Zircon U-Pb and Hf Isotopic Composition of Permian Felsic Tuffs in Southeastern Margin of Lhasa, Tibet
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摘要: 西藏东南缘记录的唐加-松多古特提斯增生杂岩带对认识古特提斯洋晚古生代的构造演化提供了新的证据.针对该杂岩带中新发现的长英质凝灰岩开展了全岩主、微量元素，锆石LA-ICP-MS U-Pb定年和锆石Hf同位素组成的研究.结果显示冲尼凝灰岩喷发于278~275 Ma，具有较高的SiO2含量（63.47%~72.65%）、Al2O3含量（14.53%~21.31%），较低的K2O含量（1.30%~2.51%）和TiO2含量（0.50%~1.17%），MgO含量较低，介于0.92%~2.00%，Mg#范围在19.9~34.2（均低于40）.富集大离子亲石元素（LILE）、亏损高场强元素（HFSE）.锆石具有较高的εHf（t）值（+10.2~+14.4）和相对年轻的地壳模式年龄TDMc=351~621 Ma，认为冲尼凝灰岩是唐加-松多古特提斯洋向北俯冲背景下的新生地壳部分熔融的产物，洋盆俯冲消减的开始时代不晚于早二叠世，并且在早二叠世拉萨地体东南缘存在新生地壳生长事件.Abstract: The Tangjia-Sumdo Paleo-Tethys accretionary complex belt, recorded in the southeastern margin of Lhasa, provides new evidence for the understanding of the Late Paleozoic tectonic evolution of the Paleo-Tethys Ocean. In this paper, it reports new data for the felsic tuff in this accretionary complex belt, including petrology, major and trace element compositions, zircon U-Pb age, and in-situ Hf isotopic compositions. U-Pb zircon dating indicates that the timing of eruption of the Chongni tuffs was ca. 278-275 Ma. They are characterized by relatively high SiO2 (63.47%-72.65%), and high Al2O3 (14.53%-21.31%), relatively low K2O (1.30%-2.51%), TiO2 (0.50%-1.17%), MgO (0.92%-2.00%), and Mg# (19.9-34.2). These tuffs exhibit LILE enrichment and HFSE depletetion. The zircons participating in the weighted age calculation have positive εHf(t) values of +10.2 to +14.4 and relatively young zircon Hf crustal model ages (TDMc=351-621 Ma). It agrees that Chongni tuffs were derived from the partial melting of the juvenile crust under the background of the northward subduction of the Tangjia-Sumdo Paleo-Tethys Ocean slab, and the beginning time of the ocean slab subduction is not later than Early Permian, before which there were the events that crust grew in the southeastern margin of Lhasa.
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Key words:
- Early Permian /
- Lhasa terrane /
- Hf isotope /
- U-Pb age /
- Tangjia-Sumdo Paleo-Tethys /
- petrology
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图 1 青藏高原地质简图以及唐加‒松多地区地质简图
a.青藏高原构造单元划分简图（李才等，2008；Zhang et al., 2014；Xu et al., 2015）；b.唐加‒松多地区地质简图.数据来源：陈松永等（2008）；Yang et al.（2009）；曾令森等（2009）；Cheng et al.(2012, 2015)；Weller et al.（2016）；Wang et al.(2019, 2021)；李楠等（2020）；于云鹏（2020）
Fig. 1. Tangjia-Sumdo geological map in the Gangdese, Tibet
图 2 冲尼凝灰岩野外照片（a, b）和镜下特征（c, d）
b.采样点位；N1.D0021-N1；N6.D0021-N6. Qtz.石英；Pl.斜长石；Bt.黑云母
Fig. 2. Field images (a, b) and micrographs (c, d) of Chongni tuffs
图 3 冲尼凝灰岩锆石的U-Pb年龄谐和图（a, c）和锆石球粒陨石标准化稀土配分图（b, d）
Fig. 3. U-Pb concordia diagrams (a, c) of the analyzed zircon and zircon chondrite-normalized REE patterns (b, d) in Chongni tuffs
图 5 冲尼凝灰岩岩石判别图
a. Zr/TiO2-Nb/Y图解，据Winchester and Floyd（1977）；b. Th-Co图解，据Hastie et al.（2007）.数据来源：大陆平均弧安山岩（Kelemen et al., 2007）；中二叠世深成岩（李楠等，2020；于云鹏，2020）；埃达克质花岗岩（Wang et al., 2021）；皮康花岗岩（Zhu et al., 2009）
Fig. 5. Classification diagrams of Chongni tuffs
图 6 原始地幔标准化微量元素蛛网图及球粒陨石标准化稀土配分曲线图
标准化数据引自Sun and McDonough（1989）.数据引用参看图 5
Fig. 6. Primitive mantle-normalized trace element spidergram and chondrite-normalized REE pattern
图 7 冲尼凝灰岩锆石微量元素特征判别图
a，b.据Belousova et al.（2002）；c，d.据Yang et al.（2012）
Fig. 7. Zircon trace element plots of Chongni tuffs
图 8 冲尼凝灰岩εHf（t）‒锆石年龄图
数据来源于Zhu et al.（2009）；牛志祥（2019）；于云鹏（2020）；Wang et al.（2021）
Fig. 8. εHf(t) vs. age diagram of Chongni tuffs
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