北山-阿拉善晚新生代变形的特征与机制

doi:10.13745/j.esf.sf.2023.8.16

地学前缘 ›› 2023, Vol. 30 ›› Issue (5): 334-357.DOI: 10.13745/j.esf.sf.2023.8.16

• “印度欧亚大陆碰撞及其远程效应”专栏之九 • 上一篇下一篇

北山-阿拉善晚新生代变形的特征与机制

张进¹^,²(), 张北航³, 赵衡¹^,², 云龙⁴, 曲军峰², 王振义², 杨亚琦⁵, 赵硕²

1.自然资源部深地科学与探测技术实验室, 北京 100037
2.中国地质科学院地质研究所, 北京 100037
3.中国科学院西北生态环境资源研究院, 甘肃兰州 730000
4.核工业北京地质研究院, 北京 100029
5.贵州大学资源与环境工程学院喀斯特地质资源与环境教育部重点实验室, 贵州贵阳 550025

收稿日期:2023-08-01 修回日期:2023-08-16 出版日期:2023-09-25 发布日期:2023-10-20
作者简介:张进(1973—),男,研究员,博士生导师,主要从事构造地质学研究。E-mail: zhangjinem@sina.com
基金资助:
中国地质调查局三级项目(DD20230217);中国地质调查局三级项目(DD20221646);国家自然科学基金项目(41972224);中国地质科学院基本科研业务费专项(JKYZD202309)

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

ZHANG Jin¹^,²(), ZHANG Beihang³, ZHAO Heng¹^,², YUN Long⁴, QU Junfeng², WANG Zhenyi², YANG Yaqi⁵, ZHAO Shuo²

1. MNR Laboratory of Deep Earth Sciences and Technology, Beijing 100037, China
2. Institute of Geology, Chinese Academy of Geological Sciences, Beijing 100037, China
3. Northwest Institute of Eco-Environment and Resources, Chinese Academy of Sciences, Lanzhou 730000, China
4. Beijing Research Institute of Uranium Geology, Beijing 100029, China
5. MOE Key Laboratory of Karst Georesources and Environment, College of Resources and Environmental Engineering, Guizhou University, Guiyang 550025, China

Received:2023-08-01 Revised:2023-08-16 Online:2023-09-25 Published:2023-10-20

摘要/Abstract

摘要：

北山-阿拉善地区位于中亚造山带中部,新生代晚期受控于印度-欧亚板块的碰撞,发生了不同程度的陆内变形,是青藏高原与蒙古高原应力传递区,是研究印度-欧亚碰撞远程效应的关键地区。北山-阿拉善地区晚新生代变形区别于中亚造山带西段的天山以及阿尔泰地区,表现为发育一系列近东西向的左行走滑断层及其间一系列北东向的正断层及其控制的断陷(拉分)盆地。近东西向的左行走滑断层规模较大,走向延伸很长,成为北山-阿拉善新生代晚期变形的骨干构造。整体上北山-阿拉善地区之间的晚新生代变形是在北侧北东东向南蒙古—天山左行走滑断层和南侧北东东向阿尔金断层之间阶区内的变形,在这个左行-左阶的区域内,变形表现为边界走滑断层派生出的近东西向次级走滑断层(P剪切)和北东向伸展盆地(如额济纳盆地和旧井盆地)。该区域是一个左行张剪区域,使得该区成为区别于蒙古戈壁阿尔泰的右行压剪构造,而阶区内区域性的伸展导致了本区平坦的地势并成为主要的汇水盆地区。GPS速度场以及上地幔-下地壳各向异性资料表明,塔里木克拉通在青藏高原向北的扩展过程中起重要作用,青藏高原北缘上地幔-下地壳在遇到塔里木克拉通后沿着该克拉通东南边缘转向,向北东流动,而塔里木本身则继续向北北东传递应力,导致天山的崛起并挤压准噶尔盆地,进而形成了阿尔泰山北北西走向的右行剪切变形;向北东方向流动的上地幔—下地壳则导致北山-阿拉善地区以及南蒙古地区的晚新生代左行剪切变形,该地区的变形宏观上呈现弥散性特点,区别于塔里木-天山-准噶尔地区新生代变形集中天山和阿尔泰山一带的现象。

关键词: 北山-阿拉善, 晚新生代, 青藏高原, 陆内变形, 变形机制

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

中图分类号:

P542

张进, 张北航, 赵衡, 云龙, 曲军峰, 王振义, 杨亚琦, 赵硕. 北山-阿拉善晚新生代变形的特征与机制[J]. 地学前缘, 2023, 30(5): 334-357.

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.

图/表 18

图1 南蒙古—青藏高原北侧活动构造(A)与地震分布(B)(活动断层分布和名称据文献[22⇓-24]) BDFS—Bogd断层系;TBFS—Töv-Bogd断层系;SMTFS—南蒙古-天山断层系;NTHF—吐哈盆地北缘断层;XDF—兴地断层;BAF—博罗科努—阿奇克库都克断层;QMF—且末断层;SWSF—三危山断层;JTNSF—金塔南山断层;MSLF—慕少梁断层;BDSF—北大山断层;TAYF—桃花拉山—阿右旗—雅布赖断层;XTF—香山—天景山断层; EHLF—贺兰山东麓断层;NESF—鄂尔多斯北缘断裂;LSDF—狼山—色尔腾山—大青山断层;NQLFS—北祁连断层系;NQDF—柴达木北缘断层;EKLF—东昆仑断层。

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

图2 北山-阿拉善地区晚新生代断层分布

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

图3 旧井盆地山前正断层地貌

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

图4 旧井盆地东缘山前活动正断层 A,B—前人开挖探槽;C—断层面上的斜滑擦痕;D—旧井盆地基底花岗糜棱岩。

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

图5 北山南部东涧泉—旧井地质图

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

图6 鄂博庙断层地质图

Fig.6 Geological map of the Ebomiao fault zone

图7 鄂博庙断层特征 A—地表断层陡坎;B—ETC-03探槽西壁局部;C—ETC-03探槽西壁解释。U1—灰白、灰黄色砂砾石层;U2—棕黄色砂砾石层;U3-1—U2层顶部白色钙质淋滤结核;U3-2—棕黄色砂砾石层;U4—深棕黄色粗砂砾石层;U5—棕黄色砂砾石层,水平层理;U6—灰黄色砂砾石层,水平层理发育;U7-1—细砂层;U7-2—灰黄色砂砾石层,水平层理;U8—棕黄色砂层,局部夹杂砾石。

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

图8 北山南部柳园地区晚新生代构造

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

图9 北山柳园地区晚新生代构造 A,B—柳园东部北东向左行压剪断层;C—地表滚落的巨石;D—地表基岩断层陡坎;E—断层山前散布的滚石。

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

图10 北山中部马鬃山(山前为逆冲断层) A,B—马鬃山南侧远景;C—马鬃山剪切带强烈剪切变形的晚古生代花岗岩;D—马鬃山剪切带内强烈发育的糜棱岩面理。

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

图11 白山泉—明水活动断层(无人机照片) A—断层西段地表断层迹线;B—断层西段沿断层的一系列左行错动的冲沟;C—断层中部断层陡坎(泉水出露);D—断层东段陡坎及左行位错的冲沟。

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

图12 白山泉—明水活动断层 A—断层中部左行走滑位移的冲沟;B—断层东段反向陡坎;C—断层西段断层陡坎;D—断层东段反向陡坎变形的上新统苦泉组砂砾岩。

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

图13 阿拉善地区晚新生代构造分布

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

图14 额济纳盆地晚新生代构造分布(断层根据文献[22])

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

图15 航天城断层 A,B—断层中段断层陡坎;C—断层东端陡坎和前人开挖探槽;D—断层西段出露断层泉与断层陡坎。

Fig.15 Landform in the Hangtiancheng fault zone

图16 北山-阿拉善地区活动断层分布图

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

图17 同性质走滑断层控制下形成的拉分盆地(据文献[102]修改)

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

图18 南蒙古—青藏高原北侧变形机制 (青藏地区上地幔/下地壳各向异性数据来自文献[115,123⇓⇓⇓⇓⇓⇓⇓⇓⇓-133];阿尔金断层两侧数据来自文献[115,134];天山地区数据来自文献[135⇓⇓-138];蒙古地区数据来自文献[109,139⇓⇓⇓-143])

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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北山-阿拉善晚新生代变形的特征与机制

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

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