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. Bulletin of the Natural Histort Museum. Geology series. REVIEW OF STRATIGRAPHY OF EASTERN PARATETHYS 37. Fig. 10 Palaeogeographic reconstruction. Konkian to Maeotian (late Middle to early Late Miocene). Key as for Fig. 7. The location of the Konkian stratotype is indicated. hinterland. The predominance of Taxodiaceae (cypresses and swamp-cypresses) indicates a warm-temperate (possibly even subtropical) climatic regime. Sarmatian (Fig. 10) The Sarmatian of Eastern Paratethys is probably equivalent to the stratotypical Sarmatian of Central Paratethys (late Middle to early Late Miocene (calcare

. Bulletin of the Natural Histort Museum. Geology series. REVIEW OF STRATIGRAPHY OF EASTERN PARATETHYS 37. Fig. 10 Palaeogeographic reconstruction. Konkian to Maeotian (late Middle to early Late Miocene). Key as for Fig. 7. The location of the Konkian stratotype is indicated. hinterland. The predominance of Taxodiaceae (cypresses and swamp-cypresses) indicates a warm-temperate (possibly even subtropical) climatic regime. Sarmatian (Fig. 10) The Sarmatian of Eastern Paratethys is probably equivalent to the stratotypical Sarmatian of Central Paratethys (late Middle to early Late Miocene (calcare Stock Photo
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Book Worm / Alamy Stock Photo

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RGDNM5

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2074 x 1205 px | 35.1 x 20.4 cm | 13.8 x 8 inches | 150dpi

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. Bulletin of the Natural Histort Museum. Geology series. REVIEW OF STRATIGRAPHY OF EASTERN PARATETHYS 37. Fig. 10 Palaeogeographic reconstruction. Konkian to Maeotian (late Middle to early Late Miocene). Key as for Fig. 7. The location of the Konkian stratotype is indicated. hinterland. The predominance of Taxodiaceae (cypresses and swamp-cypresses) indicates a warm-temperate (possibly even subtropical) climatic regime. Sarmatian (Fig. 10) The Sarmatian of Eastern Paratethys is probably equivalent to the stratotypical Sarmatian of Central Paratethys (late Middle to early Late Miocene (calcareous nannoplankton zones NN7-NN9) (Meszaros, 1992), planktonic foraminiferal zones N137-N15), but may also be equivalent to the lower part of the Pannonian (Slavonian) of that area (Late Miocene) (see, for instance, Papp et ai. 1974, 1985). Chepalyga (1985) calibrates the Sarmatian of Eastern Paratethys against magnetostratigraphic polarity epochs 10-7, while Zubakov & Borzenkova (1990) calibrate it against epochs 14-9, and Pevzner & Vangengeim (1993) calibrate it against polarity epochs 10-7. The regressive events which characterise the Sarmatian suggest that (within the limits of biostratigraphic control) its base can be correlated with the lO.SMa (glacio-eustatic) sea-level low-stand of Haqe/a/. (1988). The Sarmatian of Eastern Paratethys is characterised by areally restricted regressive marginal marine sediments including coarse elastics, and, in the Nakchichevan Depression, evaporites (though transgressive black shales (with source potential) also occur locally). The 'Sarmatian' of Northern Iran and part of the Upper Red Formation of Central Iran, also characterised by elastics and evaporites, appear correlative (Stocklin & Setudehnia, 1971, 1972). The Sarmatian of Eastern Paratethys has been divided into three sub-stages, which are, from oldest to youngest, Volkhynian, Bessarabian and Chersonian. The 'mid' Sarmatian (Bessarabian) represents the culmination of a

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