West Siberian sedimentary basin. Crustal subsidence caused by rock contraction in its lower part due to prograde metamorphism

Мұқаба

Дәйексөз келтіру

Толық мәтін

Ашық рұқсат Ашық рұқсат
Рұқсат жабық Рұқсат берілді
Рұқсат жабық Рұқсат ақылы немесе тек жазылушылар үшін

Аннотация

The history of the crustal subsidence in the Mesozoic and Cenozoic in the West Siberian Basin – the largest sedimentary basin in the world – is considered. Most researchers associate its formation with post-rift subsidence of the crust, which followed an episode of strong lithospheric stretching about 250 million years ago near to the Permian to the Triassic transition. A characteristic feature of post-rift subsidence is a decrease in its rate in time. During the Mesozoic-Cenozoic history, in Western Siberia the rate of crustal subsidence should have slow down by an order of magnitude. However, the analysis of long (700–900 km) seismic profiles in the north of Western Siberia and in the Southern Kara Sea shows that since the beginning of the Mesozoic in these regions, on average, there has been an acceleration of the crustal subsidence. Under such circumstances, lithospheric stretching in them could be responsible for only a small part of the total subsidence of the crust of 6–7 km. In Western Siberia, the Earth’s crust is close to the isostatic equilibrium. Then, in the absence of strong stretching, the accumulation of thick sedimentary sequences in the basin could only have been caused by rock contraction in the lower crust due to prograde metamorphic reactions. To obtain the above results, we used, for the first time, some simple methods to analyze the structure of the sedimentary cover in the West Siberian Basin. Detailed seismic profiles have been published for many other deep basins on all the continents. The methods of their interpretation implemented in this paper can be easily applied to determine the role of lithospheric stretching in the formation of deep sedimentary basins on the global scale.

Толық мәтін

Рұқсат жабық

Авторлар туралы

E. Artyushkov

Institute of Physics of the Earth, Russian Academy of Sciences

Хат алмасуға жауапты Автор.
Email: arty-evgenij@yandex.ru

Academician of the RAS

Ресей, Moscow

P. Chekhovich

Institute of Physics of the Earth, Russian Academy of Sciences; Moscow State University

Email: p.chekhovich@gmail.com

Музей землеведения

Ресей, Moscow; Moscow

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Әрекет
1. JATS XML
Жүктеу
2. 1. The location of ultra-deep wells and seismogeological profiles in the structure of the West Siberian basin. The colored fill shows the rift system in the Paleozoic folded basement ([11], with changes), the dotted line shows the boundaries of the sedimentary basin.

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3. Fig. 2. Seismogeological section according to regional profile No. 26 ([7, 9] – with changes). (a) – the most important geometric parameters of the section; the colored arrows show the precipitation levels that compensated for the expected post-drift dive at stage T2-J1 and the actual dive that occurred at stage J2-KZ. The vertical axis shows the propagation time of elastic waves in the forward and reverse directions in milliseconds. (b and c) are fragments of the section, which show shifts in the depth of the base of the Triassic terrigenous deposits and boundaries in the Paleozoic complex. The yellow arrows mark the places where the reflecting horizons are not broken by discontinuities. 1 is the reflecting boundary in the Paleozoic megacomplex (P), 2 is the base of the Terrigenous Triassic (reflecting horizon A), 3 is the reflecting horizons in the Jurassic seismogeological megacomplex (sole Ia and roof C of the Lower Jurassic), 4 is the base of the Neocomian megacomplex (roof of the Bazhenov formation), the base and roof of the Aptian-Albian-Cenomanian megacomplex, 5 – the base of the Cenozoic megacomplex, 6 – discontinuous disturbances: a – without displacement of the reflecting boundaries, b – the same with displacements, 7 – amplitudes of the vertical displacement of the reflectors at the discontinuities (milliseconds).

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4. Fig. 3. Stretching of the reflector in the sedimentary cover or on the surface of the foundation caused by the formation of a discharge.

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5. Fig. 4. Seismogeological section along the Kara Sea–Yamal profile ([8, 9] with changes). The colored arrows show the thickness of sediments (milliseconds) accumulated at various stages of the dive – Δt1 (post–drift dive, Triassic - Middle Jurassic) and Δt2 (Late Jurassic – Early Oligocene). (1-8) reflecting horizons: 1 – in the basement roof, 2 – in the Paleozoic complex, 3 – in the base of the Terrigenous Triassic (A1), 4 – in the base of the Middle Triassic, 5 – in the base of the Jurassic, 6 – near the roof of the Middle Jurassic (C1), 7 – in the base of the Neocomian, Aptian-Albian-Cenomanian and Turonian-Maastrichtian complexes, 8 – in the base of the Cenozoic complex, 9 – amplitudes of the largest displacements in the base of the Mesozoic-Cenozoic sedimentary cover, 10 – ruptures.

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6. Fig. 5. Seismogeological section along the Kara Sea–Gydan profile ([8] with changes). The colored arrows show the thickness of sediments (milliseconds) accumulated at various stages of the dive; reflecting horizons (1-7): 1 – in the basement roof, 2 – in the Paleozoic complex, 3 – in the base of the Terrigenous Triassic (A1), 4 – in the base of the Middle Triassic, 5 – in the base of the Jurassic (a) and near roofs of the Middle Jurassic C1 (b), 6 – in the base of the Neocomian, Aptian-Albian-Cenomanian and Turonian-Maastrichtian complexes, 7 – in the base of the Cenozoic complex, 8 – ruptures.

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7. 6. The structure of the upper part of the lithospheric layer of the deep sedimentary basin. 1 – sedimentary strata; 2 – the upper part of the consolidated crust (the basement of the basin); 3 – the lower part of the consolidated crust, which has experienced high-grade metamorphism with a significant increase in rock density (eclogite); 4 – the mantle in the lithospheric layer; 5 – the position of the Moho section, determined by seismic data; 6 – the interface between rocks the Earth's crust and mantle peridotites.

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