Maxim V. Korotaev
Moscow State University
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Tectonophysics | 1996
A.M. Nikishin; Peter A. Ziegler; Randell Stephenson; Sierd Cloetingh; A.V. Furne; P.A. Fokin; A.V. Ershov; S.N. Bolotov; Maxim V. Korotaev; A. S. Alekseev; V.I. Gorbachev; E.V. Shipilov; Anco Lankreijer; E.Yu. Bembinova; I. Shalimov
Abstract During its Riphean to Palaeozoic evolution, the East European Craton was affected by rift phases during Early, Middle and Late Riphean, early Vendian, early Palaeozoic, Early Devonian and Middle-Late Devonian times and again at the transition from the Carboniferous to the Permian and the Permian to the Triassic. These main rifting cycles were separated by phases of intraplate compressional tectonics at the transition from the Early to the Middle Riphean, the Middle to the Late Riphean, the Late Riphean to the Vendian, during the mid-Early Cambrian, at the transition from the Cambrian to the Ordovician, the Silurian to the Early Devonian, the Early to the Middle Devonian, the Carboniferous to Permian and the Triassic to the Jurassic. Main rift cycles are dynamically related to the separation of continental terranes from the margins of the East European Craton and the opening of Atlantic-type palaeo-oceans and/or back-arc basins. Phases of intraplate compression, causing inversion of extensional basins, coincide with the development of collisional belts along the margins of the East European Craton. The origin and evolution of sedimentary basins on the East European Craton was governed by repeatedly changing regional stress fields. Periods of stress field changes coincide with changes in the drift direction, velocity and rotation of the East European plate and its interaction with adjacent plates. Intraplate magmatism was controlled by changes in stress fields and by mantle hot-spot activity. Geodynamically speaking, different types of magmatism occurred simultaneously.
Sedimentary Geology | 2003
Marie-Françoise Brunet; Maxim V. Korotaev; Andrei V. Ershov; A.M. Nikishin
Abstract The basement surface of the South Caspian depression lies at a depth of 20–25 km, making it one of the deepest basins in the world. It occupies the southern, deep-water, part of the Caspian Sea and two adjacent lowlands: the West Turkmenia in the east and the Lower Kura in the west. The basin can be subdivided into several sub-basins with two main depocentres, one in the northern part of the basin, just on the southern flank of the Apsheron Sill, and one, called the Pre-Alborz trough, located in the south-eastern part of the marine basin. The sedimentary fill of the South Caspian Basin has been significantly deformed. Part of it is allochthonous and folded, overlying a ductile detachment zone within the Maikop shale (Oligocene–Early Miocene). The folded succession is unconformably overlain by Upper Pliocene–Quaternary neo-autochthonous sediments. An intense shortening event, related to the NNE–SSW convergence of the Arabian plate with Eurasia, affected the region during the Pliocene–Pleistocene. The thickness of Pliocene–Quaternary sediments alone reaches 10 km. They were deposited in a rapidly subsiding basin and were sourced from the surrounding Caucasus, Alborz, and Kopet-Dagh orogens as well as from the nearby Russian Platform. The thickness of the crust beneath the western central part of the basin is as little as 8 km in the western central part of the basin but exceeds 15 km in the eastern part. Geophysical data and gravimetric modelling provide evidence that the basement of the marine part of the basin comprises a high-velocity, thin complex crust. Subsidence of the basin is in part due to profound thinning of continental crustal or, more likely, to the formation of oceanic crust. This took place in Middle–Late Jurassic times, in the context of back-arc basin development, with possible reactivation during the Cretaceous. However, there remains controversy regarding the timing of oceanic accretion and deep-water deposition in the South Caspian Basin. The present results are based on subsidence analysis complemented by geological data from tectonic units surrounding the South Caspian Basin and on its margins. An additional mechanism, nevertheless, must be invoked to explain the younger, much more rapid Pliocene–Quaternary phase of subsidence that occurred simultaneously with the subsidence of Caucasus-related molasse basins and the uplift and erosion of the Caucasus Orogen. This rapid subsidence phase is probably of compressional origin and a simple elastic model in compression provides comparable amplitudes of subsidence. In addition, the South Caspian Basin is surrounded by orogenically loaded crust that adds to basin downwarping. To the north, the basin is bounded by a subduction zone.
Sedimentary Geology | 2003
A.M. Nikishin; Maxim V. Korotaev; A.V. Ershov; Marie-Françoise Brunet
Abstract The Black Sea basin originated as a back-arc basin during Cretaceous times. Continental rifting took place during the Aptian to Albian with large-scale crustal thinning and separation occurring since the Cenomanian, mainly along a former Albian volcanic arc. Both western and eastern Black Sea basins opened almost simultaneously during Cenomanian to Coniacian times. However, during the Santonian to Palaeocene, the Black Sea region was affected by compressional deformation. Apart from a tensional event that took place in eastern part of the region during the Eocene, deepening of the basin has been induced by compressional deformation from latest Eocene to recent times. Kinematic and dynamic modelling of the subsidence history of the Black Sea basin shows that downward bending of the lithosphere beneath the basin due to compressional deformation could be the cause of this rapid additional subsidence.
Sedimentary Geology | 2003
A.V. Ershov; Marie-Françoise Brunet; A.M. Nikishin; S.N. Bolotov; B.P. Nazarevich; Maxim V. Korotaev
Abstract Burial histories of the eastern, central and western parts of the Northern Caucasus basin are reconstructed on the basis of well data and seismic sections. Subsidence began in the Early Triassic after the Late Carboniferous–Permian orogeny. Triassic sediments were mainly removed during Late Triassic–Early Jurassic uplift and erosion. Platform cover began to form in the Middle Jurassic and Albian sediments covered the whole territory of the basin. Thermal modelling shows that Jurassic–Eocene subsidence was mainly controlled by Late Triassic–Early Jurassic intrusive warming. This heating event induced thermal uplift of the whole territory followed by exponentially decelerating subsidence due to cooling of the lithosphere. In the southern areas adjacent to Great Caucasus, subsidence was also affected by Caucasian extensional and compressional events. In the Oligocene–Early Miocene, the eastern and the central basins underwent rapid long wavelength subsidence (Maikopian subsidence). The geodynamic cause of this subsidence is probably associated with the mantle flow appearance after cessation of the Tethyan subduction, due to reequilibration of subducted slab. While in the Late Miocene–Quaternary times, the eastern and the western basins underwent foreland-type asymmetrical subsidence due to loading of the Great Caucasus orogen; the central basin was uplifted. According to flexural modelling, the main component of orogen loading was the lithospheric root load; delamination of the latter under the Central Caucasus caused rapid uplift of the orogen and adjacent basin.
Geological Society, London, Special Publications | 2017
Marie-Françoise Brunet; A.V. Ershov; Maxim V. Korotaev; Vladislav N. Melikhov; Eric Barrier; Dmitriy O. Mordvintsev; Irina Sidorova
Abstract The Amu Darya Basin (ADB) has been studied primarily for its important hydrocarbon reserves and to a lesser extent for its geodynamic evolution. The ADB is located on the SE portion of the Turan Platform, between the sutures of the Turkestan and Palaeo-Tethys oceans, which closed during the Late Palaeozoic and Early Mesozoic, respectively. Blocks and island arcs accreted to Eurasia during the Palaeozoic form a poorly defined, heterogeneous basement underlying the ADB. They played an important role in shaping its composite structure into variously orientated sub-basins and highs. In this paper, depth–structure and isopach maps, and regional cross-sections, are analysed to unravel the location and origin of the main structural elements and to characterize the subsidence evolution of the ADB. The main tectonic events leading to the formation and evolution of the ADB took place: (1) in the Late Palaeozoic–Early Triassic (back-arc, rollback and extension/strike-slip); (2) from the Middle Triassic to the Triassic–Jurassic boundary (Eo-Cimmerian collision of Gondwana-derived continental blocks with Eurasia); and (3) during the Early–Middle Jurassic (post-collision extensional event). The last part of this evolution reflects shortening and flexure due to Cenozoic collisions to the south. Palaeotectonic maps are used to relate these events to the geodynamics of the Tethyan domain.
Mémoires du Muséum national d'histoire naturelle | 2001
A.M. Nikishin; Peter A. Ziegler; Dmitry I. Panov; B.P. Nazarevich; Marie-Françoise Brunet; Randell Stephenson; S.N. Bolotov; Maxim V. Korotaev; Petr L. Tikhomirov
Tectonophysics | 1999
Andrei V. Ershov; M.F. Brunet; Maxim V. Korotaev; A.M. Nikishin; Sergei N. Bolotov
Sedimentary Geology | 2003
A.M. Nikishin; Maxim V. Korotaev; A.V. Ershov; Marie-Françoise Brunet
Peri-Tethys Memoir 4, Epicratonic Basins of Peri-Tethyan Platforms, Memoires du Museum national d'Histoire naturelle | 1998
A.V. Ershov; M.F. Brunet; A.M. Nikishin; S.N. Bolotov; Maxim V. Korotaev; S.S. Kosova
Archive | 2007
Marie-Franoise Brunet; Andrei V. Ershov; Yury A. Volozh; Maxim V. Korotaev; Mikhail P. Antipov; Jean-Paul Cadet