青藏高原新生代南北走向裂谷研究进展

doi:10.11867/j.issn.1001-8166.2020.064

地球科学进展 ›› 2020, Vol. 35 ›› Issue (8): 848 -862. doi: 10.11867/j.issn.1001-8166.2020.064

青藏高原新生代南北走向裂谷研究进展

张佳伟 ¹(

),李汉敖 ²,张会平 ¹,徐心悦 ¹

^1.中国地震局地质研究所地震动力学国家重点实验室，北京 100029
^2.中国地质大学（北京）生物地质与环境地质国家重点实验室，北京 100083

收稿日期:2020-05-28 修回日期:2020-07-20 出版日期:2020-08-10
基金资助:
第二次青藏高原综合科学考察研究项目“碰撞以来古地理格局与构造地貌过程”(2019QZKK0704);国家自然科学基金项目“西藏冈底斯山弧高海拔古地貌开始形成时间”(41902121)

Research Progress in Cenozoic N-S Striking Rifts in Tibetan Plateau

Jiawei Zhang ¹( ),Han'ao Li ²,Huiping Zhang ¹,Xinyue Xu ¹

^1.State Key Laboratory of Earthquake Dynamics，Institute of Geology，China Earthquake Administration，Beijing 100029，China
^2.State Key Laboratory of Biogeology and Environmental Geology，China University of Geosciences (Beijing)，Beijing 100083，China

Received:2020-05-28 Revised:2020-07-20 Online:2020-08-10 Published:2020-09-15
About author:Zhang Jiawei (1990-), male, Yantai County, Shandong Province, Postdoctoral fellow. Research areas include basin research and low-temperature thermochronology. E-mail: jiawei@ies.ac.cn
Supported by:
Projected supported by the Second Tibetan Plateau Scientific Expedition and Research program “Paleogeography and geomorphology process since the collision”(2019QZKK0704);The National Natural Science Foundation of China “Age constraints on the onset of high-altitude paleogeomorphology of the Gangdese Mountain, Tibet”(41902121)

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青藏高原新生代南北走向裂谷的形成是印度—欧亚大陆碰撞后持续挤压造山的重要产物，其形成和演化对于理解青藏高原的生长具有重要意义。近年来，运用地质年代学、构造地质学、岩石地球化学和地球物理探测等手段对南北走向裂谷的启动时间、形成机制和演化过程进行了深入研究，但对于青藏高原南北走向裂谷的认识仍难以达成共识。对近年来青藏高原南北走向裂谷的拉张时间、形成机制及其与高原深部圈层的关系等方面的研究现状和存在问题进行了综述：南北走向裂谷主要拉张时期为中新世；其成因复杂，不同时期可能受控于不同机制；南北走向裂谷与高原内部钾质、超钾质岩具有密切成因联系，其分布特征可能受高导低速体影响。基于现有认识，更精确的年代学约束、深部过程探测以及数值模拟是今后南北走向裂谷研究的发展趋势。

关键词: 南北走向裂谷, 高原隆升, 启动时间, 深部动力学

The formation of the Cenozoic N-S striking rifts in the Tibetan Plateau is the consequence of continuous contraction after the India-Asia collision. Its formation and evolution are of great significance for understanding the growth of the Tibetan Plateau. In recent years, geochronology, structural geology, geochemistry and geophysical exploration have been used to study the onset timing, mechanism and evolution process of the N-S striking rifts, and the N-S striking rifts are related to the deep dynamics in Tibet. However, it is still difficult to reach a consensus on the understanding of the N-S striking rifts in the Tibetan Plateau. This paper summarized the research status and existing problems on the onset timing, mechanism and their relationship with the deep layer of the plateau: the main extension period of the N-S striking rifts is Miocene; mechanisms controlling its formation are complex and may be various in different periods; the N-S striking rifts have a close genetic relationship with potassium and ultrapotassic rocks in the plateau, and their distribution may be affected by high-conductivity and low-velocity bodies. Based on existing knowledge, more precise geochronological constraints, deep process detection, and numerical modeling will be the future development trends in the study of N-S striking rifts.

Key words: N-S Striking Rifts, Uplift of Plateau, Onset timing, Deep Dynamics.

中图分类号:

P542+.31

图1 青藏高原南北走向裂谷分布、初始拉张时间及主要构造活动速率（据参考文献[ 6 , 7 ]修改）
黑色圆数字代表南北走向裂谷编号，1：Leo Pargil，2：Gular Mandhata，3：隆格尔，4：Thakkola，5：当惹雍错—孔错，6：申扎—定结，7：亚东—谷露，8：沃卡—错那，9：双湖；编号旁红色斜体数字（单位：Ma）代表裂谷初始拉张时间；蓝色数字代表主要构造活动速率（单位：mm/a） ^{[

8
,

9
]}

Fig.1 Distribution, onset timing of N-S striking rifts and slip rates of main structures in Tibet (modified after references [6,7])
The black round numbers represent N-S striking rifts， 1: Leo Pargil， 2: Gular Mandhata， 3: Lunggar， 4: Thakkola， 5: Tangra Yum Co-Kong Co， 6: Xainza-Dinggye， 7: Yadong-Gulu， 8: Woka-Cuona， 9: Shuanghu; The red italic numbers in Ma next to these numbers represent onset timing of E-W extension； Blue numbers represent slip rates of main structures (unit:mm/a） ^{[

8
,

9
]}

表1 青藏高原南北走向裂谷初始拉张时间

Table 1 Onset timing of N-S striking rifts in Tibet

裂谷名称		拉张时间/Ma	测年方法	流变学特征	活动速率/ (mm/a)	参考文献
羌塘地体	双湖	13.5 4	⁴⁰Ar/³⁹Ar 地形剖面	脆性	-	[ 44 ] [ 45 ]
羌塘地体	与东西向伸展相关的埃达克岩	47~38	U-Pb，同位素地球化学	岩脉	-	[ 41 , 46 , 47 , 48 ]
拉萨地体	隆格尔	>10	(U-Th)/He	韧性	4.0~5.0^{[ 49 ]}	[ 50 ]
	打加错	18.3	U-Pb	岩脉	-	[ 39 ]
	当惹雍错	约13 14.5	(U-Th)/He (U-Th)/He, AFT	脆性	0.3~0.7^{[ 34 ]} 4.0~5.0^{[ 49 ]}	[ 51 ] [ 34 ]
	申扎	约14	U-Pb	脆性	1.0~2.0^{[ 49 ]}	[ 52 ]
	念青唐古拉	11~5 8	⁴⁰Ar-³⁹Ar Th-Pb	韧性—脆性	4.0^{[ 24 ]}	[ 27 ] [ 24 ]
	谷露	7	(U-Th)/He	脆性	4.0~5.0^{[ 49 ]}	[ 53 ]
喜马拉雅	Leo Pargil	16.9~14.5	⁴⁰Ar/³⁹Ar	韧性	-	[ 54 , 55 ]
	Gular Mandhata	15~9	⁴⁰Ar/³⁹Ar	韧性	-	[ 56 ]
	Thakkola	11~10	磁性地层	-	-	[ 57 ]
	孔错	19 13~12 4	U-Pb (U-Th)/He U-Pb, Ar/Ar, (U-Th)/He	韧性—脆性	-	[ 40 ] [ 58 ] [ 59 ]
	Ama Drime Massif	13	Th-Pb	韧性—脆性	0.6~1.7^{[ 60 ]}	[ 53 ]
		4	(U-Th)/He			[ 61 ]
		11	P-T-D-t			[ 62 ]
	亚东	<10	Th-Pb	-	1.4^{[ 11 ]}	[ 63 ]
	亚东	5	⁴⁰Ar/³⁹Ar	脆性	1.4^{[ 11 ]}	[ 64 ]
	错那	<12	K/Ar	-	0.6~1.7^{[ 65 ]}	[ 66 ]

表1 青藏高原南北走向裂谷初始拉张时间

Table 1 Onset timing of N-S striking rifts in Tibet

裂谷名称		拉张时间/Ma	测年方法	流变学特征	活动速率/ (mm/a)	参考文献
羌塘地体	双湖	13.5 4	⁴⁰Ar/³⁹Ar 地形剖面	脆性	-	[ 44 ] [ 45 ]
羌塘地体	与东西向伸展相关的埃达克岩	47~38	U-Pb，同位素地球化学	岩脉	-	[ 41 , 46 , 47 , 48 ]
拉萨地体	隆格尔	>10	(U-Th)/He	韧性	4.0~5.0^{[ 49 ]}	[ 50 ]
	打加错	18.3	U-Pb	岩脉	-	[ 39 ]
	当惹雍错	约13 14.5	(U-Th)/He (U-Th)/He, AFT	脆性	0.3~0.7^{[ 34 ]} 4.0~5.0^{[ 49 ]}	[ 51 ] [ 34 ]
	申扎	约14	U-Pb	脆性	1.0~2.0^{[ 49 ]}	[ 52 ]
	念青唐古拉	11~5 8	⁴⁰Ar-³⁹Ar Th-Pb	韧性—脆性	4.0^{[ 24 ]}	[ 27 ] [ 24 ]
	谷露	7	(U-Th)/He	脆性	4.0~5.0^{[ 49 ]}	[ 53 ]
喜马拉雅	Leo Pargil	16.9~14.5	⁴⁰Ar/³⁹Ar	韧性	-	[ 54 , 55 ]
	Gular Mandhata	15~9	⁴⁰Ar/³⁹Ar	韧性	-	[ 56 ]
	Thakkola	11~10	磁性地层	-	-	[ 57 ]
	孔错	19 13~12 4	U-Pb (U-Th)/He U-Pb, Ar/Ar, (U-Th)/He	韧性—脆性	-	[ 40 ] [ 58 ] [ 59 ]
	Ama Drime Massif	13	Th-Pb	韧性—脆性	0.6~1.7^{[ 60 ]}	[ 53 ]
		4	(U-Th)/He			[ 61 ]
		11	P-T-D-t			[ 62 ]
	亚东	<10	Th-Pb	-	1.4^{[ 11 ]}	[ 63 ]
	亚东	5	⁴⁰Ar/³⁹Ar	脆性	1.4^{[ 11 ]}	[ 64 ]
	错那	<12	K/Ar	-	0.6~1.7^{[ 65 ]}	[ 66 ]

图2 南北走向裂谷成因模式（据参考文献[ 15 , 85 ]修改）
KLF：喀喇昆仑断裂；WHS：西构造结；EHS：东构造结

Fig.2 Theoretical models for the formation of N-S striking rifts (modified after references [15, 85])
KLF: Karakoram Fault; WHS: Western Himalayan Syntaxis; EHS: Eastern Himalayan Syntaxis

图3 南北走向裂谷板片撕裂模型（据参考文献[ 93 , 94 ]修改）
（a）印度岩石圈板片撕裂为不同的角度；（b）印度岩石圈板片撕裂角度东西两侧较缓，中部较陡；MBT：主边界断裂；MFT：主前锋断裂；MCT：主中央断裂；STDS：藏南拆离系；ZRT：泽当—仁布断裂；IYS：雅鲁藏布江缝合带；YRR：亚热裂谷带；LGR：隆格尔裂谷带；TYR：当惹雍错裂谷带；PXR：申扎裂谷带；YGR：亚东—谷露裂谷带；CR：错那裂谷带

Fig.3 Slab tearing model for the formation of N-S striking rifts (modified after references [93, 94])
(a) Slab tearing of the Indian lithosphere shows differential subduction angles; (b) Slab tearing of the Indian lithosphere shows shallow angles in the east and west and deep angles in the middle；MBT: Main Boundary Thrust; MFT: Main Frontal Thrust; MCT: Main Central Thrust; STDS: Southern Tibetan Detachment Systems; ZRT: Zedong-Renbu Thrust; IYS: Indus-Yarlung Suture; YRR: Yari Rift; LGR: Lunggar Rift; TYR: Tangra Yum Co Rift; PXR: Pumqu-Xianza Rift; YGR: Yadong-Gulu Rift; CR: Cuona Rift

图4 青藏高原低速带平面分布（a）及其东西向横剖面（b）(据参考文献[ 94 ]修改)
JS：金沙江缝合带；BNS：班公湖—怒江缝合带；IYS：雅鲁藏布江缝合带；YRR：亚热裂谷带；LGR：隆格尔裂谷带；TYR：当惹雍错裂谷带；PXR：申扎裂谷带；YGR：亚东—谷露裂谷带；CR：错那裂谷带

Fig.4 Distribution of low-velocity areas in Tibet (a) and longitudinal cross section (b) (modified after reference [ 94 ])
JS: Jinsha Suture; BNS: Bangong-Nujiang Suture; IYS: Indus-Yarlung Suture; YRR: Yari Rift; LGR: Lunggar Rift; TYR: Tangra Yum Co Rift; PXR: Pumqu-Xianza Rift; YGR: Yadong-Gulu Rift; CR: Cuona Rift

图5 青藏高原南北走向裂谷与相关岩浆岩分布关系
1：Leo Pargil；2：Gular Mandhata；3：隆格尔；4：Thakkola；5：当惹雍错—孔错；6：申扎—定结；7：亚东—谷露；8：沃卡—错那；9：双湖；ALT：阿尔金断裂；KF：昆仑断裂；KLF：喀喇昆仑断裂；JF：嘉丽断裂；JS：金沙江缝合带；BNS：班公湖—怒江缝合带；IYS：雅鲁藏布江缝合带

Fig. 5 Distribution of N-S striking rifts and related magmatic rocks in Tibet
1: Leo Pargil; 2: Gular Mandhata; 3: Lunggar; 4: Thakkola; 5: Tangra Yum Co-Kong Co; 6: Xainza-Dinggye; 7: Yadong-Gulu; 8: Woka-Cuona; 9: Shuanghu: ALT: Altyn Tagh Fault; KF: Kunlun Fault; KLF: Karakoram Fault; JF: Jiali Fault; JS: Jinsha Suture; BNS: Bangong-Nujiang Suture; IYS: Indus-Yarlung Suture

图6 青藏高原裂谷盆地演化过程（据参考文献[ 70 ]修改）
（a）裂谷初期为内流半地堑盆地，受犁式高角度正断层控制，向下延伸到近水平的糜棱岩剪切带；（b）随着伸展量增加，构造卸载导致下盘均衡反弹，同时正断层在中上地壳向上挠曲；（c）在伸展量最大的区域的均衡反弹导致裂谷盆地抬升和剥蚀，在盆地内形成分水岭

Fig. 6 Progressive development of rifts in Tibet (modified after reference [ 70 ])
(a) The rifts initiate as internal half-graben basins, bounded by a listric high-angle normal fault that soles into a subhorizontal mylonitic shear zone; (b) With increasing extension magnitude, tectonic unloading results in isostatic rebound of the footwall, as well as upwarping of the normal fault in the mid-upper crust; (c) Footwall isostatic rebound in areas of maximum extension results in uplift and incision of the rift basin and development of an intra-basinal drainage divide

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