Destiny of Neo-Tethyan Lithosphere during India-Asia Collision
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摘要: 印度-亚洲大陆碰撞之后的新特提斯洋板片的断离过程及其产生的岩浆作用一直是青藏高原南部地质研究中受到广泛关注但存在极大争议的问题.分析了青藏高原南部拉萨地块上新特提斯洋板片断离存在的问题，总结了目前用于限制板片断离过程的岩石学方法.对拉萨地块南部典型地区早新生代镁铁质岩石开展了详细的地质年代学、主微量元素和Sr-Nd-Hf同位素地球化学分析，厘定了~57 Ma和~50 Ma与新特提斯洋板片断离过程密切相关的两套岩石.~57 Ma的镁铁质岩石显示出高的Zr/Y和Ti/Y比值，不同于拉萨地块南部广泛分布的岛弧岩浆地球化学特征，表明它们形成于板内伸展背景下，很可能代表了新特提斯板片断离的开始.~50 Ma的镁铁质岩石为富闪深成岩，反映了印度-亚洲大陆碰撞后南拉萨地块岩石圈中的富水环境，暗示大洋板片断离后仍然持续释放流体至上覆岩石圈地幔中.结合拉萨地块上已有的镁铁质岩石的年代学和地球化学数据，重建了新特提斯洋在印度-亚洲大陆碰撞之后从初始撕裂至板片完全断离的全过程，即新特提斯板片在~57 Ma开始发生初始撕裂，随后以高角度俯冲并与印度大陆岩石圈脱离，导致中拉萨和南拉萨地块同时出现广泛的镁铁质岩浆作用，在~50 Ma大洋板片完全断离.拉萨地块内部岩石圈地幔地球化学组成存在极大的不均一性，中拉萨地块和南拉萨地块东部的局部地区存在古老的岩石圈物质组成，而南拉萨地块中部主要为亏损的岩石圈.拉萨地块内局部古老富集岩石圈可能受到新特提斯洋板片断离后深部地幔物质上涌的影响转变为新生的亏损岩石圈，这一过程很可能促进了拉萨地块的中酸性岩浆大爆发作用和大陆地壳生长.Abstract: The breakoff of the Neo-Tethyan slab and related magmatism after India-Asia continental collision has been controversial topics in the geological study of the southern Tibetan Plateau. In this study, it reviews the unsolved problems and petrological methods for exploring the process on the Neo-Tethyan slab breakoff. Based on the systematic geochronology, major and trace elements and Sr-Nd-Hf isotope geochemical analyses of the Early Cenozoic mafic rocks in the typical areas of the Lhasa Terrane, it is found that two suites of mafic rocks with ages of ~57 Ma and ~50 Ma have close relationship with the Neo-Tethyan slab breakoff. The ~57 Ma mafic rocks are characterized by high Zr/Y and Ti/Y ratios, and their geochemistry indicates an intraplate affinity rather than arc magmas, indicating that they likely correspond to the magmatic expression of the initial stage of Neo-Tethyan slab breakoff. The ~50 Ma mafic rocks are appinites, reflecting the water-rich environment in the lithospheric mantle of the southern Lhasa Terrane after the India-Asia collision, suggesting the flux of slab fluids through the lithospheric mantle during breakoff of the Neo-Tethyan slab. Integrating the geochronological and geochemical data of the Early Cenozoic mafic magmatism in the Lhasa Terrane, we have reconstructed the processes from initial tear to completely breakoff of the Neo-Tethyan lithosphere after India-Asia continent collision. The initial tear of the Neo-Tethyan lithosphere occurred at ~57 Ma, then the slab detached from the India lithosphere with a high angle subduction, which resulted in the simultaneous occurrence of extensive mafic magmatism in the central and southern Lhasa Terrane. The complete slab breakoff happened at ~50 Ma. The isotopic compositions of Early Cenozoic magmatic rocks reveal that there was great geochemical heterogeneity of lithospheric mantle beneath the Lhasa Terrane. There were ancient lithospheric materials in the central Lhasa Terrane and eastern part of the southern Lhasa Terrane, while there was mainly depleted juvenile lithosphere in the central part of the southern Lhasa Terrane. The local ancient enriched lithosphere in the Lhasa Terrane is likely to transform into a juvenile depleted lithosphere by the upwelling of the deep mantle material, which may promote the eruption of the felsic magmatism and the growth of continental crust in the Lhasa Terrane.
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Key words:
- India-Asian continental collision /
- Neo-Tethys Ocean /
- slab breakoff /
- mafic rock /
- Lhasa Terrane /
- Tibetan Plateau /
- geochronology /
- geochemistry
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图 1 板片断离过程的简单图示
据Davies and von Blanckenburg（1995）. a.大陆碰撞开始，俯冲的大洋岩石圈诱发了周围软流圈地流动；b.板片的撕裂开始，软流圈上涌到断裂带中，俯冲一侧的大陆壳底垫到活动大陆边缘的大陆岩石圈之下；c.窄的岩石圈断裂带持续发展为板片断离，热的软流圈冲击之前交代的岩石圈底部会形成岩浆作用，大陆岩石圈之下板片断离后应力和势能地释放会导致地表的初步抬升；d.大洋板片沉入地幔深部，伴随着地表的进一步抬升，软流圈的深部对流使岩石圈底部遭受高温作用，大陆缝合带变得陡峭，向被动大陆边缘一侧迁移的逆冲断层导致在两侧大陆内部均会出现侵入岩石
Fig. 1. Schematic breakoff processes
图 2 青藏高原和拉萨地块简图
修改自Zhu et al. (2011).早新生代岩浆岩数据来源：岳雅慧和丁林(2006), Mo et al. (2008), Wen et al.(2008), Ji et al.(2009, 2012), Lee et al. (2009), 赵志丹等(2011)，陈晓锋等(2012)，黄丰(2015)，Zhu et al. (2015)，Huang et al.(2016, 2017, 2019a, 2019b)，Pan et al. (2016)，Liu et al. (2018)，Shu et al. (2018)，Guo et al. (2019)，Wang et al. (2019b), Zhang et al. (2019)
Fig. 2. Sketch maps of the Tibetan Plateau and the Lhasa Terrane
图 3 拉萨地块早新生代镁铁质岩石的Zr/TiO2-Nb/Y(a)和Zr/Y-Ti/Y(b)图解
图a据Winchester and Floyd (1977)；图b据Pearce and Gale (1977)
Fig. 3. Zr/TiO2-Nb/Y (a) and Zr/Y-Ti/Y (b) diagrams for the Early Cenozoic mafic rocks in the Lhasa Terrane
图 4 拉萨地块早新生代镁铁质岩石的球粒陨石标准化REE分配模式(a、b)和原始地幔标准化多元素图解(c、d)
Fig. 4. Chondrite-normalized rare earth element (REE) patterns (a, b) and primitive-mantle-normalized multi-element patterns (c, d) for the Early Cenozoic mafic rocks in the Lhasa Terrane
图 5 拉萨地块早新生代镁铁质岩石的Sr-Nd同位素组成
雅江蛇绿岩数据引自Mahoney et al. (1998)和Xu and Castillo (2004)
Fig. 5. εNd(t) vs. (87Sr/86Sr)i for the Early Cenozoic mafic rocks in the Lhasa Terrane
图 6 拉萨地块早新生代镁铁质岩石的锆石εHf(t)-t图解
南拉萨和中拉萨地块侵入岩锆石Hf同位素数据引自Zhang et al. (2019)
Fig. 6. Plots of εHf(t)-t for Early Cenozoic mafic rocks in the Lhasa Terrane
图 7 拉萨地块早新生代（~57 Ma）新特提斯洋板片初始断离及岩浆活动的概念图
Fig. 7. A conceptual diagram illustrating the tectonic position of magmatic rocks in the Lhasa Terrane during the Early Cenozoic (~57 Ma)
图 8 拉萨地块早新生代（~50 Ma）构造-岩浆事件的概念图
Fig. 8. Conceptual diagrams illustrating the tectonic and magmatic processes in the Lhasa Terrane during the Early Cenozoic (~50 Ma)
图 9 拉萨地块早新生代镁铁质岩浆岩的形成时代与其分布纬度的关系
Fig. 9. The relations of ages and latitude of Early Cenozoic mafic rocks in the Lhasa Terrane
表 1 南拉萨地块中部早新生代镁铁质岩石数据
Table 1. The Early Cenozoic mafic magmatism in the central part of southern Lhasa Terrane
样品号 位置 岩性 年龄（Ma） SiO2 (%) Mg# 数据来源 13DJ-04 达居 辉长岩脉 57.1±1.7 51.15 47.9 Huang et al. (2017) 13DJ-05 达居 辉长岩脉 57.4±0.9 53.42 46.7 Huang et al. (2017) 15DJ-07 达居 辉长岩脉 55.9±0.9 50.70 54.0 Huang et al. (2017) 16PCL-13 彭措林 富闪深成岩 50.8±0.4 46.57 52.5 Huang et al. (2019b) 16PCL-07 彭措林 富闪深成岩 51.1±0.5 44.83 43.5 Huang et al. (2019b) 15XTM53 仁钦则 闪长岩包体 50.4±0.4 56.23 47.5 Shu et al. (2018) T041F 日喀则 玄武安山岩 49.3±1.2 52.25 41.8 Lee et al. (2009) T044C 南木林 石英闪长岩 48.3±1.2 52.10 48.2 Wen et al. (2008) T047 南木林 玄武岩 44.0±0.8 50.87 42.0 Lee et al. (2009) 06FW175 Karu 闪长岩 52.6±1.2 57.57 45.6 Ji et al. (2012) 06FW174 Karu 闪长岩 50.2±1.5 56.45 43.6 Ji et al. (2012) 06FW152-2 Qulin 闪长岩 57.3±0.9 53.49 46.8 Ji et al. (2012) ST147A 尼木 石英闪长岩 50.6±0.7 53.87 48.4 Wen et al. (2008) T1031 尼木 苏长岩 57.3±0.9 54.00 62.8 Wang et al. (2019b) 06FW176 尼木 闪长岩 53.6±1.0 54.48 42.0 Ji et al. (2012) T1034 尼木 辉长岩 57.3±0.9 49.82 63.2 Wang et al. (2019b) ST152A 曲水 石英辉长岩 52.7±1.4 49.75 53.9 Wen et al. (2008) 06FW151 曲水 闪长岩 55.5±1.2 56.09 45.1 Ji et al. (2012) 06FW146 曲水 二长闪长岩 56.9±1.4 52.88 47.8 Ji et al. (2012) T0594 曲水 辉长岩 54.2±1.7 50.54 67.9 Wang et al. (2019b) 16TB-33 曲水 辉长苏长岩 50.3±2.0 51.15 53.0 Wang et al. (2019a) 16TB-46 曲水 辉长苏长岩 51.6±1.2 52.80 51.6 Wang et al. (2019a) 16TB-42 曲水 石英闪长岩 53.0±1.9 55.13 48.2 Wang et al. (2019a) T083C 拉萨西 玄武岩 43.2±1.6 50.85 37.5 Lee et al. (2009) 06FW126 南木电站 花岗闪长岩 55.3±1.0 56.62 43.2 Ji et al. (2012) 06FW128 南木电站 闪长岩脉 49.9±1.0 54.99 49.9 Ji et al. (2012) 06FW129 南木 花岗闪长岩 52.9±0.7 57.43 42.4 Ji et al. (2012) 06FW120 聂当 闪长质包体 50.3±0.6 51.94 42.3 Ji et al. (2012) ET021E 驱龙 石英辉长岩 64.0±1.4 55.05 50.9 Wen et al. (2008) 11DZ-21 达孜 辉长岩脉 56.8±1.7 53.23 43.7 黄丰(2015) 12DZ-07 达孜 辉长岩脉 57.6±1.2 58.44 50.2 黄丰(2015) 13DZ-10 达孜 辉长岩脉 57.4±1.2 49.21 54.3 黄丰(2015) 
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