (SLI#2) stability at +2 to +3 m for the initial several thousand years (～130 to ～125 ka) during which fringing reefs were established and terrace morphology was imprinted along the coastlines; (SLI#3) a brief fall to near or below present around 125 ka; (SLI#4) a secondary rise to and through ～+3–4 m (～124 to ～122 ka); followed by (SLI#5) a brief period of instability (～120 ka) characterized by a rapid rise to between +6 to +9 m during which multiple notches and benches were developed; and (SLI#6) an apparently rapid descent of sea level into MIS 5d after 119 ka. U/Th ages are used to confirm the Last Interglacial age of the deposits, but unfortunately, in only two cases was it possible to corroborate the highstand subdivisions using radiometric ages.Sea levels above or at present were relatively stable during much of early MIS 5e and the last 6–7 ka of MIS 1, encouraging a comparison between them. The geological evidence suggests that significant oceanographic and climatic changes occurred thereafter, midway through, and continuing through the end of MIS 5e. Fluctuating sea levels and a catastrophic termination of MIS 5e are linked to the instability of grounded and marine-based ice sheets, with the Greenland (GIS) and West Antarctic (WAIS) ice sheets being the most likely contributors. Late MIS 5e ice volume changes were accompanied by oceanographic reorganization and global ecological shifts, and provide one ominous scenario for a greenhouse world. |
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