Late Cenozoic deformation characteristics and mechanism of the Beishan-Alxa region

doi:10.13745/j.esf.sf.2023.8.16

Abstract

Abstract:

The Beishan-Alxa region is located in the middle segment of the Central Asian Orogenic Belt. This region, controlled by the Indian-Eurasian collision in the Late Cenozoic, has undergone intracontinental deformation to varying degrees. It is a stress transfer area between the Qinghai-Tibetan Plateau and the Mongolian Plateau, and a key area to study the remote effects of the Indian-Eurasian collision. Differing from the Late Cenozoic deformation in the Tianshan/Altai regions in the western segment of the Central Asian Orogenic Belt, the Beishan-Alxa region developed a set of near EW-trending left-lateral strike-slip faults, and between them a series of NE-trending normal faults were developed which control faulted depression (pull-apart) basins. The much larger near EW-trending faults, with a long strike extension, become the main structure of Late Cenozoic deformation in this region. On the whole, the deformation is in the step area between the NEE-trending South Mongolian-Tianshan left-lateral strike-slip fault on the north side, and the NEE-trending Altyn Tagh fault on the south side. In this left-lateral left-step area, the deformation is manifested as nearly E-W secondary strike slip faults (P shear), derived from the boundary strike-slip faults and the NE extensional basins (such as the Ejina basin, Jiujing basin). Under sinistral transtensional setting this area develops a sinistral shear structure distinct from the dextral shear structure of the Mongolian Gobi Altai; while its flat landform, developed under regional extension within the step area, makes it the main catchment basin area in the Beishan-Alxa region. The GPS velocity field and anisotropy data of the upper mantle-lower crust indicate the Tarim Craton plays an important role in the northward expansion of the Qinghai-Tibetan Plateau. At the Tarim Craton the upper mantle-lower crust of the Qinghai-Tibetan Plateau turns northeastward along the southeastern edge of the craton while the Tarim continues to exert stress northeastward, leading to the rise of the Tianshan mountain range and northward compression of the Junggar Basin to cause NNW-trending dextral shear deformation in the Altay Mountains. On the other hand, the northward movement of the upper mantle-lower crust causes Late Cenozoic sinistral shear deformation in the Beishan-Alxa region and southern Mongolia. Deformation in the Beishan-Alxa region is widespread, which is different from Cenozoic deformation in the Tarim-Tianshan-Junggar region where deformation is concentrated in the Tianshan and Altay Mountains.

Key words: Beishan-Alxa, Late Cenozoic, Qinghai-Tibetan Plateau, intracontinental deformation, deformation mechanism

CLC Number:

P542

ZHANG Jin, ZHANG Beihang, ZHAO Heng, YUN Long, QU Junfeng, WANG Zhenyi, YANG Yaqi, ZHAO Shuo. Late Cenozoic deformation characteristics and mechanism of the Beishan-Alxa region[J]. Earth Science Frontiers, 2023, 30(5): 334-357.

Figures/Tables 18

Fig.1 Active faults (A) and earthquakes (B) in the southern Mongolia and northern Qinghai-Tibetan Plateau regions. Modified from [22⇓-24].

Fig.2 Late Cenozoic faults in the Beishan-Alxa region

Fig.3 Typical landforms formed by active normal faults along the eastern boundary of the Jiujing basin

Fig.4 Active normal faults along the eastern boundary of the Jiujing basin

Fig.5 Geological map of Dongjianquan-Jiujing region, southern Beishan

Fig.6 Geological map of the Ebomiao fault zone

Fig.7 Landform and structural characteristics of the Ebmiao fault zone

Fig.8 Late Cenozoic structural features in Liuyuan, southern Beishan

Fig.9 Late Cenozoic geomorphic features in Liuyuan, southern Beishan

Fig.10 Mazongshan in the central Beishan (the front fault of Mazongshan range is a thrust fault)

Fig.11 Aerial veiw of the Baishanquan-Mingshui active fault (drone photos)

Fig.12 Field photos of the Baishanquan-Mingshui active fault

Fig.13 Distribution of Late Cenozoic faults in the Alxa region

Fig.14 Distribution of Late Cenozoic structures in the Ejina basin. Modified from [22].

Fig.15 Landform in the Hangtiancheng fault zone

Fig.16 Distribution of active faults in the Beishan-Alxa region

Fig.17 Pull-apart basins in the overstep region between two strike-slip faults with the same kinematics. Modified after [102].

Fig.18 A deformation model for the northern Tibetan Plateau-southern Mongolia region (Tibetan Plateau anisotropy data of upper mantle/lower crust from [115,123⇓⇓⇓⇓⇓⇓⇓⇓⇓-133]; Altyn Tagh Fault data from [115,134]; Tianshan data from [135⇓⇓-138]; Mongolia data from [109,139⇓⇓⇓-143])

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