2022, Vol. 38
2. 成都理工大学地球科学学院, 成都 610059
2. College of Earth Sciences, Chengdu University of Technology, Chengdu 610059, China
花岗岩作为大陆地壳的重要组成部分，是地球岩石圈区别于其它行星岩石圈、大陆地壳有别于大洋地壳最主要的物质标志(Lundstrom and Glazner, 2016; 陈国能等, 2017)，详细记录了陆壳形成演化、壳-幔相互作用过程的丰富信息(Hawkesworth and Kemp, 2006; 吴福元等, 2007a; 翟明国, 2017; Zhang et al., 2021)。因此，长期以来花岗岩的成因、形成的构造环境与地球动力学背景，以及花岗质岩浆和矿化之间的关系等问题都是重要的前沿研究课题，也是大陆形成演化研究的核心内容(Chappell and White, 1974; Pearce et al., 1984; Monecke et al., 2002; Clemens, 2003; Zurevinski et al., 2017; 王孝磊, 2017; 翟明国, 2017; Zhang et al., 2021)。俯冲造山和碰撞造山是大陆地壳生长和花岗岩形成的重要动力学机制，造山带花岗岩是探索大陆地壳形成和演化的重要对象(Zhang et al., 2021)，岩浆作用发生的时间和位置以及熔融产物的类型和组成研究，可以再造造山带的构造演化历史(高永丰等, 2003)。
拉萨地块位于青藏高原南部，其作为东冈瓦纳大陆的重要组成部分，从古生代到新生代经历了复杂的演化历史(Zhu et al., 2011a, 2013, 2016)。尤其是中生代以来，拉萨地块经历了班公湖-怒江特提斯洋俯冲消减、拉萨-羌塘地块碰撞、新特提斯洋俯冲以及印度-欧亚大陆碰撞等一系列地质过程，导致中-新生代岩浆大爆发，形成的岩浆岩完好地记录了拉萨地块构造演化与深部作用过程，为研究和探索拉萨地块中-新生代演化及岩石圈构造提供了重要依据(Yin and Harrison, 2000; Kapp et al., 2005, 2007; Mo et al., 2008; Zhu et al., 2008, 2009a, b, 2011a; 朱弟成等, 2008a; Zhao et al., 2009; 闫晶晶等, 2017; 崔浩杰等, 2019)。前人对于南拉萨地块的中-新生代岩浆作用已有较好的研究，而对于中拉萨地块和北拉萨地块，同样保存了三叠纪-白垩纪的岩浆作用记录，但目前还缺乏深入系统的研究。近年来在中拉萨地块和北拉萨地块相继发现了一系列中生代的岩浆活动(Wang et al., 2014; Zheng et al., 2015; Cao et al., 2019)，涉及到洋壳岩石圈俯冲和羌塘地块-拉萨地块碰撞等重要地质过程。目前对于中拉萨地块中-西段的晚侏罗世-早白垩世岩浆作用已取得了部分认识，这些广泛发育的岩浆岩被认为与班公湖-怒江洋的南向俯冲、板片回转以及随后的板片断离作用密切相关(Zhu et al., 2009a, 2011a; Cao et al., 2016; Cao et al., 2019)。相比之下，对于中拉萨地块东段该时期发育的岩浆作用的系统研究还相对薄弱，除了有些年代学及部分锆石Hf同位素研究成果的报道之外，尚缺乏高质量的岩石地球化学数据来约束中拉萨地块岩浆作用的性质与成因及其深部动力学机制。
基于此，本文以西藏中拉萨地块东段南缘那茶淌地区花岗岩类为研究对象，在详细的野外地质调研和室内岩相学观察基础上，对该地区黑云母二长花岗岩和花岗闪长岩开展了系统的岩石学、元素地球化学、锆石U-Pb年代学和Hf同位素研究，结合区域上已发表的相关文献数据，以期揭示中拉萨地块东段晚侏罗世-早白垩世时期的岩浆作用过程、源区性质及岩石成因，并为揭示该时期岩浆作用的深部动力学机制提供更加全面的岩石学和地球化学新证据。
1 地质背景与样品特征青藏高原是由一系列起源于冈瓦纳大陆的地块从早古生代开始不断增生到亚洲大陆形成的(Dewey et al., 1988; Yin and Harrison, 2000; Pan et al., 2012; 张泽明等, 2019)。其组成单元从北到南依次可分为昆仑地块、松潘-甘孜地块、南羌塘、北羌塘、拉萨地块和喜马拉雅地块(图 1a; Allégre et al., 1984; Yin and Harrison, 2000; Yin, 2006; Gehrels et al., 2011; Zhang and Santosh, 2012; Zhang et al., 2017)，这些地体依次被昆仑(KSZ)、金沙江(JSSZ)、龙木错-双湖(LSSZ)、班公湖-怒江(BNSZ)和雅鲁藏布江缝合带(IYZSZ)分隔(Yin and Harrison, 2000; Pan et al., 2012)。作为青藏高原的重要组成部分，拉萨地块是夹持于班公湖-怒江缝合带以南和雅鲁藏布缝合带以北的巨型构造-岩浆岩带，东西向长约2500km，南北向宽150~300km，面积达45万平方千米(朱弟成等, 2006; 闫晶晶等, 2017)，主要由前寒武纪的结晶基底、古生代-中生代的沉积岩和古生代-新生代的岩浆岩组成(潘桂棠等, 2006; Zhu et al., 2011a; Zhang et al., 2012; Lin et al., 2013; Xu et al., 2013; Hu et al., 2018; 张泽明等, 2019)。根据沉积盖层和基底性质的差异，拉萨地块可以进一步划分为北拉萨地块(NL)、中拉萨地块(CL)和南拉萨地块(SL)，其间分别以狮泉河-纳木错蛇绿混杂岩带(SNMZ)和洛巴堆-米拉山断裂带(LMZ)为界(图 1, Zhu et al., 2011a, 2013)。已有研究表明，南拉萨地块和北拉萨地块以新生地壳为其主要特征(Mo et al., 2007, 2008; Zhu et al., 2011b)，目前尚未发现寒武纪结晶基底(Dong et al., 2011; Zhu et al., 2012)，而中拉萨地块是具有古老结晶基底的微陆块(Zhu et al., 2009a, 2011a)。
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图 1 西藏高原构造单元(a)及拉萨地块主要岩浆岩分布图(b)(据Zhu et al., 2011a; Cao, et al., 2019修改) 年龄数据引自Chu et al., 2006; Zhu et al., 2009b, c, 2011a; Chen et al., 2014, 2015, 2017a, b; Meng et al., 2014; Hou et al., 2015; Fei et al., 2015; Zhang et al., 2015; Sun et al., 2015a, 2015b; Yang et al., 2015; Zhao et al., 2015; Zhao et al., 2016; Cao et al., 2016; Wang et al., 2015, 2016, 2017; 曲晓明等, 2006; 康志强等, 2008; 周长勇等, 2008; 高一鸣等, 2009; 刘伟等, 2010, 2012; 孟繁一等, 2010; 李奋其等, 2010; 姜昕等, 2010; 费光春等, 2010a, b; 杜德道等, 2011; 余红霞等, 2011; 于玉帅等, 2011; 崔晓亮等, 2011; 李应栩等, 2011, 张亮亮等, 2011; 张晓倩等, 2010, 2012; 姚晓峰等, 2012; 黄克贤等, 2012; 王保弟等, 2012, 2013; 李湘玉等, 2013; 张予杰等, 2014; 王力圆等, 2014, 2016; 张志等, 2015; 范淑芳等, 2015; 周华等, 2016; 王立强等, 2016; 高家昊等, 2016; 李跃等, 2017 Fig. 1 Tectonic subdivision of the Tibetan Plateau (a) and distribution of main magmatic rocks in Lhasa Block (b) (modified after Zhu et al., 2011a; Cao, et al., 2019) |
本文研究的花岗岩体位于中拉萨地块东段南缘，地理位置处于拉萨市墨竹工卡县北东约30km的扎雪乡那茶淌地区(30°10'57″~30°12'01″N、91°55'15″~91°56'57″E)。岩性包括黑云母二长花岗岩和花岗闪长岩，其中黑云母二长花岗岩呈近东西向侵位于上石炭统-下二叠统来姑组(C2-P1l)砂岩、板岩中(图 2)，热接触变质作用较弱，在局部地段发生轻微角岩化；花岗闪长岩以岩脉形式侵入于黑云母二长花岗岩体中，在钻孔中二者接触界线清晰可见(图 3a)，研究样品采集自不同钻孔的不同深度。
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图 2 那茶淌地区地质图 1-来姑组第三岩性段第一亚层砂岩、板岩；2-来姑组第三岩性段第二亚层灰岩、大理岩；3-矽卡岩；4-黑云母二长花岗岩；5-钻孔及编号 Fig. 2 Geological map of the Nachatang area |
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图 3 那茶淌地区花岗岩野外及岩相学照片 (a)黑云母二长花岗岩与花岗闪长岩接触带；(b)黑云母二长花岗岩野外露头；(c、d)黑云母二长花岗岩镜下照片，见斜长石聚片双晶和卡氏双晶；(e)花岗闪长岩岩心照片；(f、g)花岗闪长岩镜下照片，石英晶体见溶蚀结构，斜长石见聚片双晶. Qtz-石英；Pl-斜长石；Bt-黑云母 Fig. 3 Photos of handspeciem and microphotographs of the granites in the Nachatang area |
黑云母二长花岗岩，呈灰白色，中-粗粒半自形粒状结构，块状构造，主要矿物组成为：石英(25%~30%)、斜长石(35%~40%)、钾长石(30%~35%)、黑云母(5%~8 %)、角闪石(2%~3 %)，副矿物(磁铁矿、磷灰石、褐帘石、锆石等)小于1%。石英为他形粒状，粒度不均，粒径2~5mm，镜下见溶蚀和次生加大边，波状消光，偶见裂纹；长石多为柱状、板状等自形结构，可见聚片双晶、简单双晶和环带结构；黑云母多为片状结构，具有明显多色性(图 3c, d)。
花岗闪长岩，呈灰绿色-灰白色，中-粗粒半自形粒状结构和似斑状结构，块状构造，主要矿物组成为：石英(20%~25%)、斜长石(40%~45%)、钾长石(15%~20%)、角闪石(8%~10%)、黑云母(3%~5%)，副矿物(磁铁矿、榍石、磷灰石、锆石等)小于1%；石英颗粒见贝壳断口，油脂光泽，镜下波状消光，溶蚀孔明显，偶见次生加大边；斜长石多为半自形长板状，镜下有明显的聚片双晶和环带结构；角闪石主要为黑色，长柱状，两组解理明显；黑云母主要呈片状，镜下有棕绿色-棕黄色多色性(图 3f, g)。
2 分析方法 2.1 岩石地球化学分析本次研究采集8件花岗岩样品用于全岩主、微量元素分析，相关测试在西南冶金地质测试所完成。采集新鲜岩石样品利用蒸馏水进行清洗，经过破碎、缩分、称重产生的粉末用于元素地球化学测试。主量元素测试方法为XRF法，仪器为Axios X荧光仪(PANalytical Company, Netherlands)。微量元素检测方法为等离子体质谱法，仪器为NexLON 300x ICP-MS。主、微量元素分析精度优于5%。
2.2 锆石U-Pb测年本次研究采集2件测年样品，黑云母二长花岗岩(NCTYT-1)和花岗闪长岩(NCTYT-2)。岩石碎样、锆石挑选、样品制靶和阴极发光(CL)显微照相由中国科学院广州地球化学研究所实验室完成。锆石U-Pb同位素定年在中国地质调查局天津地质调查中心实验室分析完成，所采用的测试设备为激光烧蚀多接收器电感耦合等离子体质谱仪(LA-MC-ICP-MS)系统，其中多接收器电感耦合等离子体质谱仪为Thermo Fisher公司制造的Neptune，激光器为美国ESI公司生产的UP193-FX ArF准分子激光器，激光波长193nm，脉冲宽度5ns。详细的仪器操作条件和实验流程方法见李怀坤等(2009)。采用208Pb校正法对普通铅进行校正。元素含量及U-Th-Pb同位素比值和年龄计算均采用软件ICPMSDataCal 9.0进行处理。锆石U-Pb年龄谐和图的绘制和MSWD的计算则采用Isoplot /Ex_ver3。
2.3 锆石Hf同位素分析锆石原位Hf同位素的分析测试在中国地质调查局天津地质调查中心同位素实验室利用Neptune公司LA-MC-ICP MS完成，分析测试点位于锆石U-Pb同位素测试点附近，激光剥蚀束斑直径约35μm，具体实验条件和流程详见耿建珍等(2011)。使用GJ-1作为标准锆石检测实验数据，本次分析过程中GJ-1的Hf同位素含量为0.282020±0.000016 (2σ，N=11)，与文献报道值在误差范围内一致。εHf(t)值根据测点的锆石U-Pb年龄计算，采用176Lu衰变常数为1.876×10-11y-1(Söderlund et al., 2004)，球粒陨石176Hf/177Hf比值为0.282785，176Lu/177Hf比值为0.0336 (Bouvier et al., 2008)。亏损地幔模式年龄(tDM)的计算参考现今亏损地幔176Lu/177Hf比值0.28325，176Lu/177Hf比值为0.0384 (Griffin et al., 2000)。假设每颗锆石的母岩浆来自平均大陆地壳，采用176Lu/177Hf比值为0.015 (Griffin et al., 2002)计算锆石Hf同位素的地壳模式年龄(tDMC)。选择不同衰变常数不会影响实验结果。
3 分析结果 3.1 岩石地球化学 3.1.1 主量元素黑云母二长花岗岩的SiO2含量为71.02%~71.81%，平均71.47%；Al2O3含量为13.45%~13.57%，平均13.51%；Na2O含量为2.26%~2.59%，平均2.45%；K2O含量为4.53%~4.89%，平均4.77%；MgO含量为0.32%~0.38%，平均0.35%；全碱(Na2O+K2O)含量为6.79%~7.47%，K2O/Na2O值为1.89~2.00(表 1)。
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表 1 那茶淌地区花岗岩主量元素(wt%)和微量元素(×10-6)地球化学数据 Table 1 Whole-rock major (wt%) and trace (×10-6) elements of the granites in the Nachatang area |
花岗闪长岩的SiO2含量为65.17%~66.73%，平均66.21%；Al2O3含量为14.43%~15.20%，平均14.63%；Na2O含量为2.85~3.09%，平均3.01%；K2O含量为3.70% ~4.28%，平均4%；MgO含量为1.11%~1.20%，平均1.15%；全碱(Na2O+K2O)含量为6.55%~7.37%，K2O/Na2O值为1.29~1.38(表 1)。
在A/NK-A/CNK图(图 4a)上，两种岩石投点主要落在准铝质-弱过铝质区域，其中，黑云母二长花岗岩A/CNK值为1.03~1.14(＞1)、平均1.01，A/NK值为1.41~1.57(＞1)，Al2O3＞CaO+Na2O+K2O，属于弱过铝质岩石特征；花岗闪长岩A/CNK值为0.98~1.02，平均值为0.99(＜1)，A/NK值为1.50~1.66(＞1)，显示准铝质-弱过铝质的特征。在SiO2-K2O图解上，黑云母二长花岗岩样品成分的投点落在花岗岩区，花岗闪长岩成分投点落入花岗闪长岩区域，二者同属于高钾钙碱性系列岩石(图 4b)。
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图 4 那茶淌地区花岗岩地球化学图解(a, 据Rickwood, 1989; b, 据Peccerillo and Taylor, 1976) Fig. 4 Geochemical plots of granitiods in the Nachatang area (a, after Rickwood, 1989; b, after Peccerillo and Taylor, 1976) |
那茶淌地区两类花岗岩具有相似的微量元素地球化学特征。黑云母二长花岗岩的大离子亲石元素(LILE)Rb、Ba、K含量分别为：212.6×10-6~216.5×10-6、727.0×10-6~2001×10-6和37585×10-6~40552×10-6；花岗闪长岩的大离子亲石元素(LILE)Rb、Ba、K含量分别为：147.4×10-6~185.0×10-6、646.9×10-6~1283×10-6和30718×10-6~35537×10-6；黑云母二长花岗岩的高场强元素(HFSE)Nb、P、Ta、Ti含量分别为：10.50×10-6~15.77×10-6、201.6×10-6~231.8×10-6、0.74×10-6~1.56×10-6和869.9×10-6~1233×10-6，花岗闪长岩的高场强元素(HFSE)Nb、P、Ta、Ti含量分别为：17.13×10-6~20.11×10-6、640.7×10-6~767.3×10-6、1.24×10-6~1.71×10-6和3692×10-6~4117×10-6(表 1)。由原始地幔标准化微量元素蛛网图(图 5a)可以看出，该地区黑云母二长花岗岩和花岗闪长岩均表现出大离子亲石元素(LILE)Rb、Ba、K富集，高场强元素(HFSE)Nb、P、Ta、Ti亏损，Nd、La等元素富集的特征，说明花岗岩成岩过程中经历了斜长石、磷灰石和钛铁矿等矿物的分离结晶作用。
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图 5 那茶淌地区花岗岩原始地幔标准化微量元素蛛网图(a, 标准化值据Sun and McDonough, 1989)和球粒陨石标准化稀土元素配分图(b, 标准化值据Boynton, 1984) Fig. 5 Primitive-mantle normalized trace element spider diagrams (a, normalization values after Sun and McDonough, 1989) and chondrite-normalized rare earth element patterns (b, normalization values after Boynton, 1984) for the granites in the Nachatang area |
稀土元素组成方面，花岗闪长岩稀土元素总量(ΣREE=263.9×10-6~313.8×10-6，平均289.8×10-6)高于黑云母二长花岗岩的(ΣREE=116.3×10-6~168.8×10-6，平均145.2×10-6)，(表 1)。总体上黑云母二长花岗岩和花岗闪长岩具有相似的稀土元素配分型式(图 5b)，黑云母二长花岗岩LREE/HREE的比值范围为9.84~12.49，花岗闪长岩LREE/HREE的比值范围为10.1~11.6，均表现为轻稀土元素相对富集，重稀土元素亏损的特征。黑云母二长花岗岩δEu值范围为0.69~0.94，花岗闪长岩δEu值范围为0.59~0.76，呈现铕亏损的特征；黑云母二长花岗岩δCe值范围为0.91~0.92，花岗闪长岩δCe值范围为0.88~0.93，呈现轻微亏损的特征。黑云母二长花岗岩(La/Yb)N比值范围为16.5~25.0，花岗闪长岩(La/Yb)N比值范围为14.8~18.0，说明该地区花岗岩类在成岩过程中轻重稀土元素发生了强烈的分馏作用。
3.2 锆石U-Pb定年那茶淌地区花岗岩的锆石CL图像(图 6)显示，锆石的主要特征为灰白色-灰黑色，半自形-自形结构，外形主要为长柱状或菱柱形，长约30~300μm，宽约20~110μm，长宽比值为1.5~2.7，发育明显的振荡环带结构，Th/U值为0.68~2.16，具有典型的岩浆锆石特征(吴元保, 2004)。黑云母二长花岗岩(样品NCTYT-1)21个锆石测点的U含量为140×10-6~860×10-6，Th含量为490×10-6~1826×10-6，Th/U比值为1.38~2.16(表 2)。花岗闪长岩(样品NCTYT-2)20个锆石测点的U含量为140×10-6~750×10-6，Th含量为234×10-6~1120×10-6，Th/U比值为0.68~2.08(表 2)。207Pb/235U-206Pb/238U协和图(图 7)，所有测试点均落在谐和线上或者附近，说明锆石没有发生明显的Pb流失，得到的年龄真实可靠，对测点获得年龄进行加权平均计算，得到黑云母二长花岗岩结晶年龄为147±1.4Ma (MSWD=1.50, n=21)，花岗闪长岩结晶年龄为140.6±1.3Ma (MSWD=0.89, n=20)，显示那茶淌地区花岗岩的成岩时代为晚侏罗世-早白垩世。
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图 6 那茶淌地区黑云母二长花岗岩(NCTYT-1)和花岗闪长岩(NCTYT-2)的锆石阴极发光CL图像 Fig. 6 Cathodoluminescence images of selected zircon grains from the biotite granite(NCTYT-1) and granodiorite(NCTYT-2) |
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表 2 那茶淌地区花岗岩LA-MC-ICPMS锆石U-Pb定年结果 Table 2 Zircon LA-MC-ICPMS U-Pb analysis data of the granites in the Nachatang area |
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图 7 那茶淌地区黑云母二长花岗岩(NCTYT-1)和花岗闪长岩(NCTYT-2)锆石U-Pb定年谐和图及加权平均年龄图 Fig. 7 Zircon U-Pb dating concordances and weighted mean ages of the biotite monzogranite (NCTYT-1) and granodiorite (NCTYT-2) in the Nachatang area |
本次研究在锆石U-Pb年代学测试基础上，对黑云母二长花岗岩(NCTYT-1)和花岗闪长岩(NCTYT-2)样品的年代学测点开展了Lu-Hf同位素测试，数据见表 3。黑云母二长花岗岩锆石原位21个测点进行Hf同位素测试，176Hf/177Hf值为0.282073~0.282467，平均为0.282397；176Lu/177Hf值为0. 000721~0.001822，平均为0.001389；两种花岗岩锆石176Lu/177Hf值均小于0.002，说明锆石在形成过程中具有很低的放射性成因Hf的积累，可以判定锆石的176Hf/177Hf比值和锆石形成时的比值一致(Amelin et al., 1999)。黑云母二长花岗岩锆石εHf(0)值为-24.73~-13.25，εHf(t)值为-21.64~-7.66，Hf同位素地壳模式年龄(tDMC)介于1.69~2.56Ga之间，平均为1.84Ga。花岗闪长岩锆石原位20个测点进行Hf同位素进行分析测试，176Hf/177Hf值为0.282349~0.282456，平均为0.282404；176Lu/177Hf值为0.000699~0.001762，平均为0.001126；εHf(0)值-14.96~-11.18，平均为-13.02；εHf(t)值为-11.95~-8.15，平均为-10.04；Hf同位素地壳模式年龄(tDMC)介于1.71~1.95Ga之间，平均为1.83Ga。
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表 3 那茶淌地区花岗岩的锆石Hf同位素组成 Table 3 Hf isotopic composition of zircons of the granites in the Nachatang area |
区域上，中拉萨地块晚侏罗世岩浆岩主要分布于措勤、雄巴、盐湖、许如错、亚热、门巴等地区(黄俊平等, 2006; 姜昕等, 2010; Zhu et al., 2011a; 闫晶晶等, 2017)。许如错岩体，岩性主要为黑云母二长花岗岩和闪长岩，成岩时代为155~161Ma(黄俊平等, 2006; 闫晶晶等, 2017)；夏定勒岩体，岩性为二长花岗岩，成岩时代为153Ma(闫晶晶等, 2017)；雄巴岩体，岩性主要为花岗闪长岩，成岩时代为149Ma(姜昕等, 2010)；则弄群火山岩，成岩时代为129~131Ma(朱弟成等，2008b)；措勤花岗岩体，成岩时代为152Ma(Zhu et al., 2011a)；盐湖地区的流纹岩，成岩时代为146Ma(Zhu et al., 2011a)。1/25万区域地质调查报告在文部、科波熊、夏定勒地区也报道了该时期的岩浆活动(闫晶晶等, 2017)，在文部复式岩体中获得了154±8.4Ma的锆石U-Pb年龄(闫晶晶等, 2017)，在央雄勒复式岩体中分别获得了142Ma的白云母K-Ar年龄(卢书炜等, 2006)。此外，Zhu et al.(2011a)在门巴(154Ma)、梅朵(153Ma)和亚热(146Ma，160Ma)地区也发现了晚侏罗世中酸性岩浆作用的记录。本文锆石U-Pb年代学研究显示，那茶淌地区黑云母二长花岗岩侵位时代为147±1.4Ma，为晚侏罗世中酸性岩浆活动的产物，与上述年龄值较为一致。
中拉萨地块的早白垩世岩浆岩整体上呈东西向带状展布，主要分布于措勤、申扎、门巴、波密、八宿、察隅等地区。措勤地区的早白垩世花岗质岩石主要分布于江让-尼雄一带，岩体主要侵位于石炭系-二叠系、侏罗系和白垩系地层中，岩石类型丰富，主要包括花岗闪长(斑)岩、黑云母二长花岗岩、石英闪长岩和正长花岗岩等，富含大量同期闪长质包体(张晓倩等, 2012)，这些岩体成岩时代为107~122Ma，大多数据集中于110Ma左右(周长勇等, 2008; Zhu et al., 2009a; 张晓倩等, 2012)。申扎地区的早白垩世花岗岩类分布于娘热藏布、甲岗山、阳定、扁前浦南一带，包括闪长岩、花岗闪长岩、二云母花岗岩、黑云母花岗岩和花岗斑岩等，同期闪长岩多以包体形态产出，侵位于石炭系-二叠系沉积地层中，侵位时代为113~134Ma(Zhu et al., 2009a; 张亮亮等, 2011; 孟繁一, 2014)。门巴地区的早白垩世花岗质岩石主要分布于巴嘎-色日荣一带，岩石类型主要为黑云母二长花岗岩、斑状花岗闪长岩和二长花岗岩等，侵入于石炭系-二叠系来姑组地层中，成岩时代为117~128Ma(孟繁一, 2014)。此外，前人对中拉萨地块念青唐古拉成矿带部分矿区的早白垩世岩浆作用也进行了报道，如亚贵拉铅锌矿区石英斑岩(126.7~130.6Ma，高一鸣等, 2009)，洞中拉铅锌矿区花岗斑岩(124±1.9Ma，费光春等, 2010a)和辉绿玢岩(117±1Ma，费光春等，2010b)。波密-八宿-察隅地区的早白垩世花岗岩类岩性主要为闪长岩、花岗闪长岩、和二长花岗岩，成岩时代为110~133Ma(Booth et al., 2004; Chiu et al., 2009; Zhu et al., 2009b)，有学者将其解释为后碰撞背景下增厚地壳重熔形成的S型花岗岩，并受到了新特提斯洋壳岩石圈北向俯冲的影响(Chiu et al., 2009)。Zhu et al.(2009b)发现了同期的察隅Ⅰ型花岗岩，认为该岩体很可能是在班公湖-怒江海洋岩石圈南向俯冲作用下，由俯冲带之上的幔源岩浆既提供热量诱发古老地壳物质重熔，又与该壳源熔体发生混合而形成。本文获得的那茶淌地区花岗闪长岩锆石U-Pb年龄为140.6±1.3Ma，为早白垩世中酸性岩浆活动的产物，这一年龄结果与前人研究相比有些偏老。
4.2 岩石成因及岩浆源区每种源岩和岩石形成作用都与特定的构造环境密切相关(Pitcher, 1983)，因此准确鉴别花岗岩的成因类型是解译岩石成因和构造背景的基础。根据实际矿物含量、全岩地球化学成分和微量元素丰度的不同，可以将花岗岩类分为Ⅰ型、S型、A型和M型4类(Chappell and White, 1974; 马鸿文, 1992; Chappell, 1999)。Chappell and White(1974)根据源岩的性质提出Ⅰ型和S型花岗岩的分类标准；Collins et al.(1982)提出A型花岗岩的概念，具有相对不含水(Anhydrous)、富碱(Alkali)和非造山环境(Anorogenic)的特征；随后Pitcher(1983)识别出M型花岗岩，认为这种类型花岗岩主要是产于大洋盆地之中，常与蛇绿岩套共生产出，岩浆源区来自于地幔(Mantle)。不同成因类型的花岗岩代表了不同构造活动带、不同源岩和岩石形成作用过程的最终产物，每一种成因类型都具有代表其物质来源和形成条件的特殊标志。
不同成因类型的花岗岩在矿物组成和元素地球化学成分上通常存在较大差异(马鸿文, 1992)。岩石矿物成分在确定了岩石的铝饱和指数(A/CNK)基础上，根据源岩是否经历地表化学沉积作用，划分出了Ⅰ型和S型花岗岩。如，堇青石、角闪石和碱性暗色矿物是识别Ⅰ型、S型和A型花岗岩最重要的标志性矿物。堇青石、白云母、石榴子石等富铝矿物的出现则可以说明岩石达到铝饱和状态，同时这些矿物也是鉴别S型花岗岩的特征矿物，尤其是岩石中若出现堇青石则可以确定为S型花岗岩；而角闪石则是Ⅰ型花岗岩的特征判别矿物(谢富伟, 2019)。
本文研究的那茶淌地区黑云母二长花岗岩和花岗闪长岩都含有角闪石，未见堇青石和碱性暗色矿物，从矿物学特征上表明该区花岗岩具有Ⅰ型花岗岩的特征。在元素地球化学成分上，黑云母二长花岗岩和花岗闪长岩具有高度相似的稀土配分型式和微量元素蛛网曲线，表明二者具有强烈的亲缘关系，且经历了相似的演化过程。
在(Zr+Nb+Ce+Y)-(Na2O+K2O)/CaO图解中(Whalen et al., 1987)，本文的研究样品均落入未分异的花岗岩区域(图 8b)，而未经强烈分异的花岗岩可用A/CNK=1.1作为划分Ⅰ和S型花岗岩的分界，前已述及本文花岗岩样品多数为A/CNK < 1.1(图 3)，符合Ⅰ型花岗岩的地球化学特征。
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图 8 那茶淌地区花岗岩体岩石成因判别图解 (a)SiO2-P2O5图解；(b)(Zr+Nb+Ce+Y)-(Na2O+K2O)/CaO图解 Fig. 8 Discrimination diagrams of petrogenetic types for granitoids in the Nachatang area |
实验岩石学研究表明，磷灰石在准铝质-弱过铝质岩浆中的溶解度较低(P2O5含量约为0.1%)，并会随着岩浆温度的降低和SiO2的增加而降低，所以准铝质-弱过铝质的花岗岩中磷灰石总是会优先结晶，残余岩浆的P2O5含量也会逐渐降低(Watson, 1979; Watson and Capobianco, 1981)。然而，磷灰石在过铝质花岗岩中(A/CNK=1.1~1.3)的溶解度表现出不同的变化趋势，会随着A/CNK的增加而增加(A/CNK=1.3时，P2O5含量可达到0.63%)，过铝质岩浆中由于磷灰石的溶解度较高，不会优先结晶，所以过铝质花岗岩中随着SiO2的增加，P2O5含量会增高或保持不变(Watson, 1979; Watson and Capobianco, 1981; 谢富伟, 2019)。因此，磷灰石的这种地球化学行为被用于区分Ⅰ型和S型花岗岩(Chappell，1999; Wu et al., 2003; 闫晶晶等，2017; 谢富伟, 2019)。在SiO2-P2O5图解中(图 8a)，本文花岗岩类岩石样品SiO2与P2O5呈现出一定负相关关系，与中拉萨地块同期岩浆岩样品的P2O5含量主体显示出随SiO2含量的增加而降低的趋势(闫晶晶等，2017)，与Ⅰ型花岗岩的演化趋势较一致。综上所述，那茶淌地区的晚侏罗世-早白垩世花岗质岩石为准铝质-弱过铝质钙碱性Ⅰ型花岗岩。
在判别岩浆源区方面，锆石原位Lu-Hf同位素是可以详细记录岩浆混合和分异过程中同位素的组成变化，以及有效识别地幔岩浆端元的一种重要同位素示踪方法(Li et al., 2007; 吴福元等, 2007b)。一般而言，具有较高的εHf(t)值和相应较年轻的模式年龄，表明花岗岩可能来源于大陆地壳中地幔物质的混入或新生地壳的再循环；而具有较低的εHf(t)值和相应老的模式年龄，则表明花岗岩可能来源于古老地壳的深融或重融(Ben-Bassat et al., 1980; Mo et al., 2007)。Ⅰ型花岗岩可由地壳重熔过程中幔源物质的加入而形成(Kemp et al., 2007; Collins and Richards, 2008; Zhu et al., 2009b, c)或是壳内中基性火成岩或变质岩部分熔融形成(Chappell and Stephens, 1988)。本文黑云母二长花岗岩和花岗闪长岩均以较负的、变化范围较大的锆石εHf(t)值为特征(表 3、图 9)。其中，黑云母二长花岗岩锆石εHf(t)值为-21.64~-7.66，Hf同位素地壳模式年龄(tDMC)为1.68~2.56Ga；花岗闪长岩锆石εHf(t)值为-11.95~-8.15，Hf同位素地壳模式年龄(tDMC)为1.71~1.95Ga。这种变化范围大的锆石Hf同位素组成可能是由于长英质岩浆和镁铁质岩浆发生岩浆混合的产物或是表明岩石的源区物质组成的不均一性。大量的中拉萨地块样品显示出非常负的εHf(t)值特征(图 9)，结合中拉萨地块具有古老地壳基底的特征，认为那茶淌地区准铝质-弱过铝质Ⅰ型花岗岩可能来源于中拉萨地块古老下地壳物质的重熔。
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图 9 中拉萨地块晚侏罗世-早白垩世岩浆活动的锆石εHf(t)与U-Pb年龄图解 中拉萨地块其它岩浆岩锆石Hf同位素数据引自Zhu et al., 2009b, 2011a Fig. 9 Plot of zircon εHf(t) vs. ages of the Late Jurassic-Early Cretaceous igneous rocks in the Central Lhasa Terrane |
花岗岩类的形成和大地构造环境具有密切的关系(Barbarin, 1999)，岩石的地球化学特征在判别构造环境和地球动力学演化方面提供有用的信息。那茶淌地区黑云母二长花岗岩和花岗闪长岩的主量元素地球化学特征分析显示Al2O3含量较高，分别为13.45%~13.57%(平均13.51%)和14.43%~15.20%(平均14.63%)，TiO2含量较低，分别为0.15%~0.21%(平均0.17%)和(0.62%~0.69%，平均0.64%)，与弧背景下的岩浆岩地球化学特征相似(Crawford et al., 1987)。微量元素以富集K、Rb、Ba、Th等大离子亲石元素，亏损Ta、Nb、P、Ti等高场强元素为特征；稀土元素均表现为轻稀土元素富集，重稀土元素相对亏损，具弱的负Eu异常，同样显示出弧岩浆岩的地球化学特征(Pearce, 1983)。在构造环境判别Yb-Ta图(图 10a)和(Yb+Ta)-Rb图(图 10b)中，两种岩石样品均落入火山弧花岗岩区域内；在Y-Sr/Y图解(图 10c)和YbN-(La/Yb)N图解(图 10d)中，样品均落入经典岛弧岩石区域，显示出那茶淌地区花岗岩具有弧型岩浆岩的地球化学特征(Sun and McDonough, 1989; Taylor et al., 1985; Kang et al., 2014)，表明那茶淌地区花岗岩类形成于与板片俯冲有关的火山弧环境中。
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图 10 那茶淌地区花岗岩Yb-Ta(a)、(Nb+Y)-Rb(b)、Y-Sr/Y(c)和YbN-(La/Yb)N(d)图解(a, b, 底图据Pearce et al., 1984；c, d, 底图据Defant and Drummond, 1990) Fig. 10 Diagrams of Yb vs. Ta (a), (Nb+Y) vs. Rb (b), Y vs. Sr/Y (c) and YbN vs. (La/Yb)N (d) for the granites in the Nachatang area (a, b, after Pearce et al., 1984; c, d, after Defant and Drummond, 1990) |
目前对于中拉萨地块中生代岩浆岩的成因和地球动力学背景还存在较大争论，主要集中在新特提斯洋壳北向的低角度或平板俯冲(Coulon et al., 1986; Kapp et al., 2007)和班公湖-怒江洋壳南向俯冲及断离(潘桂棠等, 2006; 朱弟成等, 2006, 2008a, b; Zhu et al., 2009a, b)两大观点的争论。研究表明，洋壳板片俯冲作用形成的弧型岩浆作用，将产生从缝合带到内部的逐渐年轻的趋势(Gutscher et al., 2000; Cao et al., 2019)，然而这种趋势从南拉萨地块到中拉萨地块的岩浆活动尚未得到证实(Chen et al., 2017a；Cao et al., 2019)。通过对中部和北部拉萨地块已发表年代学和地球化学数据的综合归纳，结合本文数据，表明在中侏罗世-早白垩世期间，中部和北部拉萨地块有连续的岩浆作用记录，岩石类型从偏铝质到过铝质均有出现，主要为Ⅰ型花岗岩(大部分A/CNK＜1.1)(Cao et al., 2016; 闫晶晶等, 2017)。此外，有学者研究了中拉萨地块早白垩世花岗岩的K2O含量与班公湖-怒江缝合带的距离呈正相关关系，认为是班公湖-怒江大洋板块南向俯冲导致了这些岩浆岩的形成(Wu et al., 2016; Cao et al., 2019)。因此，根据本文研究结果，结合拉萨地块同时代岩浆作用成果(Zhu et al., 2011a; 闫晶晶等, 2017; Cao et al., 2019)，本文认为中拉萨地块东段晚侏罗世-早白垩世岩浆活动，是在班公湖-怒江洋壳南向俯冲的地球动力学背景之下(图 11)，由俯冲带之上的幔源岩浆提供热量诱发中拉萨地块古老地壳物质重熔所形成的。
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图 11 拉萨地块晚侏罗世-早白垩世岩浆活动的动力学模型(据Cao et al., 2019修改) Fig. 11 Schematic illustration of the tectono-magmatic evolution of the Lhasa subterrane during Late Jurassic- Early Cretaceous time (modified after Cao et al., 2019) |
(1) 锆石LA-MC-ICP-MS U-Pb定年结果显示中拉萨地块东段南缘那茶淌地区黑云母二长花岗岩成岩年龄为147.1±1.4Ma，花岗闪长岩成岩年龄为140.6±1.3Ma，表明该区花岗岩类为晚侏罗世-早白垩世岩浆活动的产物。
(2) 那茶淌地区黑云母二长花岗岩和花岗闪长岩具有相似的地球化学特征，表现为：富SiO2、Al2O3和(Na2O+K2O)，低TiO2；微量元素富集大离子亲石元素K、Rb、Ba和轻稀土元素，亏损高场强元素Ta、Nb、P、Ti和重稀土元素，有弱的负Eu异常；显示Ⅰ型准铝-弱过铝质的高钾钙碱性系列特征。
(3) 那茶淌地区花岗岩类锆石εHf(t)为较大的负值和古老的地壳模式年龄，指示岩浆可能来源于古老下地壳物质的重熔，其形成的构造背景与班公湖-怒江洋南向俯冲有关。
致谢 西藏鑫茂矿业有限公司为本研究的野外工作提供了大量帮助；四川省核工业地质调查院李盛俊、史子豪、李文祥参与了野外地质调查；审稿专家提出了大量富有建设性的修改意见和建议；在此一并致以诚挚的谢意！
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