Spatiotemporal distribution and geodynamic mechanism of the nearly NS-trending rifts in the Tibetan Plateau
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摘要:
青藏高原南部发育的一系列近南北向裂谷是印度-欧亚大陆持续挤压作用下的大型伸展构造，也是揭示高原后碰撞构造演化过程的重要对象。目前，关于南北向裂谷的形成机制存在多种假说模型，并对裂谷时空分布特征做出了不同的预测，这成为约束裂谷成因机制的关键条件。综合关于裂谷启动时间的已有研究成果，进一步梳理了南北向裂谷的时空分布特征，结果表明近南北向裂谷的启动时间似乎具有自西向东逐步减小的趋势，这与拉萨地体广泛出露的后碰撞岩浆作用演化过程一致。在此基础上，结合地球物理观测，推断近南北向裂谷的动力学机制与印度板片向东拆离假说最为契合。印度板片自西向东的拆离建立了向东传播的重力势能梯度，从而驱动岩石圈向东流动，最终导致南北向裂谷依次向东发育。
Abstract:A set of nearly NS-trending rifts developed in the Himalayan orogen and southern Tibet, which are the large-scale extensional structures formed under the continuous compression of the Indo-Eurasia continent, playing a significant role in revealing the post-collisional evolution of the Tibetan Plateau. Different predictions have been made on the spatiotemporal distribution of these rifts through the existing hypothesis models, constituting the key factors constraining the formation system of the rifts. In this study we synthesized previous studies on the initiation time of rifting, and further clarified the spatiotemporal trend. The analysis results showed that the rifting initiated progressively earlier westward, which is consistent with the evolution of post-collisional magmatism in the Lhasa Terrain. Moreover, combined with the geophysical observations, it is inferred that the geodynamic mechanism of the nearly NS-trending rifts accords closely with the hypothesis model concerning the eastward-propagating lateral detachment of the subducted Indian slab. The Indian slab detachment resulted in asynchronous gravitational potential energy gradients, which drove the lithosphere flow eastward and eventually caused the eastward development of the rifting.
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图 1 青藏高原伸展构造及其与后碰撞岩浆岩关系示意图(据Chung et al., 2005; Tayor and Yin, 2009; Guo et al., 2015修改)
Figure 1.
图 2 东西向伸展成因模式(据Molnar and Tapponnier, 1978；England and Houseman, 1988；Yin，2010；Styron et al., 2011；Yin and Taylor, 2011；Chen et al., 2015；Webb et al., 2017修改)
Figure 2.
表 1 青藏高原南北向裂谷启动时间
Table 1. Initiation time of the NS-trending rifts in the Tibetan Plateau
在图 1b中的编号 裂谷名称 启动时间/Ma 方法 流变学特征 参考文献 (A) 双湖 >13.5 Rb-Sr和40Ar/39Ar 脆性 Blisniuk et al., 2001 < 4 伸展速率和伸展量估算 脆性 Yin et al., 1999 (B) 北隆格尔 ~15 锆石U-Pb 韧性 Kapp et al., 2008 15~10 磷灰石、锆石(U-Th)/He 脆性-韧性 Sundell et al., 2013 10~8 磷灰石、锆石(U-Th)/He 脆性 Woodruff et al., 2013 (C) 南隆格尔 16~12 锆石(U-Th)/He 韧性 Styron et al., 2013 (D) Lopukangri 15~14 云母40Ar/39Ar - Sanchez et al., 2010 17~15 锆石U-Pb 韧性 Laskowski et al., 2017 (E) 当惹雍错 13 磷灰石、锆石(U-Th)/He 脆性 Dewane et al., 2006 14.5 锆石(U-Th)/He 脆性 Wolff et al., 2018 (F) 申扎 14 锆石U-Pb；磷灰石、锆石(U-Th)/He 脆性 Hager et al., 2009 (G) 谷露 7~5 磷灰石(U-Th)/He 脆性 Stockli et al., 2002 (H) 念青唐古拉 8 云母、钾长石40Ar/39Ar 韧性 Harrison et al., 1995 8 钾长石40Ar/39Ar 脆性 Kapp et al., 2005 8~6.8 磷灰石裂变径迹 脆性 吴珍汉等，2002 (I) Leo Pargil 23 独居石U-Pb 韧性 Langille et al., 2012 16~14 白云母40Ar/39Ar 韧性 Thiede et al., 2006 16 白云母40Ar/39Ar 韧性 Hintersberger et al., 2010 (J) Gurla Mandhata ~15 独居石Th-Pb 韧性 Murphy and Copeland, 2005 14~11 锆石(U-Th)/He 韧性 McCallister et al., 2014 9 云母40Ar/39Ar 韧性 Murphy et al., 2002 ~9 磁性地层 - Saylor et al., 2009, 2010 (K) Thakkhola >14 白云母40Ar/39Ar 伸展岩脉 Coleman and Hodges, 1995 11~10 磁性地层 - Garzione et al., 2000, 2003 ~17 白云母40Ar/39Ar 韧性 Larson et al., 2020 (L) 孔错 13-12 磷灰石、锆石(U-Th)/He 脆性 Lee et al., 2011 < 4 磷灰石(U-Th)/He 脆性 Mahéo et al., 2007 (M) 定结 13~10 云母40Ar/39Ar 韧性 Zhang and Guo, 2007 12~10 黑云母40Ar/39Ar 韧性 Kali et al., 2010 (N) 亚东 < 10 独居石Th-Pb 韧性 Edwards and Harrison, 1997 < 11.5 独居石U-Pb 韧性 Ratschbacher et al., 2011 13~11 云母40Ar/39Ar 韧性 Xu et al., 2013 7 磷灰石裂变径迹、磷灰石、锆石(U-Th)/He 脆性 Dong et al., 2020 (O) 错那 ~3 黑云母、钾长石40Ar/39Ar和锆石、磷灰石(U-Th)/He 脆性 Bian et al., 2020 ~5 电子自旋共振 脆性 吴中海等，2008 
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