2020, Vol. 36
2. 中国科学院大学, 北京 100049;
3. 中国科学院地球科学研究院, 北京 100029;
4. 新疆地矿局物化探大队, 昌吉 831100
2. University of Chinese Academy of Sciences, Beijing 100049, China;
3. Institutions of Earth Science, Chinese Academy of Sciences, Beijing 100029, China;
4. Geophysical and Geochemical Exploration Team, Xinjiang Bureau of Geology and Mineral Exploration and Development, Changji 831100, China
喀喇昆仑地体处于金沙江缝合线和什约克缝合带之间，北接巴颜喀喇地体与西昆仑地体，南连科西斯坦-拉达克地体(图 1a)，是研究特提斯构造演化、特别是西昆仑-喀喇昆仑构造演化的关键地区之一。近年来，对于喀喇昆仑地体基底特征及其与西昆仑地体的拼贴过程等前中生代构造演化有许多进展和共识(张传林等, 2007; 王春英等, 2009; 计文化等, 2011; 刘铮, 2015; 朱杰等, 2016)。但是，对喀喇昆仑地体中生代构造格架与演化特征研究较少，对发育于喀喇昆仑地体中林济塘盆地构造演化特征不清，对喀喇昆仑地体南侧的什约克洋片俯冲结束时间还存在不同认识(晚侏罗世，Murphy et al., 1997；早白垩世，Crawford and Searle, 1992; Matte et al., 1996; Heuberger et al., 2007; Jiang et al., 2014; 朱杰等, 2016; Chapman et al., 2018；晚白垩世，Jain and Singh, 2008; Li et al., 2016; Pan, 1996; Searle et al., 1987; Treloar et al., 1989；以及在40Ma之后，Bouilhol et al., 2013)。
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图 1 青藏高原及其西北部构造简图(a、b, 底图据Li et al., 2019)和甜水海区域地质图(c) 1-第四系；2-上新统阿图什组；3-上白垩统铁龙滩组；4-中侏罗统龙山组；5-二叠系红山湖组；6-上石炭统恰提尔群；7-下志留统下温泉沟群；8-寒武系甜水湖组；9-长城系甜水海岩群；10-林济塘中生代盆地；11-喀喇昆仑地体；12-三叠纪花岗岩；13-早白垩世花岗岩类；14-晚白垩世花岗岩类；15-侏罗纪玄武岩；16-羌塘地体；17-区域大断裂；18-地质界线；19-缝合带；20-断裂；21-河流；22-不整合界线；23-矿点；24-剖面位置；Ⅰ-库地-苏巴什缝合带；Ⅱ-康西瓦缝合带；Ⅲ-金沙江缝合带；Ⅳ-什约克缝合带；Ⅴ-班公湖缝合带；Ⅵ-雅鲁藏布缝合带；①布伦阔勒岩群流纹岩锆石U-Pb年龄(计文化等, 2011)；②阿依里西花岗质斑岩继承锆石U-Pb年龄(朱杰等, 2016)；③阿依里西花岗质斑岩继承锆石U-Pb年龄(朱杰等, 2016)；④种羊场流纹岩继承锆石U-Pb年龄(胡军等, 2016)；⑤大红柳滩铁矿含铁白云质大理岩继承锆石U-Pb年龄(Hu et al., 2016)；⑥大红柳滩铁矿白云母石英片岩继承锆石U-Pb年龄(Hu et al., 2016)；⑦大红柳滩二云母花岗岩继承锆石U-Pb年龄(魏小鹏等, 2017) Fig. 1 Structural sketch map of northwestern Tibetan Plateau (a, b, after Li et al., 2019) and geological map of the Tianshuihai area (c) 1-Quaternary; 2-Pliocene Atushi Fm.; 3-Late Cretaceous Tielongtan Fm.; 4-Middle Jurassic Longshan Fm.; 5-Permian Hongshanhu Fm.; 6-Late Carboniferous Qiatier Group; 7-Lower Wenquangou Group of Early Silurian; 8-Tianshuihu Fm. of Cambrian; 9-Tianshuihai Group of Changcheng System; 10-Linjitang Mesozoic basin; 11-Karakoram terrane; 12-Triassic granite; 13-Early Cretaceous granodiorite; 14-Early Cretaceous granite; 15-Early Cretaceous diorite; 16-Qiangtang terrane; 17-regional major fault; 18-geological boundary; 19-suture; 20-fault; 21-rivers; 22-unconformity; 23-deposits; 24-section position; Ⅰ-Kudi-Subashi suture; Ⅱ-Kangxiwa suture; Ⅲ-Jinshajiang suture; Ⅳ-Shyok suture; Ⅴ-Bangonghu suture; Ⅵ-Yarlung Zangbo suture; ① the zircon U-Pb age of rhyolite from the Bulunkuo Group (Ji et al., 2011); ② the zircon U-Pb age of granite porphyry from Ayilixi (Zhu et al., 2016); ③ the inherited zircon U-Pb age of granitic porphyry from Aylixi (Zhu et al., 2016); ④ the inherited zircon U-Pb age of rhyolite from Zhongyangchang (Hu et al., 2016b); ⑤ the inherited zircon U-Pb age of iron-bearing dolomitic marble from Dahongliutan iron mine (Hu et al., 2016); ⑥ the detritus zircon U-Pb age of muscovite quartz schist from Dahongliutan iron mine (Hu et al., 2016); ⑦ the inherited zircon U-Pb age of two-mica granite from Dahongliutan (Wei et al., 2017) |
近来，我们对林济塘中生代盆地地层与构造进行了调查，并在甜水海地区中侏罗统龙山组地层中发现了辉长岩侵入体。基于该岩体岩石学、地球化学、年代学和构造背景的研究，并结合新的地质构造资料，建立了区域中生代构造演化模式，以期为喀喇昆仑地区中生代构造演化过程提供新的信息与约束。
1 区域地质特征喀喇昆仑地体位于青藏高原西北缘。青藏高原西北缘北接塔里木地块，南邻喜马拉雅造山带(图 1a; Dewey et al., 1988; 潘裕生等, 1994; Yin and Harrison, 2000; Xiao et al., 2000, 2002, 2005; 张传林等, 2007)，由8个构造单元组成，从北向南依次为库地-苏巴什缝合带、西昆仑地体、康西瓦缝合带、巴颜喀喇地体、金沙江缝合带、喀喇昆仑地体、什约克缝合带、科西斯坦-拉达克地体(图 1b; 许荣华等, 1994; 张传林等, 2007)。区域上喀喇昆仑地体被认为是羌塘地体的西向延伸(Yin and Harrison, 2000; 潘桂棠等, 2004)。
喀喇昆仑地体前寒武系到中新生代地层均有出露。三叠系地层主要由中三叠统河尾滩组和上三叠统克勒青河组成，中三叠统河尾滩组主要由深灰色结晶灰岩和砂质灰岩组成(崔建堂等, 2013)，上三叠统克勒青河组为一套岩屑石英砂岩、泥岩、岩屑砂岩，被侏罗系地层不整合。侏罗-白垩系地层主要分布于喀喇昆仑地体的东南部，并被称为林济塘盆地(Pan et al., 2012)，出露地层包括下侏罗统巴工布兰莎组、中侏罗统龙山组、中-上侏罗统红其拉甫组和上白垩统铁龙滩组(崔建堂等, 2013; 计文化等, 2013)。下侏罗统巴工布兰莎组形成在浅海环境下，由从下到上依次为灰色到紫色的砂岩和砾岩、灰色灰岩和石膏层。中侏罗统龙山组由下部砂岩，上部灰岩(层间含有玄武-安山岩夹层)组成(董连慧等, 2015)。中-上侏罗统红其拉甫组由生物碎屑，泥质灰岩层组成。铁龙滩组地层下部为一套粗碎屑岩、砂砾岩，上部为一套褐红色灰岩(图 2)。
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图 2 甜水海-多宝山地质剖面图 1-中侏罗统龙山组；2-上白垩统铁隆滩组；3-砂岩；4-砂砾岩；5-灰岩；6-辉长岩；7-地质界线；8-角度不整合界线；9-剖面走向；10-断层；11-产状 Fig. 2 Geological section map of the Tianshuihai-Duobaoshan 1-Middle Jurassic Longshan Fm.; 2-Upper Cretaceous Tielongtan Fm.; 3-sandstone; 4-sand conglomerate; 5-limestone; 6-gabbro; 7-geological boundary; 8-angular unconformity; 9-section strike; 10-fault; 11-occurrence |
喀喇昆仑地体出露的岩浆岩主要为晚三叠世花岗岩、侏罗纪火山岩和白垩纪花岗岩类。晚三叠世岩浆岩主要分布在林济塘盆地以北靠近巴颜喀拉地体和慕士塔格的局部地区，岩石类型包括二云母花岗岩(~210Ma)、二长花岗岩(217~220Ma)、黑云二长花岗岩(230Ma)、花岗闪长岩(232Ma)(康磊等, 2015)，形成于喀喇昆仑地体与巴颜喀喇地体挤压碰撞的构造背景(姜春发, 1992; 刘训等, 1997; 毕华等, 1999; 张传林等, 2005; 韩芳林, 2006; 杨文强等, 2011; 杨文强, 2013; 宋志冬, 2013; 乔耿彪等, 2015; 魏小鹏等, 2017; Zhang et al., 2019)。侏罗纪火成岩发育在林济塘盆地龙山组地层中，岩石类型以玄武质和安山质为主，有玄武岩、辉长岩与辉绿岩、安山岩与粗面安山岩，形成于弧后盆地的构造背景，主要分布于宝塔山、岔路口、兴山、吉利山等地区(Li et al., 2019)。早白垩世花岗闪长岩和英云闪长岩呈北西西向分布于红其拉甫-卡拉其古-乔戈里峰-温泉一带(潘桂棠, 2004; 李荣社等, 2008; Pan et al., 2012; Jiang et al., 2014)，岩体年龄为103~121Ma(Heuberger et al., 2007; Ravikant et al., 2009; Jiang et al., 2014; Li et al., 2016)。晚白垩世花岗岩以林济塘南侧潘公的层状和片麻状花岗岩(73Ma, Ravikant et al., 2009)和红其拉甫的闪长岩(100Ma, Li et al., 2016)为主。白垩纪花岗岩类被认为是什约克洋片北向俯冲于喀喇昆仑地体之下形成的岩浆弧(丁道桂等, 1996; 姜春发等, 2000; Bhutani et al., 2003; 李荣社等, 2008)。
喀喇昆仑地体大型断裂主要包括喀喇昆仑断裂、乔尔天山断裂和龙木错-郭扎错断裂(图 1b)。喀喇昆仑断裂带是喜马拉雅山脉北部重要的右旋走滑断裂带，断裂带大略呈NW-SE走向，平行于喜马拉雅西部山脉，其分布从冈仁波齐(神山)至帕米尔长约1200km，形成时代约23Ma(李海兵等, 2006, 2007; Chevalier, 2019)。林济塘盆地为弧后盆地(李荣社等, 2008; Pan et al., 2012; Li et al., 2019)，位于喀喇昆仑地体的东南部，被龙木错-郭扎错断裂截切，并被乔尔天山断裂穿切。喀喇昆仑地体褶皱构造发育，其中林济塘中生代盆地侏罗系地层发生强烈褶皱(图 2, 崔建堂等, 2013; 计文化等, 2013)，并被上白垩统铁龙滩组不整合。上白垩统铁龙滩组地层整体较平缓。林济塘中生代盆地不整合包括平行不整合和角度不整合，其中主要发育的是上白垩统铁龙滩组地层角度不整合于中侏罗统龙山组地层之上(图 2)，中侏罗统龙山组平行不整合于下侏罗统巴工布兰莎组之上。
2 岩体地质与岩石学特征甜水海辉长岩发现于林济塘盆地北部(图 1c)。研究区出露的地层以中侏罗统龙山组和上白垩统铁龙滩组为主。中侏罗统龙山组与上白垩统铁龙滩组间为不整合接触，龙山组主要包括下部砂岩和上部灰岩(层间含有玄武-安山岩夹层)(董连慧等, 2015)。铁龙滩组地层下部为一套粗碎屑岩、砂砾岩，上部为一套褐红色灰岩(图 3a, b)。
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图 3 甜水海地区地质图(a)和野外照片(b) 1-第四系；2-白垩系铁龙滩组灰岩；3-白垩系铁龙滩组砂岩；4-侏罗系龙山组灰岩；5-辉长岩岩体；6-岩体界线；7-采样点；8-角度不整合接触界线 Fig. 3 Geological map (a) and filed photograph (b) of the Tianshuihai area 1-Quaternary; 2-limestone of Cretaceous Tielongtan Fm.; 3-sandstone of Cretaceous Tielongtan Fm.; 4-limestone of Jurassic Longshan Fm.; 5-gabbro pluton; 6-pluton boundary; 7-sample collecting points; 8-angular unconformity |
辉长岩岩体侵位于侏罗系龙山组灰岩中，呈透镜状断续出露，整体沿北西-南东向延伸，宽可达72m，长累计约305m(图 3b)。经追索辉长岩岩体并未侵入到铁龙滩组灰岩中。
辉长岩手标本呈灰绿色，中粒结构，块状构造(图 4a)。主要造岩矿物为单斜辉石、斜长石、钾长石、角闪石和黑云母。其中单斜辉石含量25%~35%(透辉石含量15%~20%、普通辉石含量10%~15%)，呈半自形-自形短柱状；斜长石含量45%~50%，呈半自形板柱状；角闪石含量5%~10%，呈他形粒状；钾长石含量3%~5%，呈半自形-自形柱状；黑云母含量2%~5%，呈片状(图 4b)。辉长岩呈典型的辉长结构，其中斜长石长宽比大于5:1，可见聚片双晶；辉石粒径0.2~0.5mm，可见完全解理。
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图 4 甜水海辉长岩手标本(a)及正交偏光镜下照片(b) Pl-斜长石；Di-透辉石；Aug-普通辉石 Fig. 4 Hand specimen (a) and microscopic picture under cross-polarized light (b) of gabbro from the Tianshuihai area Pl-plagioclase; Di-diopside; Aug-augit |
针对辉长岩样品开展了系统的地球化学、同位素年代学研究。样品采集按等距离贯穿岩体完成，采集的样品较新鲜。
对辉长岩岩石样品进行主、微量测试(5件：16TSH06-3、16TSH06-4、16TSH06-7、16TSH06-8、16TSH06-11)、全岩Rb-Sr-Sm-Nd同位素测试(16TSH06-4、16TSH06-7)及锆石LA-ICP-MS U-Pb测年(16TSH05)。
3.1 主量与微量元素样品主量与微量元素分析测试工作均在在中国科学院矿产资源研究院重点实验室完成。主量元素的测定采用X-射线荧光光谱法(XRF)：首先称取0.5g样品放入坩埚，然后加入适量硼酸高温熔融成玻璃片，最后在日本岛津公司生产的顺序式X射线荧光光谱仪(XRF-1500)上采用外标法测定氧化物含量，分析误差小于5%。主量元素分析结果列于表 1，并借助Geokit 2012(路远发, 2004)计算程序得到岩石的主要岩石化学参数。
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表 1 甜水海地区辉长岩主量元素(wt%)和微量元素(×10-6)分析结果 Table 1 Major element (wt%) and trace element (×10-6) analysis results of gabbro from the Tianshuihai area |
微量元素的测定采用ICP-MS法，称取40mg样品用酸溶法制成溶液，然后在ICP-MS Element Ⅱ上进行测定，其精度为:元素含量小于10×10-6的误差小于10%，大于10×10-6的误差小于5%。具体分析方法参见李献华等(2002)。岩石稀土元素及微量元素测试结果列于表 1，运用Geokit 2012(路远发, 2004)对稀土元素数据采用原始地幔数据(Sun and McDonough, 1989)进行标准化，并计算主要的稀土元素参数。
3.2 锆石U-Pb测年锆石U-Pb同位素定年分析在武汉上谱分析科技有限责任公司利用LA-ICP-MS分析完成。详细的仪器参数和分析流程见(Zong et al., 2017)。GeolasPro激光剥蚀系统由COMPexPro102 ArF193nm准分子激光器和MicroLas光学系统组成，ICP-MS型号为Agilent 7700e。激光剥蚀过程中采用氩气为补偿气、氦气作载气以调节灵敏度，二者在进入ICP之前通过一个T型接头混合，激光剥蚀系统配置有信号平滑装置(Hu et al., 2015)。本次分析的激光束斑和频率分别为32μm和5Hz。U-Pb同位素定年和微量元素含量处理中采用锆石标准91500和玻璃标准物质NIST 610作外标分别进行同位素和微量元素分馏校正。每个时间分辨分析数据包括大约20~30s空白信号和50s样品信号。对分析数据的离线处理(包括对样品和空白信号的选择、仪器灵敏度漂移校正、元素含量及U-Pb同位素比值和年龄计算)采用软件ICPMSDataCal(Liu et al., 2008, 2010)完成。锆石样品的U-Pb年龄谐和图绘制和年龄加权平均计算采用Isoplot/Ex_ver3(Ludwig, 2003)完成。数据处理结果见表 2。
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表 2 甜水海地区辉长岩(样品16TSH05)中锆石LA-ICP-MS U-Pb定年结果 Table 2 LA-ICP-MS zircon U-Pb dating results for gabbro (Sample 16TSH05) from the Tianshuihai area |
全岩Sr-Nd同位素样品的前处理在中国科学院岩石圈演化国家重点实验室的超净实验室完成，同位素比值测量在中国科学院地质与地球物理研究所固体同位素地球化学实验室的MAT-262型热电离质谱仪上完成，详细的Sr-Nd同位素测定流程遵照Li et al. (2012)和Yang et al. (2010)。分别采用146Nd/144Nd=0.7219和86Sr/88Sr=0.1194校正Nd和Sr同位素比值。国际标样NbS-987和JNdi-1用来评估测量数据收集过程中的仪器稳定性，本次测定过程中NbS-987的87Sr/86Sr=0.710236±0.000010 (2σ, n=4)，JNdi-1的143Nd/144Nd=0.512124±0.000012(2σ, N=4)。USGS标样BCR-2被用来监测分析流程的精确度，本次测量过程中，BCR-2的87Sr/86Sr=0.715021±0.000015，143Nd/144Nd=0.512635±0.000011，和应用TIMS以及MC-ICP-MS方法得到的测量结果(Li et al., 2012)在误差范围内保持一致。对岩石样品按其岩浆锆石U-Pb年龄(102Ma)推算它们的(87Sr/86Sr)i、(143Nd/144Nd)i、εNd(t)等值。同位素分析结果及参数列于表 3。
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表 3 甜水海辉长岩Sr、Nd同位素组成 Table 3 Sr-Nd isotopic composition of gabbro from the Tianshuihai area |
辉长岩样品SiO2含量变化范围为49.84%~51.52%，平均含量50.4%，属于基性岩类。Al2O3含量为15.07%~15.32%，平均含量15.22%。MgO含量为8.00%~9.15%，平均含量8.43%。TiO2含量为1.31%~1.34%，平均含量1.33%。K2O含量为0.47%~0.64%，平均含量0.56%。Na2O含量为2.89%~3.14%，平均含量3.06%。镁指数Mg#为40.9~42.9，平均含量41.6。全碱(Na2O+K2O)含量为3.49%~3.72%，铝饱和指数A/CNK为1.16~1.43，里特曼指数σ为1.53~2.01(表 1)。
在TAS图解中，样品落在亚碱性辉长岩范围内，与岩相学特征一致(图 5a)。在SiO2-K2O(图 5b)和FAM(图 5c)图解中，样品大多位于钙碱系列区域。从Ta/Yb-Th/Yb图解中(图 5d)可看出，甜水海辉长岩产于板内环境。在Zr/Sm-(La/Sm)N和Y/Pb-(La/Sm)N图解中，甜水海辉长岩样品多落入地壳附近(图 6)。
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图 5 甜水海辉长岩TAS图解(a, 据Middlemost, 1994)、SiO2-K2O(b, 据Peccerillo and Taylor, 1976; Middlemost, 1985)、FAM(c, 据Irvine and Baragar, 1971)及Ta/Yb-Th/Yb图解(d, 据Pearce, 1982) 詹姆斯罗斯岛弧后盆地玄武岩数据引自Košler et al. (2009)；冲绳弧后盆地玄武岩数据引自Shinjo et al. (1999)；N-MORB、E-MORB、OIB数据引自Sun and McDonough (1989) Fig. 5 TAS diagram (a, after Middlemost, 1994), SiO2 vs. K2O diagram (b, after Peccerillo and Taylor, 1976; Middlemost, 1985), FAM diagram (c, after Irvine and Baragar, 1971) and Ta/Yb vs. Th/Yb diagram (d, after Pearce, 1982) of gabbro from the Tianshuihai area The values of James Ross Island BABB from Košler et al. (2009); the values of Okinawa BABB from Shinjo et al. (1999); the values of N-MORB, E-MORB and OIB from Sun and McDonough (1989) |
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图 6 甜水海辉长岩Zr/Sm-(La/Sm)N (a)和Y/Pb-(La/Sm)N (b)图解 PM值据Hofmann (1988)；MORB、OIB、UCC、LCC、BC值据Taylor and McLennan (1985) Fig. 6 Zr/Sm vs. (La/Sm)N (a) and Y/Pb vs. (La/Sm)N (b) diagrams of gabbro from the Tianshuihai area PM data from Hofmann (1988); MORB, OIB, UCC, LCC, BC data from Taylor and McLennan (1985) |
辉长岩样品稀土元素含量(∑REE)为83.0×10-6~92.2×10-6，平均为86.6×10-6。δCe的平均值为0.92(表 2)。在球粒陨石标准化稀土元素配分图上(图 7a)，样品呈富集轻稀土元素(LREE)、贫重稀土元素(HREE)的右倾型配分型式((La/Yb)N=6.17~7.39)且轻重稀土分馏比较明显(LREE/HREE=5.21~5.78，均值5.46)。重稀土斜率较为平坦((Gd/Yb)N=1.76~2.03，均值1.90)，而轻稀土斜率相对较大((La/Sm)N=2.56~2.77，均值2.65)，稀土配分曲线整体与洋岛玄武岩(OIB)、詹姆斯罗斯岛弧后盆地玄武岩整体趋势相似(图 7)。样品中均具有富集La、Th、Nd与Tb，亏损Rb、Ce、Y、Sr与P元素的特征，除U、Th外，样品的微量元素蛛网图与OIB、詹姆斯罗斯岛弧后盆地玄武岩相似。
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图 7 甜水海辉长岩球粒陨石标准化稀土元素配分模式图(a, 标准化值据Boynton, 1984)和原始地幔标准化微量元素蛛网图(b, 标准化值据Sun and McDonough, 1989) N-MORB、E-MORB和OIB值据Sun and McDonough (1989)；詹姆斯罗斯岛弧后盆地玄武岩数据引自Košler et al. (2009)；阿留申弧玄武岩数据引自Stelling et al. (2002), George et al. (2003), Jicha et al. (2004), Jicha and Singer (2006), Finney et al. (2008)及Mangan et al. (2009) Fig. 7 Chondrite-normalized REE patterns (a, normalization values after Boynton, 1984) and primitive mantle-normalized trace element spidergrams (b, normalization values after Sun and McDonough, 1989) diagrams of gabbro from the Tianshuihai area Data for the N-MORB, E-MORB and OIB from Sun and McDonough (1989); the values of James Ross Island BABB from Košler et al. (2009); the compositions of Aleutian arc basalts compiled from Stelling et al. (2002), George et al. (2003), Jicha et al. (2004), Jicha and Singer (2006), Finney et al. (2008) and Mangan et al. (2009) |
鉴于甜水海辉长岩岩体侵位于中侏罗统龙山组地层中，岩体侵位时间应晚于中侏罗世(164Ma)。结合锆石CL图像(图 8a, b)和锆石年龄将甜水海辉长岩锆石分为两类。一类为岩浆锆石：以半自形-自形、长柱状为主，锆石多呈灰-灰白色、透明，晶形较完整，CL图像显示该类锆石具有清晰的震荡环带，是典型的岩浆成因(Hoskin and Schaltegger, 2003)，震荡环带较清晰且年龄较小的一组锆石(G01~G14)；另一类为继承锆石：以半自形-不规则次圆状、长柱状为主，大小不一，锆石多呈灰-灰黑白色、透明，晶形较好，少数锆石具碎裂现象，根据年龄分布和CL图像将其分为两组。第一组为岩浆成因的继承锆石(G15~G46)，CL图像亦具有清晰的震荡环带，年龄分布不集中；第二组继承锆石(G47~G52)CL图像显示其表面呈灰黑色且环带不发育。
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图 8 甜水海辉长岩锆石CL图像及U-Pb定年测点位置(a、b)和锆石U-Pb年龄谐和曲线(c、d) 1/99.3代表 1号锆石测点206Pb-238U年龄为99.3Ma，红圆圈为测点位置；年龄 < 1000Ma的锆石，以206Pb/238U年龄表示，年龄>1000Ma的锆石，以207Pb/206Pb年龄表示 Fig. 8 Cathodoluminescence (CL) images and measuring positions of zircon grains (a, b), concordia diagrams of zircon U-Pb ages (c, d) from gabbro in the Tianshuihai area 1/99.3 represents that the 206Pb-238U age of the No.1 zircon is 99.3Ma, the red ellipses show the LA-ICP-MS analysis location; zircons age < 1000Ma, was applied in 206Pb/238U apparent age, zircons age >1000Ma, was applied in 207Pb/206Pb apparent age |
第一类锆石(G01~G14)，锆石Th、U与Pb含量分别为178×10-6~795×10-6、285×10-6~1078×10-6、18×10-6~78×10-6，Th/U比值在0.4~1.0之间，显示出岩浆锆石的特点(表 2; 图 8a; Hoskin and Schaltegger, 2003)，锆石206Pb/238U年龄在99.3~107Ma之间，平均年龄为102±1Ma(图 8d, MSWD=0.92; n=14)；第二类锆石为岩浆侵位过程中从围岩捕获的继承锆石：第一组锆石(G15~G46)U、Th与Pb含量分别为17×10-6~1288×10-6、5×10-6~1104×10-6、4×10-6~439×10-6，Th/U比值在0.3~1.3之间，其年龄数据较分散且跨度很大，从三叠纪到新元古代均有出现(232~986Ma)；第二组锆石(G47~G52)呈短柱状、浑圆状，锆石U、Th与Pb含量分别为121×10-6~471×10-6、61×10-6~289×10-6、96×10-6~584×10-6，Th/U比值在0.4~1.1之间，207Pb/206Pb年龄为1167~2450Ma(图 8b)。
4.3 全岩Sr-Nd同位素样品(16TSH06-4、16TSH06-7)的(87Sr/86Sr)i值和(143Nd/144Nd)i值分别为0.70577、0.706398和0.512203、0.512210。(87Sr/86Sr)i值均高于原始地幔初始值(0.7045; DePaolo, 1988)，εNd(t)值分别为-5.8、-5.9，(143Nd/144Nd)i值低于原始地幔值(0.512638; Jacobsen and Wasserburg, 1980), 岩石的地幔模式年龄tDM在1775~1811Ma之间(表 3)。在(87Sr/86Sr)i-(143Nd/144Nd)i图解(图 9)上样品均落入Ⅰ型富集地幔与甜水海地壳之间的区域。
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图 9 甜水海辉长岩(87Sr/86Sr)i-(143Nd/144Nd)i图解(底图据Zindler and Hart, 1986) PREMA值据Hofmann (1988)；MORB、OIB、BSE值据Taylor and McLennan (1985).卡拉其古、阿然保泰和红其拉甫花岗岩Sr-Nd值据Jiang et al. (2014)；红其拉甫闪长岩和花岗闪长岩Sr-Nd值据Li et al. (2016)；麻扎石英闪长岩和花岗闪长岩Sr-Nd值据Liu et al. (2015) Fig. 9 (87Sr/86Sr)i vs. (143Nd/144Nd)i diagram of gabbro from the Tianshuihai area (base map after Zindler and Hart, 1986) PREMA data from Hofmann (1988); MORB, OIB, BSE data from Taylor and McLennan (1985); granite Sr-Nd data of Kalaqigu, Aranbaota and Hongqilafu from Jiang et al. (2014); diorite and granodiorite Sr-Nd data of Hongqilafu from Li et al. (2016); quartz diorite and granodiorite Sr-Nd data of Mazha from Liu et al. (2015) |
由于甜水海辉长岩侵位于中侏罗统龙山组地层中，而没有侵入到上白垩统铁龙滩组，说明岩体形成于中侏罗世之后晚白垩世之前。辉长岩第一类岩浆锆石14个测点(G01~G14)给出了一组加权平均年龄为102±1Ma(MSWD=0.92, n=14)，可代表辉长岩岩体的年龄。与喀喇昆仑天文点一带辉长岩的年龄(105±4Ma)一致(菅坤坤等, 2018)，表明早白垩世晚期的基性岩浆活动在区域上是较广泛的。
第二类第一组岩浆成因锆石(G15~G46)为继承锆石，根据其年龄范围将其分为两个年龄段进行解释：(1)第1年龄段继承锆石的年龄为412~986Ma，主要集中区间为412~548Ma。与康西瓦一带的三十里营房年龄为447Ma的俯冲型石英闪长岩(崔建堂等, 2006)及许志琴等(2004)在康西瓦一带发现的年龄为428~492Ma的加里东期孔兹岩系相对应，属于加里东期构造旋回岩浆作用的产物(朱杰等, 2016)。(2)第2年龄段继承锆石的年龄为232~341Ma，记录了晚古生代及中生代喀喇昆仑与西昆仑地体的构造演化过程。可能产生于250~240Ma喀喇昆仑与西昆仑地体沿着康西瓦缝合带碰撞(张传林等, 2005)和240~200Ma期间的后碰撞伸展环境(张传林等, 2005; 康磊等, 2012; Liu et al., 2015; Zhang et al., 2019)。
第二类第二组年龄较老的锆石(G47~G52)，结晶年龄主要有1167~1751Ma、1988~2450Ma两个阶段，与前人关于甜水海地区的古老基底测年结果范围基本相一致(图 1b; 计文化等, 2011; 朱杰等, 2016; 胡军等, 2016, 2017; 魏小鹏等, 2017)，进一步证实了甜水海地块存在前寒武纪结晶基底。
5.2 辉长岩的岩浆源区特征与构造背景甜水海辉长岩具负的εNd(t)值(2个样品分别为-5.8、-5.9)，富集La、Pb、Th与Nd，亏损Rb、Nb、Ta、Ce、Pr与P，在(87Sr/86Sr)i-(143Nd/144Nd)i图解(图 9)上样品均落入Ⅰ型富集地幔与甜水海地壳之间的区域，Sc值介于18.7×10-6~20.3×10-6之间(Frey and Prinz, 1978)的特征，这些特征说明辉长岩样品的源区可能为富集型岩石圈地幔。
甜水海辉长岩中大量继承锆石的发育意味着岩浆在上升过程中有陆壳物质的混入与混染，这一结论还被下面的现象与资料所佐证：(1)样品中Sr含量(195×10-6~226×10-6)显著高于地幔值(17.8×10-6; Taylor and McLennan, 1985; McCulloch and Gamble, 1991; Hawkesworth et al., 1993)，而辉长岩样品的源区为富集型岩石圈地幔；(2)地壳中Ce/Pb < 15，而典型地幔Ce/Pb=25±5(Hofmann, 1986)，本文辉长岩样品中Ce/Pb为9.72~11.3，处于地壳和典型地幔之间；(3)洋中脊玄武岩和洋岛玄武岩Nb/U比值为47±10，而大陆地壳和原始地幔Nb/U平均值分别为8.93、33.59(Taylor and McLennan, 1985; Hofmann, 1986; 曹圣华等, 2006; 莫宣学和潘桂棠, 2006; 邓晋福等, 2015)，本文辉长岩样品中Nb/U为26.6~29.1，处于大陆地壳和原始地幔Nb/U平均值之间；(4)样品中La/Nb比值在1.33~1.47之间，均大于1(袁超等, 2005; 夏林圻等, 2006, 2008)；另外，微量元素蛛网图(图 7)显示辉长岩样品中Pb的含量位于上地壳和洋岛玄武岩之间；(5)在Zr/Sm-(La/Sm)N和Y/Pb-(La/Sm)N图中(图 6)，样品的(La/Sm)N值位于地壳和地幔之间，这意味着甜水海辉长岩岩浆受到地壳混染。
甜水海辉长岩缺少明显的Nb、Ta负异常，不同于弧玄武岩(图 7b)。又因为其为钙碱性系列岩石(图 5b, c)，源区为富集岩石圈地幔，所以排除其形成于洋中脊环境。甜水海辉长岩具有较高的Th/Yb值(位于1.07~1.16之间)，在Ta/Yb-Th/Yb图投点位于板内玄武岩区，与弧后盆地玄武岩的地化性质相似(图 5d)，结合其含有大量碎屑锆石及前寒武纪基底，排除其形成于洋岛环境(图 5d)。甜水海辉长岩与正常的弧后盆地玄武岩有明显的差异，其元素和同位素特征与弧后盆地玄武岩的亚族(詹姆斯罗斯岛弧后盆地玄武岩)类似(图 5d, Košler et al., 2009)，詹姆斯罗斯岛弧后盆地玄武岩为弧后盆地拉开前的玄武岩(Shuto et al., 2004, 2006)，具有明显富集LREE、LILE和HFSE的特征(Gorring et al., 2003; Guivel et al., 2006; Košler et al., 2009; Shuto et al., 2006; Sinton et al., 2003; Wang et al., 2007)，不同于MORB(图 5d、图 7)，这种玄武岩与成熟弧后盆地玄武岩有明显的差异。在FAM图解(图 5c)中甜水海辉长岩与詹姆斯罗斯岛弧后盆地玄武岩投点位于钙碱性系列，不同于以冲绳弧后盆地玄武岩为代表的正常弧后盆地玄武岩，可能与甜水海辉长岩形成于伸展背景的初始阶段有关。所以判定甜水海辉长岩形成于陆内伸展体制。即102Ma时，甜水海地区处于伸展构造背景。这与甜水海辉长岩侵位于褶皱的中侏罗统龙山组灰岩中并被上白垩统铁龙滩组砂砾岩和灰岩不整合的特征所显示的晚白垩世时甜水海地区为海相盆地环境、为伸展构造背景的结论是一致的。
综上，甜水海辉长岩岩浆的源区可能为富集型岩石圈地幔，其侵位过程中经历了地壳混染作用，形成于板内伸展背景。
5.3 区域构造演化林济塘盆地侏罗系灰岩地层和龙山组地层中玄武岩建造的发育，说明侏罗纪林济塘海盆形成于伸展构造背景。鉴于林济塘盆地西侧乔戈里峰-温泉一带早白垩世岩浆弧的发育(潘桂棠, 2004; 李荣社等, 2008; Pan et al., 2012; Jiang et al., 2014)，可以认为侏罗纪-早白垩世早期的林济塘盆地为弧后盆地(李荣社等, 2008; Pan et al., 2012)，形成于什约克洋片的北向俯冲。林济塘盆地中侏罗统龙山组地层发生褶皱并被上白垩统铁龙滩组不整合(缺失早白垩世地层)，说明喀喇昆仑地体在早白垩世发生造山作用，这意味着什约克洋片在早白垩世期间曾发生平板俯冲作用。这种造山作用与45Ma时美国西部洋底岩石圈的浅俯冲导致区域岩浆活动停止并形成Sevier、Laramide造山带(Yonkee and Weil, 2015)及与南美安第斯低角度俯冲造山相似(Elger et al., 2005; Sobolev and Babeyko, 2005; Cawood et al., 2009)。甜水海地区102Ma辉长岩的发育意味着在102Ma时该地区又进入伸展构造背景。上白垩统铁龙滩组砂砾岩与灰岩的发育意味着较大海盆的形成。林济塘盆地南侧潘公等地晚白垩世时弧花岗岩的发育(100~73Ma, Ravikant et al., 2009)说明晚白垩世时林济塘盆地仍为弧后盆地。基于此，我们认为喀喇昆仑地体中生代的构造演化经历了3个阶段(图 10)：
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图 10 甜水海地区中生代构造演化模式图 Fig. 10 Tectonic evolution model in Mesozoic of the Tianshuihai area |
(1) J至K1早期正常弧盆演化阶段(图 10a)：什约克洋片向北正常俯冲，形成中生代喀喇昆仑地体岩浆弧及林济塘弧后盆地。林济塘弧后盆地在中-晚侏罗世时强烈拉伸并发育玄武岩建造。
(2) K1早期至102Ma平板俯冲与造山阶段(图 10b)：什约克洋片开始由向北的正常俯冲变为平板俯冲，导致弧岩浆活动停止(Yonkee and Weil, 2015; Dailey et al., 2018)、侏罗系地层发生褶皱以及下白垩统地层缺失。这种挤压作用可能与平板俯冲导致的区域挤压与隆升有关，与南美安第斯低角度俯冲造山相似。
(3) 102Ma至K2正常弧盆演化阶段(图 10c)：102Ma时，什约克洋片俯冲角度开始变陡，林济塘地区再次发生弧后扩张形成伸展盆地，深部软流圈的物质伴随着地壳在张应力下开始减薄发生快速上涌，大量的热使上覆的岩石圈地幔发生减压部分熔融，在102Ma时形成甜水海辉长岩。在晚白垩世时完全变为海相盆地，发育海相地层。
6 结论新发现的甜水海辉长岩锆石LA-ICP-MS U-Pb年龄为102±1Ma，形成于早白垩世晚期。辉长岩中大量古老继承锆石的发育意味着研究区存在前寒武纪基底，且岩浆经历了强烈的地壳混染。甜水海辉长岩富集LREE及部分LILE，相对亏损HREE，形成于板内伸展的构造背景。其发育意味着林济塘地区早白垩世晚期再次进入伸展与弧后盆地发育阶段。喀喇昆仑地体中生代经历了三阶段的构造演化，即侏罗纪-早白垩世早期的正常俯冲与弧盆演化、早白垩世的平板俯冲与造山阶段、及晚白垩世的正常俯冲与弧盆演化。
致谢 论文相关野外地质调查及样品采集工作得到了新疆地矿局第八地质大队范廷宾总工程师及全体项目组工作人员的大力支持；室内研究工作得到了中国科学院地质与地球物理研究所主、微量实验室、固体同位素地球化学实验室的大力帮助与支持；两位审稿人百忙之中对本文的审阅并提出建设性问题及建议，使得本文能更加规范、完整，内容上也更加严谨、充实。在此向他们表示衷心感谢！
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