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    西藏东南缘早二叠世长英质凝灰岩锆石U-b年龄和Hf同位素特征

    麦源君 朱利东 杨文光 解龙 童霞 郝金月 钟摇

    麦源君, 朱利东, 杨文光, 解龙, 童霞, 郝金月, 钟摇, 2021. 西藏东南缘早二叠世长英质凝灰岩锆石U-b年龄和Hf同位素特征. 地球科学, 46(11): 3880-3891. doi: 10.3799/dqkx.2020.397
    引用本文: 麦源君, 朱利东, 杨文光, 解龙, 童霞, 郝金月, 钟摇, 2021. 西藏东南缘早二叠世长英质凝灰岩锆石U-b年龄和Hf同位素特征. 地球科学, 46(11): 3880-3891. doi: 10.3799/dqkx.2020.397
    Mai Yuanjun, Zhu Lidong, Yang Wenguang, Xie Long, Tong Xia, Hao Jinyue, Zhong Yao, 2021. Zircon U-Pb and Hf Isotopic Composition of Permian Felsic Tuffs in Southeastern Margin of Lhasa, Tibet. Earth Science, 46(11): 3880-3891. doi: 10.3799/dqkx.2020.397
    Citation: Mai Yuanjun, Zhu Lidong, Yang Wenguang, Xie Long, Tong Xia, Hao Jinyue, Zhong Yao, 2021. Zircon U-Pb and Hf Isotopic Composition of Permian Felsic Tuffs in Southeastern Margin of Lhasa, Tibet. Earth Science, 46(11): 3880-3891. doi: 10.3799/dqkx.2020.397

    西藏东南缘早二叠世长英质凝灰岩锆石U-b年龄和Hf同位素特征

    doi: 10.3799/dqkx.2020.397
    基金项目: 

    国家自然科学基金项目 41972118

    冈底斯-喜马拉雅铜矿资源基地调查项目 DD20160015

    详细信息
      作者简介:

      麦源君(1995-), 男, 博士研究生, 古生物学与地层学专业.ORCID: 0000-0001-8830-0400.E-mail: maiyuanjun@126.com

      通讯作者:

      朱利东, ORCID: 0000-0001-5047-0017.E-mail: zhuld@cdut.edu.cn

    • 中图分类号: P548;P581

    Zircon U-Pb and Hf Isotopic Composition of Permian Felsic Tuffs in Southeastern Margin of Lhasa, Tibet

    • 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εHft)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.

       

    • 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,2008Zhang et al., 2014Xu 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  4  冲尼凝灰岩锆石的阴极发光图像

      Fig.  4.  Zircon CL images of the analyzed zircon 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εHft)‒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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