喜马拉雅造山带东段错那裂谷的地壳结构

doi:10.13745/j.esf.sf.2022.4.66

地学前缘 ›› 2022, Vol. 29 ›› Issue (4): 221-230.DOI: 10.13745/j.esf.sf.2022.4.66

所属专题：印度-欧亚大陆碰撞及其远程效应

• “印度-欧亚大陆碰撞及其远程效应”专栏之五 • 上一篇下一篇

喜马拉雅造山带东段错那裂谷的地壳结构

吴佳杰¹^,²(), 徐啸¹^,²^,^*(), 郭晓玉¹^,², 卢占武³, 吴优¹^,², 向波¹^,², 于洋¹^,², 李春森¹^,², 余嘉豪¹^,², 仝霄飞¹^,², 罗旭聪¹^,²

1.中山大学地球科学与工程学院, 广东珠海 519082
2.南方海洋科学与工程广东省实验室(珠海), 广东珠海 519082
3.中国地质科学院地质研究所, 北京 100037

收稿日期:2022-04-25 修回日期:2022-04-30 出版日期:2022-07-25 发布日期:2022-07-28
通信作者: 徐啸
作者简介:吴佳杰(1995—),男,硕士研究生,主要从事远震接收函数研究。E-mail: wujj68@mail2.sysu.edu.cn
基金资助:
国家自然科学基金项目(41974097);国家自然科学基金项目(41874102);国家自然科学基金项目(U1901214);科学技术部第二次青藏高原综合科学考察研究项目(2019QZKK0701);国家重点研发计划合作研究课题(2016YFC0600301);广东省引进人才创新创业团队“深部地球探测与资源环境团队项目(2017ZT07Z066)

Crustal structure of the Cona rift, eastern Himalaya

WU Jiajie¹^,²(), XU Xiao¹^,²^,^*(), GUO Xiaoyu¹^,², LU Zhanwu³, WU You¹^,², XIANG Bo¹^,², YU Yang¹^,², LI Chunsen¹^,², YU Jiahao¹^,², TONG Xiaofei¹^,², LUO Xucong¹^,²

1. School of Earth Sciences and Engineering, Sun Yat-sen University, Zhuhai 519082, China
2. Southern Marine Science and Engineering Guangdong Laboratory (Zhuhai), Zhuhai 519082, China
3. Institute of Geology, Chinese Academy of Geological Sciences, Beijing, 100037, China

Received:2022-04-25 Revised:2022-04-30 Online:2022-07-25 Published:2022-07-28
Contact: XU Xiao

摘要/Abstract

摘要：

喜马拉雅造山带由印度与欧亚大陆板块的陆陆碰撞而形成。为何在挤压造山的碰撞前缘形成代表垮塌的藏南裂谷系存在巨大的争议。回答这个问题需要对裂谷的地壳结构有一个全面的认识。各裂谷带的起始活动年代自西向东逐渐年轻。本研究选取喜马拉雅东部较为年轻的错那裂谷,利用密集台阵接收的远震数据,通过P波接收函数方法,揭示错那裂谷的精细地壳结构,进而通过地壳结构分析裂谷的形成。结果显示错那裂谷为全地壳尺度结构,裂谷下方莫霍面发生明显错断,且壳内结构侧向不连续发育显著。本研究表明裂谷的形成可能关联更大尺度的区域构造运动,单一的重力垮塌是否能形成地壳尺度的裂谷需要进一步研究。综合前人对藏南裂谷系区域的超钾岩和埃达克岩研究以及深部地球物理观测结果,推断因俯冲的印度板片撕裂导致软流圈物质上涌弱化了错那裂谷区域下地壳,并且结合研究区内喜马拉雅淡色花岗岩研究显示中上地壳也存在弱化现象。因此,结合本研究结果推测全地壳尺度裂谷的形成需要不同深度的地壳弱化。

关键词: 错那裂谷, 短周期密集台阵, 接收函数, 地壳弱化

Abstract:

The Himalayan mountain range is the result of continental-continental collision between the Indian and Eurasian plates. It has been under great debate as to why the rifts of southern Tibet are formed at the front of the collision zone. To answer this question, it is necessary to understand the crustal structure of the rifts. The age of each rift zone tends to be younger from west to east. In this study, we revealed the crustal structure of the Cona rift, a relatively young continental rift, using the P-wave receiver function calculated from teleseismic data received by a dense array across the rift, and analyzed the rift formation process based on the crustal structure. We showed that the Cona rift is a crustal-scale rift, where Moho offsets beneath the rift and significant lateral variations develops. We suggest that the formation of the rifts may be associated with regional tectonic activities, and further studies are needed to ascertain whether a single gravity collapse can form crustal-scale rifts. Based on the previous studies of magmatic rocks and geophysical observations, we infer that the asthenospheric upwelling caused by tearing of the subducting Indian plate weakened the lower crust of the Cona rift region where the middle and upper crust is also weakened as shown by the study of Himalayan leucogranites. Considering all the study results, we hypothesize that the formation of crustal-scale rift requires crustal weakening at different depths.

Key words: Cona rift, short-period dense array, receiver function, crustal weakening

中图分类号:

P315.2

吴佳杰, 徐啸, 郭晓玉, 卢占武, 吴优, 向波, 于洋, 李春森, 余嘉豪, 仝霄飞, 罗旭聪. 喜马拉雅造山带东段错那裂谷的地壳结构[J]. 地学前缘, 2022, 29(4): 221-230.

WU Jiajie, XU Xiao, GUO Xiaoyu, LU Zhanwu, WU You, XIANG Bo, YU Yang, LI Chunsen, YU Jiahao, TONG Xiaofei, LUO Xucong. Crustal structure of the Cona rift, eastern Himalaya[J]. Earth Science Frontiers, 2022, 29(4): 221-230.

图/表 5

图1 青藏高原地质简图(a)及南北向裂谷分布示意图(b)(b据文献[15-16]修改)

Fig.1 (a) Simplified geological map of and (b) distribution of NS-trending rifts (modified after [15-16]) in the Tibetan Plateau

图2 研究区地质构造、台站位置(a)及地震事件分布图(b)(a据文献[8,23]修改)

Fig.2 (a) Topographic map of the study area showing the major tectonic features (modified from [8,23]) and (b) distribution of seismic stations and seismic events in the study area

图3 101号台站的三分量波形示意图 101号台站的滤波后三分量波形。震级M=6.2,震源深度=5 km,震中距=47.09°,方位角=116.78°。三分量由Z、N、E旋转至Z、R、T。

Fig.3 Three-component seismogram for station 101

图4 N-S剖面接收函数叠加结果及偏移成像示意图 a—所有接收函数结果的时间域叠加,未做叠加平滑;b—在图3a结果的基础上做搜索半径6 km的叠加平滑;c—所有接收函数结果在N-S剖面上的偏移成像。STD—藏南拆离系;MHT—主喜马拉雅逆冲断裂。

Fig.4 Receiver function stacking and migration imaging results for N-S profile

图5 N-S剖面解释和研究区岩相转换及裂谷形成模型示意图(c据文献[55,63]修改) a—所有接收函数结果在N-S剖面的偏移成像,其中线条代表地层信息,上覆地形剖面颜色代表不同地质块体;b—研究区淡色花岗岩形成示意图,印度下地壳底部受上涌软流圈作用被加热和弱化,高喜马拉雅熔融发生在俯冲通道的高压变质岩折返和上地壳的减压熔融过程中;c—喜马拉雅中东部高喜马拉雅的混合麻粒岩p-T-t-D变质路径;d—上地壳的熔体迁移和下地壳的弱化导致了坍塌发生,由于高喜马拉雅的折返和地壳的横向伸展,石香肠构造在此处逐渐发育。MHT—主喜马拉雅逆冲断裂;CD—错那洞穹隆;YD—也拉香波穹隆。

Fig.5 (a) N-S profile interpretation, (b) metamorphic p-T-t-D paths in the study area and (c,d) rift formation models.c modified after [55,63].

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喜马拉雅造山带东段错那裂谷的地壳结构

Crustal structure of the Cona rift, eastern Himalaya

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