Isotopic and solar geochronology and climatostratigraphy of the Late Pleistocene of Northern Eurasia

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Abstract

The possibility of explaining the causes of global climatic changes in the Late Pleistocene of Northern Eurasia on the basis of the astronomical theory of climate change is shown.

In the Late Pleistocene, the effect of dividing seasonal radiation intensity by phases of annual Earth radiation intensity was found, which explains the mechanism of manifestation of the 100-millennial cycle in the Earth’s natural system. Solar tuning (modeling) of the climatic epochs of the Late Pleistocene of Northern Eurasia has been performed. Based on the model, the solar conditions and the mechanism of development of cover glaciations in Northern Eurasia in the Late Pleistocene are determined. The cause of global climate change is related to the dynamics of the radiation factor, the representative characteristics of which are the intensity of summer radiation and the intensity of winter meridional radiation heat transfer in the Northern Hemisphere. The chronological discrepancies between the model and actual climatic epochs, reflecting the nonlinear response of the natural system to the dynamics of irradiation, average about 7 thousand years. There is a weak response of the oxygen isotope composition (δ18O) of bottom foraminifera (maximum range of 0.2% fluctuations) to fluctuations in radiation factors of global climatic changes in Northern Eurasia.: the intensity of summer radiation in the phase division of seasonal radiation (the average range for the summer half-year is 0.486%, for July – 0.785%) and in the phases of climatic precession (the average range is 4.336%).

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V. M. Fedorov

Lomonosov Moscow State University

Author for correspondence.
Email: fedorov.msu@mail.ru
Russian Federation, Moscow

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2. Fig. 1. Change in insolation during the summer caloric half-year for the latitude of 65° of the Northern Hemisphere according to data from different researchers [Melnikov and Smulsky, 2009]: (a) – [Milankovich, 1939]; (b) – [Brouwer and Van Woerkom, 1950]; (c) – [Sharaf and Budnikova, 1969]; d – [Berger and Loutre, 1992]. The abscissa axis shows time in millions of years from 1950; The ordinate axis: (a, b, c) – insolation in equivalent latitudes during the summer half-year, (d) – average monthly insolation in July W (W/m2).

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3. Fig. 2. Intensity of annual irradiation of the Earth (and hemispheres) in the Neopleistocene.

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4. Fig. 3. Changes in summer radiation intensity of the Northern Hemisphere in the Neopleistocene.

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5. Fig. 4. The modulus of deviation of summer radiation intensity (amplitude) at extremes in the Northern Hemisphere from the long-term average for the Neopleistocene.

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