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→Oxygen isotope model
==Oxygen isotope model==
==Oxygen isotope model==
[[file:applied-paleontology_fig17-29.png|thumb|{{figure number|1}}Typical oxygen isotope record for the middle Tertiary. Copyright: Wright and Miller, 1993;{{citation needed}} courtesy American Geophysical Union. Time scale adapted from Berggren et al.<ref name=ch17r12>Berggren, W., A., Kent, D., V., Flynn, J., J., 1985a, Paleogene geochronology and chronostratigraphy, in Snelling, N., J., ed., The Chronology of the Geological Record: Geological Society of London Memoir 10, p. 141–195.</ref><ref name=ch17r13>Berggren, W., A., Kent, D., and J.A. van Couvering, 1985b, Neogene geochronology and chronostratig- raphy, in N.J. Snelling, ed., The Chronology of the Geological Record: Geological Society of London Memoir 10, p. 211–260.</ref>]]
[[file:applied-paleontology_fig17-29.png|300px|thumb|{{figure number|1}}Typical oxygen isotope record for the middle Tertiary. Copyright: Wright and Miller, 1993;{{citation needed}} courtesy American Geophysical Union. Time scale adapted from Berggren et al.<ref name=ch17r12>Berggren, W., A., Kent, D., V., Flynn, J., J., 1985a, Paleogene geochronology and chronostratigraphy, in Snelling, N., J., ed., The Chronology of the Geological Record: Geological Society of London Memoir 10, p. 141–195.</ref><ref name=ch17r13>Berggren, W., A., Kent, D., and J.A. van Couvering, 1985b, Neogene geochronology and chronostratig- raphy, in N.J. Snelling, ed., The Chronology of the Geological Record: Geological Society of London Memoir 10, p. 211–260.</ref>]]
Glacial-interglacial climatic fluctuations during the late Paleogene and Neogene have been causally related to Milankovitch orbital parameters (eccentricity, obliquity, and precession). During colder glacial climates the oceans become enriched in <sup>18</sup>O relative to <sup>16</sup>O because the lighter <sup>16</sup>O molecule is more easily evaporated from seawater and becomes locked on land in the form of ice. During warmer intervals the reverse is true.
Glacial-interglacial climatic fluctuations during the late Paleogene and Neogene have been causally related to Milankovitch orbital parameters (eccentricity, obliquity, and precession). During colder glacial climates the oceans become enriched in <sup>18</sup>O relative to <sup>16</sup>O because the lighter <sup>16</sup>O molecule is more easily evaporated from seawater and becomes locked on land in the form of ice. During warmer intervals the reverse is true.