Marine Isotope Stages (abbreviated MIS), sometimes referred to as Oxygen Isotope Stages (OIS), are the discovered pieces of a chronological listing of alternating cold and warm periods on our planet, going back to at least 2.6 million years. Developed by successive and collaborative work by pioneer paleoclimatologists Harold Urey, Cesare Emiliani, John Imbrie, Nicholas Shackleton, and a host of others, MIS uses the balance of oxygen isotopes in stacked fossil plankton (foraminifera) deposits on the bottom of the oceans to build an environmental history of our planet. The changing oxygen isotope ratios hold information about the presence of ice sheets, and thus planetary climate changes, on our earth's surface.
How Measuring Marine Isotope Stages Work
Scientists take sediment cores from the bottom of the ocean all over the worldand then measure the ratio of Oxygen 16 to Oxygen 18 in the calcite shells of the foraminifera. Oxygen 16 is preferentially evaporated from the oceans, some of which falls as snow on continents. Times when snow and glacial ice buildup occur therefore see a corresponding enrichment of the oceans in Oxygen 18. Thus the O18/O16 ratiochanges over time, mostly as a function of the volume of glacial ice on the planet.
Supporting evidence for the use of oxygen isotope ratios as proxies of climate change is reflected in the matching record of what scientists believe the reason for the changing amount of glacier ice on our planet. The primary reasons glacial ice varies on our planet was described by Serbian geophysicist and astronomer Milutin Milankovic (or Milankovitch) as the combination of the eccentricity of Earth's orbit around the sun, the tilt of the Earth's axis and the wobble of the planet bringing the northern latitudes nearer to or farther from the sun's orbit, all of which changes the distribution of incoming solar radiation to the planet.
Sorting Out Competing Factors
The problem is, however, that although scientists have been able to identify an extensive record of global ice volume changes through time, the exact amount of sea level rise, or temperature decline, or even ice volume, is not generally available through measurements of isotope balance, because these different factors are interrelated. However, sea level changes cansometimes be identified directly in the geological record: for example, datable cave encrustations which develop at sea levels (see Dorale and colleagues). This type of additional evidence ultimately helps sorts out the competing factors in establishing a more rigorous estimation of past temperature, sea level, or the amount of ice on the planet.
Climate Change on Earth
The following table lists a paleo-chronology of life on earth, including how the major cultural steps fit in, for the past 1 million years. Scholars have taken the MIS/OIS listing well beyond that.
Table of Marine Isotope Stages
MIS Stage | Start Date | Cooler or Warmer | Cultural Events |
MIS 1 | 11,600 | warmer | the Holocene |
MIS 2 | 24,000 | cooler | last glacial maximum, Americas populated |
MIS 3 | 60,000 | warmer | upper Paleolithic begins; Australia populated, upper Paleolithic cave walls painted, Neanderthals disappear |
MIS 4 | 74,000 | cooler | Mt. Toba super-eruption |
MIS 5 | 130,000 | warmer | early modern humans (EMH) leave Africa to colonize the world |
MIS 5a | 85,000 | warmer | Howieson's Poort/Still Bay complexes in southern Africa |
MIS 5b | 93,000 | cooler | |
MIS 5c | 106,000 | warmer | EMH at Skuhl and Qazfeh in Israel |
MIS 5d | 115,000 | cooler | |
MIS 5e | 130,000 | warmer | |
MIS 6 | 190,000 | cooler | Middle Paleolithic begins, EMH evolves, at Bouri and Omo Kibish in Ethiopia |
MIS 7 | 244,000 | warmer | |
MIS 8 | 301,000 | cooler | |
MIS 9 | 334,000 | warmer | |
MIS 10 | 364,000 | cooler | hom*o erectus at Diring Yuriahk in Siberia |
MIS 11 | 427,000 | warmer | Neanderthals evolve in Europe. This stage is thought to be the most similar to MIS 1 |
MIS 12 | 474,000 | cooler | |
MIS 13 | 528,000 | warmer | |
MIS 14 | 568,000 | cooler | |
MIS 15 | 621,000 | ccooler | |
MIS 16 | 659,000 | cooler | |
MIS 17 | 712,000 | warmer | H. erectus at Zhoukoudian in China |
MIS 18 | 760,000 | cooler | |
MIS 19 | 787,000 | warmer | |
MIS 20 | 810,000 | cooler | H. erectus at Gesher Benot Ya'aqov in Israel |
MIS 21 | 865,000 | warmer | |
MIS 22 | 1,030,000 | cooler |
Sources
Jeffrey Dorale of the University of Iowa.
Alexanderson H, Johnsen T, and Murray AS. 2010.Re-dating the Pilgrimstad Interstadial with OSL: a warmer climate and a smaller ice sheet during the Swedish Middle Weichselian (MIS 3)?Boreas39(2):367-376.
Bintanja , R. "North American ice-sheet dynamics and the onset of 100,000-year glacial cycles." Nature volume 454, R. S. W. van de Wal, Nature, August 14, 2008.
Bintanja, Richard. "Modelled atmospheric temperatures and global sea levels over the past million years." 437, Roderik S.W. van de Wal, Johannes Oerlemans, Nature, September 1, 2005.
Dorale JA,OnacBP, Fornós JJ, Ginés J, Ginés A, Tuccimei P, and Peate DW. 2010.Sea-Level Highstand 81,000 Years Ago in Mallorca.Science 327(5967):860-863.
Hodgson DA, Verleyen E, Squier AH, Sabbe K, Keely BJ, Saunders KM, and Vyverman W. 2006.Interglacial environments of coastal east Antarctica: comparison of MIS 1 (Holocene) and MIS 5e (Last Interglacial) lake-sediment records.Quaternary Science Reviews25(1–2):179-197.
Huang SP, Pollack HN, and Shen PY. 2008.A late Quaternary climate reconstruction based on borehole heat flux data, borehole temperature data, and the instrumental record.Geophys Res Lett35(13):L13703.
Kaiser J, and Lamy F. 2010.Links between Patagonian Ice Sheet fluctuations and Antarctic dust variability during the last glacial period (MIS 4-2).Quaternary Science Reviews29(11–12):1464-1471.
Martinson DG, Pisias NG, Hays JD, Imbrie J, Moore Jr TC, and Shackleton NJ. 1987.Age dating and the orbital theory of the ice ages: Development of a high-resolution 0 to 300,000-year chronostratigraphy.Quaternary Research27(1):1-29.
Suggate RP, and Almond PC. 2005.The Last Glacial Maximum (LGM) in western South Island, New Zealand: implications for the global LGM and MIS 2.Quaternary Science Reviews24(16–17):1923-1940.
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Hirst, K. Kris. "Marine Isotope Stages." ThoughtCo, Feb. 16, 2021, thoughtco.com/marine-isotope-stages-climate-world-171568.Hirst, K. Kris. (2021, February 16). Marine Isotope Stages. Retrieved from https://www.thoughtco.com/marine-isotope-stages-climate-world-171568Hirst, K. Kris. "Marine Isotope Stages." ThoughtCo. https://www.thoughtco.com/marine-isotope-stages-climate-world-171568 (accessed June 12, 2024).