Abstract
The Mongol-Okhotsk orogenic belt, finally formed in the end of the Mesozoic as a result of later tectonic events, is divided into two flanks: western and eastern. Its formation is obviously due to a regular change in geodynamic events significantly obscured by late tectonic and magmatic processes in the western flank and more clearly defined in the eastern flank from both magmatic and stratified formations. The early changes in geodynamic environment are most clearly determined by the formation of magmatic complexes whose completion is usually accompanied by the strata formation. Stratons framing the eastern flank of the Mongol-Okhotsk orogenic belt in the Mesozoic were formed in sedimentary basins, which are currently isolated to the Krestovkinsky and Ogodzhinsky basins along the southern border and to the Strelkinsky, Malotyndinsky, Toromsky and Udsky basins along the northern border. The deposition environment varied from deep-sea marine to continental. The article attempts to correlate the cross-sections of sedimentary basins on the framing of the eastern Mongol-Okhotsk orogenic belt and considers similarity or difference in their structure, conditions of sedimentation, tectonic positions and dependence of their evolution on geodynamic processes in the region
Highlights
The early changes in geodynamic environment are most clearly determined by the formation of magmatic complexes whose completion is usually accompanied by the strata for mation
Stratons framing the eastern flank of the Mongol-Okhotsk orogenic belt in the Mesozoic were formed in sedimen tary basins, which are currently isolated to the Krestovkinsky and Ogodzhinsky basins along the southern border and to the Strelkinsky, Malotyndinsky, Toromsky and Udsky basins along the northern border
The article attempts to correlate the cross-sections of sedimentary basins on the framing of the eastern Mongol-Okhotsk orogenic belt and considers similarity or difference in their structure, conditions of sedimentation, tectonic positions and dependence of their evolution on geodynamic processes in the region
Summary
Воз раст свиты по этим остаткам определяется неоднознач но: как поздняя юра – готерив [Geological Map..., 2001] или готерив – апт [State Geological Map..., 2009]. Установлено, что конец юры в регионе ознаменовал ся магматической деятельностью, связанной с субдук ционными процессами [Derbeko, Chugaev, 2020] и, соот ветственно, орогенезом в пределах Монголо-Охотского бассейна (МОБ). Сопровождающие ее вулканические комплексы проявились только в ин тервале 145–138 млн лет и более интенсивно – в пост готеривское время [Derbeko, 2012], поэтому отсутствие туфового материала в осадках крестовкинской сви ты позволяет отнести нижнюю возрастную границу как минимум к концу берриаса, а весь цикл осадкона копления крестовкинской свиты к берриас – готериву БЦС не принимал участия в эволюции МООП, а аккретиро вал к нему в постмезозойское время, после заверше ния всех магматических событий на его территории [Derbeko, 2013, 2018].
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