内蒙古镶黄旗哈达庙地区晚古生代中酸性侵入岩的年代学、地球化学、Sr-Nd同位素组成及其地质意义**

刘军 武广 李铁刚 王国瑞 吴昊LIU Jun, WU Guang*, LI TieGang, WANG GuoRui and WU Hao

1. 中国地质科学院矿产资源研究所，国土资源部成矿作用与资源评价重点实验室，北京 1000372. 中国地质大学，北京 1000831. MLR Key Laboratory of Metallogeny and Mineral Assessment, Institue of Mineral Resources, Chinese Academy of Geological Sciences, Beijing 100037, China2. China University of Geosciences, Beijing 100083, China2013-08-20 收稿, 2013-11-30 改回.

中亚造山带是全球显生宙陆壳增生与改造最显著的大陆造山带(Jahnetal., 2000; Wuetal., 2000; Badarchetal., 2002; Xiaoetal., 2003; 何国琦和朱永峰，2006)，同时也是世界上最重要的铜、金、钼、铅锌及稀有稀土金属矿产地之一(洪大卫等，2003；Chenetal., 2007；杨富全等，2007；周振华等，2010； Zhouetal., 2012; 刘军等，2013a，b，c；毛景文等，2013)，是研究造山带大陆生长、构造演化及成矿作用过程的天然场所。目前，中亚造山带最终碰撞的时间、地点及方式等问题仍存在争议，在缝合带位置上，存在索伦山-林西地区(Wang and Liu, 1986)、二连-贺根山地区(曹从周等，1986；engöretal., 1993)和西拉木伦-长春-延吉一线(Wuetal., 2002)等观点，在缝合时间上，大多数学者认为我国北山或包头以西地区的缝合时代为石炭纪末，东部西拉木伦河一带的缝合时代为二叠纪末(毛景文等，2002a，b，2005；高俊等，2006；Li, 2006；李锦轶等，2006，2013)，但也有部分学者主张缝合时间为三叠纪末(Xiaoetal., 2008)。区域上发育不同时代(早古生代、晚古生代、早中生代)、不同岩石类型花岗岩类(与俯冲、碰撞有关的花岗岩类，与造山后伸展有关的A型花岗岩)，已经构成我国重要的成矿带(童英等，2010)。

目前，研究者更多地关注于中亚造山带内部的岩浆-热液活动及相关成矿作用(毛景文等，2002a，b，c；Yangetal., 2006, 2009；Zhangetal., 2008, 2010; Liuetal., 2012；张作衡等，2012；刘军等，2010，2013a，b，c)，但对中亚造山带与华北克拉通结合部岩浆岩的侵位时代、地球化学属性及源区性质缺乏研究。内蒙古镶黄旗哈达庙地区中酸性侵入岩位于华北板块北缘的温都尔庙俯冲-增生杂岩带内，区域内构造岩浆活动频繁，其中夹杂着众多前寒武纪地块、高压变质岩和条带状蛇绿岩带，正确认识该区域内各期岩浆-热液活动的时空关系及其成因对探讨古亚洲洋在华北克拉通北侧的俯冲过程及其闭合时限具有重要意义。本课题组对哈达庙地区进行了1:1万区域地质填图工作，掌握了本区详细的第一手基础地质资料。本文针对哈达庙地区的花岗斑岩和闪长岩开展了岩石学、岩石地球化学、同位素地球化学和SHRIMP锆石U-Pb定年的工作，探讨了中酸性侵入岩的地球化学性质、成因及其形成的地球动力学背景。

1 区域地质及岩体特征

哈达庙地区位于内蒙古中部镶黄旗西北约20km处，大地构造位置位于温都尔庙俯冲-增生杂岩带内(图1)。区内出露地层较简单，主要由第四系和下二叠统包特格组构成。第四系主要为砂砾、粉砂和风成砂，分布于研究区的东部、东北部及区内的3条冲沟内。下二叠统包特格组主要为中细粒长石石英砂岩，夹少量的粉砂岩和泥岩，局部见含砾砂岩，主要分布在研究区的西南部(图2a)。区内岩浆岩分布广泛，主要有闪长岩、花岗闪长岩、二长花岗岩、花岗斑岩及少量隐爆火山角砾岩脉和流纹岩脉(图2a, b)。闪长岩在区内大面积分布，侵入下二叠统包特格组。二长花岗岩和花岗闪长岩区内少量出露，侵入闪长岩或包特格组中。花岗斑岩脉分布较广泛，呈近东西向侵位到闪长岩及包特格组内，延长3km左右，近直立状产出，宽约10～30m，最宽处可达60m。隐爆角砾岩脉分布于西北部，主要由33条规模不等的隐爆火山角砾岩脉构成。流纹岩脉多沿近东西向构造断裂分布，成群出现(聂凤军和张洪涛，1989)。本区的断裂构造主要受研究区南部的赤峰-白云鄂博断裂控制，晚期遭到中生代北东向断裂及褶皱构造活动的影响(聂凤军等，1989)。

图1 内蒙古中部及其邻区区域地质图(底图据鲁颖淮等，2009)Fig.1 Geological map of central Inner-Mongolia and adjacent area (after Lu et al., 2009)

图2 哈达庙地区地质简图(a)和采样剖面图(b)Fig.2 Sketch geological map (a) and sampling profile (b) of the Hadamiao area

花岗斑岩 呈斑状结构，斑晶主要为石英(7%～9%)、钾长石(3%～5%)和斜长石(<1%)。石英：他形粒状，聚合晶体出现，大小在0.5～1.0mm，有的与钾长石组成聚合斑晶。钾长石：自形、半自形乃至他形均见，见卡钠复合双晶，有的与先晶出钾长石构成聚斑晶，大小在0.4～1.0mm。斜长石：半自形，板状，有聚片双晶，见绢云母化，大小在0.4～0.6mm。基质呈细晶结构，由微细晶粒的长石、石英他形晶组成，大小在0.04～0.10mm。岩石整体有轻微绢云母化。

闪长岩 半自形粒状结构，主要由斜长石(65%～75%)、角闪石(15%～20%)、黑云母(5%～8%)及石英(<3%)组成。斜长石：半自形板状，发育聚片双晶，双晶纹较宽，为中长石。斜长石晶体破碎，并存在不同程度的绢云母化，大小在0.9～2.7mm。角闪石：半自形柱状、粒状，多色性微弱，有解理，但解理纹较细，聚片双晶发育，大小在0.6～1.9mm。黑云母：片状，多色性不明显，解理发育，干涉色因绿泥石化和绿帘石化而显异常蓝色，大小在0.3～1.5mm。石英：他形粒状，表面干净，有裂纹，大小在0.3～0.8mm。

2 样品采集和分析方法

在综合分析区域地质背景及野外地质调查基础上，对闪长岩及花岗斑岩露头进行了采样(图2a，b)，采集年代学测试样品2件、岩石地球化学测试样品11件。锆石分选工作在河北省区域地质调查队完成，通过常规的重选和磁选进行初选，然后在双目镜下挑出晶形和透明度较好的锆石，将锆石置于环氧树脂中，磨制约一半大小，使锆石内部暴露，用于阴极发光及随后的SHRIMP U-Pb分析，锆石阴极发光在中国地质科学院矿产资源研究所电子探针研究室完成，锆石SHRIMP U-Pb分析在北京离子探针中心SHRIMPⅡ上完成，详细分析流程和原理参考Williams (1998)、刘敦一等(2003)和简平等(2003)的文章，一次离子流强度约7.5nA，加速电压约10kV，样品靶上的离子束斑直径约25～30μm。应用澳大利亚国家地调局标准锆石TEM(417Ma)进行元素间的分馏校正。应用RSES(澳大利亚国立大学地学院)标准锆石SL13(年龄572Ma；U含量238×10-6)标定所测锆石的U、Th和Pb含量。数据处理采用国际标准程序ISOPLOT(ver 3.0)。表1中所列单次测量的数据点的误差均为1σ。采用206Pb/238U年龄，其加权平均值具95%的置信度。

岩石主量、稀土和微量元素测试由国土资源部廊坊地球物理地球化学勘查研究所完成。其中全岩主量元素采用XRF分析，稀土和微量元素采用ICP-MS分析。主量元素分析精度优于3%，稀土和微量元素分析精度优于5%。Sr、Nd同位素分析在中国科学院广州地球化学研究所超净实验室进行前处理。Sr和REE分离采用AG50-8X离子交换柱，分别收集Sr和REE解析液；REE的分离采用HDEHP交换柱，收集Nd解析液，测试工作在北京大学造山带实验室完成，测试所用实验仪器为VG Axiom HR-MC-ICP-MS，Sr和Nd同位素比值用86Sr/88Sr=0.1194和146Nd/144Nd=0.7219作质量分馏校正。实验室对Sr标样NIST SRM 987测定结果为87Sr/86Sr=0.710255±15(2σ)，对Nd标样Shin-Etsu JNdi-1测定结果为143Nd/144Nd=0.512121±9(2σ)。87Rb/86Sr和143Nd/144Nd的测试精度优于2%和0.5%。

3 锆石SHRIMP U-Pb年龄

花岗斑岩(HK3)：锆石为无色到浅褐色，玻璃光泽，透明-半透明，无包体，呈短柱状-长柱状，大小150～300μm，长宽比1.2:1～3:1。从阴极发光图像上看，所有锆石均发育韵律环带和明暗相间的条带结构，显示了岩浆成因锆石的特征(图3a)。锆石U-Pb测年结果见表1，11个点的测试结果显示锆石的Th/U比值介于0.73～1.24之间，均大于0.1，属于典型的岩浆成因锆石。在锆石U-Pb年龄谐和图中(图4a)，所有分析数据都分布在谐和线上及附近，11个点的年龄数据在259.1～277.8Ma之间，206Pb/238U年龄的加权平均值为271±3Ma，MSWD=1.1。

图3 哈达庙地区花岗斑岩和闪长岩中锆石的形态及分析点位图Fig.3 Cathodoluminescence (CL) images of zircons from granite porphyry and diorite from the Hadamiao areaCircles in zircon crystals indicate positions of SHRIMP U-Pb analytical sites. 3-1.1: Number of analyzed spot

闪长岩(H30-19)：锆石呈无色到浅褐色，透明-半透明，无包体发现，为短柱状-长柱状，大小150～300μm，长宽比1.5:1～3:1。锆石阴极发光显示，锆石均发育明暗相间的条带结构及韵律环带结构，显示锆石为岩浆成因的锆石(图3b)。对该样品测定了11个单颗粒锆石，显示锆石的Th/U比值介于0.71～1.24之间，均大于0.1，为典型的岩浆成因锆石。从表1中可以看出，11个点的年龄数据比较集中，分布在259.6～275.4Ma之间，206Pb/238U年龄的加权平均值为267±3Ma，MSWD=1.5(图4b)。

表1哈达庙地区中酸性侵入岩锆石SHRIMP U-Pb测试结果

Table 1 SHRIMP U-Pb isotopic analyses for zircons of intermediate-acidic intrusive rocks from the Hadamiao area

测点号206Pbc(%)U(×10-6)Th(×10-6)232Th238U206Pb*(×10-6)206Pb238U年龄(Ma)207Pb*206Pb*±%207Pb*235U±%206Pb*238U±%HK3-1.10.288649231.1031.9270.9±4.60.049462.00.29272.70.042911.7HK3-2.10.11119314751.2844.7274.8±4.70.050201.20.30142.10.043551.7HK3-3.10.436346631.0823.9275.8±4.90.04953.50.2984.00.043711.8HK3-4.10.453352740.8512.3269.6±4.80.05163.20.3043.70.042711.8HK3-5.10.333993610.9314.8272.1±5.60.04974.20.2954.70.043122.1HK3-6.10.203072760.9311.4271.5±5.20.04913.10.2913.70.043022.0HK3-7.10.202582130.859.35265.9±4.90.05012.80.29083.30.042111.9HK3-8.10.453833420.9214.6277.8±4.90.05063.70.3074.10.044031.8HK3-9.10.056576871.0823.2259.1±4.70.051431.60.29082.40.041021.8HK3-10.10.346727311.1225.0272.6±4.70.050701.70.30202.50.043201.8HK3-11.1—1851350.766.78270.6±5.00.05303.20.3133.70.042861.9H30-19-2.10.217518081.1127.6269.3±4.60.04982.20.29282.80.042661.8H30-19-3.10.007527521.0326.6260.0±4.60.052571.50.29832.30.041161.8H30-19-4.10.611831300.736.55261.9±5.00.05065.60.2895.90.041471.9H30-19-5.10.086436191.0023.1263.7±4.60.051971.70.29922.50.041761.8H30-19-6.10.442211920.898.07267.0±5.00.05004.80.2915.10.042291.9H30-19-7.10.007428121.1326.2259.6±4.50.050921.40.28862.30.041101.8H30-19-8.10.137838591.1328.7268.7±4.60.050031.80.29372.50.042571.8H30-19-9.10.414284020.9715.7268.0±4.70.04942.60.28893.20.042451.8H30-19-10.10.1691111281.2833.9273.4±4.70.050701.60.30292.40.043331.8H30-19-11.10.2088710781.2633.3274.9±4.70.050161.60.30132.40.043571.7H30-19-12.10.464935761.2118.6275.4±4.80.04862.90.2933.40.043651.8

注：误差为1σ；Pbc和Pb*分别为普通铅和放射成因铅;年龄和同位素比值均为测定的204Pb校正

图4 哈达庙地区花岗斑岩和闪长岩锆石的SHRIMP U-Pb年龄谐和图Fig.4 Concordia diagrams of SHRIMP U-Pb zircon dating results for the granite porphyry and diorite from the Hadamiao area

图5 哈达庙地区花岗斑岩和闪长岩的QAP分类图解(a, 据Streckeisen, 1976)和SiO2-K2O关系图解(b, 据Peccerillo and Taylor, 1976)Fig.5 Diagrams of QAP (a, after Streckeisen, 1976) and K2O-SiO2 (b, after Peccerillo and Taylor, 1976) of granite porphyry and diorite from the Hadamiao area

花岗斑岩和闪长岩的锆石U-Pb年龄在误差范围内接近，花岗斑岩的年龄略大于闪长岩的年龄。我们在野外观察中发现花岗斑岩侵位于闪长岩中并沿东西向延伸，因此两类岩体是较短时间间隔内岩浆活动的产物，花岗斑岩的形成应该略晚于闪长岩。

4 岩石地球化学

4.1 主量元素

花岗斑岩的SiO2含量介于74.13%～77.61%，Al2O3含量介于12.40%～14.09%，K2O含量介于2.92%～6.25%，Na2O含量介于1.93%～2.80%，K2O/Na2O介于1.27～3.20，MgO含量介于0.11%～0.87%，Mg#介于22～46，平均值为36，铝饱和指数介于1.11～1.92(表2)。在QAP分类图解(图5a)中，主要落入花岗岩区域，在SiO2-K2O图解(图5b)中，投影点全部落入高钾钙碱性系列区域。花岗斑岩的Mg#平均值略低于太古代TTG(奥长花岗岩-英云闪长岩-花岗闪长岩)的平均值(平均值为43，Drummondetal., 1996; Martinetal., 2005)，接近实验熔体的平均值(平均值为40，Martinetal., 2005)。TTG所具有的低Mg#是加厚的地壳底部含水的玄武质岩石部分熔融的结果(Smithies, 2000; Sheppardetal., 2001; Condie, 2005)，花岗斑岩的低Mg#、Ni和Cr值特征，暗示其形成可能与地壳深部岩石的部分熔融有关。

图6 哈达庙地区花岗斑岩和闪长岩稀土元素配分曲线(a、c, 球粒陨石标准化值据Boynton, 1984)和微量元素原始地幔标准化蛛网图(b、d,原始地幔标准化值据Taylor and McLennan, 1985)Fig.6 Chondrite-normalized REE patterns (a, c, normalization values after Boynton, 1984) and primitive mantle-normalized trace elements spidergrams (b, d, normalization values after Taylor and McLennan, 1985) of granite porphyry and diorite from the Hadamiao area

闪长岩的SiO2含量介于54.43%～60.45%，Al2O3含量介于15.61%～17.49%，K2O含量介于0.36%～2.68%，Na2O含量介于2.15%～2.66%，K2O/Na2O介于0.17～1.00。闪长岩的MgO含量和Mg#值明显高于花岗斑岩，其MgO含量介于3.16%～8.56%，Mg#值介于48～69，平均值为58，铝饱和指数介于0.71～1.12(表2)。在QAP分类图解(图5a)中，投影点落入闪长岩区域，在SiO2-K2O图解(图5b)中，投影点较分散，分布于低钾系列至高钾钙碱性系列的广泛区域。

4.2 微量元素

花岗斑岩稀土元素总量介于79.95×10-6～169.7×10-6，(La/Yb)N介于5.24～9.97，岩石以轻稀土元素富集和重稀土元素亏损为特征(表2和图6a)，δEu介于0.39～0.60，显示铕负异常。一般认为铕负异常是斜长石分离结晶作用的表现。花岗斑岩富集Rb、K、La、Ce和Nd等大离子亲石元素及Th、Zr和 Hf等高场强元素，同时强烈亏损Ta、Nb、Sr、P及Ti，弱亏损Ba(表2和图6b)。

闪长岩稀土元素总量介于34.45×10-6～89.03×10-6，(La/Yb)N介于1.90～5.59，岩石以轻稀土元素富集和重稀土元素亏损为特征(表2和图6c)，δEu介于0.90～1.11，显示正异常或弱负异常，这与花岗斑岩明显的铕负异常形成鲜明对比。从闪长岩到花岗斑岩，稀土元素总量增加，铕负异常越来越明显，轻重稀土元素分馏程度增大，表明岩浆分异程度越来越高。闪长岩富集Rb、K、Sr和La等大离子亲石元素及Zr、Hf等高场强元素，亏损Ba、Ce、Ta、Nb、P和Ti等元素 (表2和图6d)。

5 同位素地球化学

本次选取2件花岗斑岩样品(HK1、HK3)和3件闪长岩样品(H4-186、H30-7、H30-19)进行Sr、Nd同位素测试，结果列于表3。

花岗斑岩ISr介于0.706166～0.707025， 闪长岩ISr介于0.704803～0.706752，均低于现今大陆壳ISr平均值0.719。花岗斑岩的εNd(t)介于-3.92～-2.88，对应的Nd模式年龄为1150～1189Ma。闪长岩的εNd(t)介于-3.62～1.03，略高于花岗斑岩的εNd(t)值，Nd模式年龄介于898～1322Ma，较花岗斑岩的Nd模式年龄稍老，较中亚造山带内花岗岩类的Nd模式年龄(集中在600～800Ma，个别为1000Ma，洪大卫等，2000；邵济安等，2002)偏老。不管是花岗斑岩还是闪长岩，fSm/Nd值均为负值，变化范围不大(-0.49～-0.30)，表明源区的稀土元素Sm、Nd分馏不明显，Nd模式年龄是有效的(Jahnetal., 2000)。

表2哈达庙地区中酸性侵入岩主量元素(wt%)、稀土元素及微量元素(×10-6)分析结果

Table 2 The analyzed data of major (wt%), rare earth and trace (×10-6) elements of intermediate-acidic intrusive rocks from the Hadamiao area

注：A/CNK=Al2O3/(CaO + Na2O + K2O)分子数，Mg#= 100×[Mg2+/(Mg2++ Fe2+)]原子数

表3哈达庙地区中酸性侵入岩Sr-Nd同位素分析结果及主要参数

Table 3 The Sr-Nd isotopic determination data and some major parameters of intermediate-acidic intrusive rocks from the Hadamiao area

样品号Rb(×10-6)Sr(×10-6)87Rb/86Sr(87Sr/86Sr)sISrεSr(t)Sm(×10-6)H4-18690.61635.200.41300.706372±90.704803±98.764.31H30-743.68329.000.38500.708149±60.706687±635.522.52H30-1956.14285.800.56950.708915±90.706752±936.443.89HK1124.18153.202.35030.716087±90.707025±940.394.73HK3114.8085.803.87940.721124±60.706166±628.183.15样品号Nd(×10-6)147Sm/144Nd(143Nd/144Nd)s(143Nd/144Nd)iεNd(t)tDM(Ma)fSm/NdH4-18623.780.109718180.512539±50.512347±51.03898-0.44H30-711.020.138560090.512502±60.512260±6-0.671316-0.30H30-1920.100.117107890.512313±60.512109±6-3.621322-0.40HK128.570.100208640.512266±50.512088±5-3.921189-0.49HK318.270.104500630.512327±50.512142±5-2.881150-0.47

注：εNd=[(143Nd/144Nd)s/(143Nd/144Nd)CHUR-1]×10000,fSm/Nd=(147Sm/144Nd)/(147Sm/144Nd)CHUR-1，tDM=1/λ×ln{1+[(143Nd/144Nd)s-0.51315]/[(147Sm/144Nd)-0.2135]}，(143Nd/144Nd)CHUR=0.512638; (147Sm/144Nd)CHUR=0.1967; (143Nd/144Nd)DM=0.51315; (147Sm/144Nd)DM=0.2135

6 讨论

6.1 岩石成因

图7 哈达庙地区闪长岩的MgO-SiO2图解(底图据McCarro and Smellie, 1998)Fig.7 MgO vs. SiO2 diagram of diorite of Hadamiao area (after McCarro and Smellie, 1998)

哈达庙地区闪长岩与花岗斑岩的稀土和微量元素配分模式相似，暗示两者具有相似的岩浆源区，可能为同源岩浆不同演化阶段的产物。在微量元素蛛网图上两者均表现出富集Rb、K等大离子亲石元素，亏损Nb、Ta、P、Ti等高场强元素，显示出俯冲带岩浆岩的特征(Kelemenetal., 2003)，并暗示两类岩石经历了强烈的结晶分异作用。花岗斑岩和闪长岩均富集Zr、Hf，强烈亏损Nb、Ta，表明其源岩可能来自地壳物质或曾遭遇地壳物质的混染，并受到与大洋板块俯冲有关的流体交代作用(La Flècheetal., 1998；孙德有等，2004)。与正常的岛弧钙碱性安山岩相比(Pearce and Peate, 1995)，哈达庙地区闪长岩具有更高的Mg#、MgO、Cr(30.80×10-6～498.3×10-6)、Ni(20.33×10-6～132.1×10-6)含量，类似于高镁安山岩(图7)(Yogodzinskietal., 1995; Tatsumi, 2001)。这种富镁闪长质岩浆的成因仍存在争议，主要观点有：(1)受交代的富集地幔部分熔融的产物(Smithies and Champion, 2000；; Zhao and Zhou, 2007)；(2)由板片熔体与地幔楔反应形成(Smithiesetal., 2007)；(3)由拆沉下地壳熔融的熔体与地幔橄榄岩反应形成(Gaoetal., 2004)；(4)消减沉积物熔融以及随后的熔体与地幔楔反应而成(Tatsumi, 2001)。无论何种成因机制，富镁闪长岩的形成均需要一个被交代的地幔源区，而差异表现为交代组分来源的不同(尹继元等，2013)。

图8 哈达庙地区花岗斑岩(Y+Nb)-Rb图解(a, 底图据Pearce, 1996)和闪长岩Y-Sr/Y图解(b, 底图据Defant and Drummond, 1993)syn-COLG-同碰撞花岗岩；VAG-火山弧花岗岩；ORG-洋脊花岗岩；WPG-板内花岗岩 Fig.8 (Y+Nb)vs. Rb diagram of granite porphyry (a, after Pearce, 1996) and Y vs. Sr/Y diagram of diorite (b, after Defant and Drummond, 1993) from the Hadamiao areasyn-COLG-syn-collisional granites; VAG-volcanic arc granites; ORG-oceanic ridge granites; WPG-within plate granites

通常认为比较高的ISr值是地壳来源的标志，而εNd(t)为负值则指示源区为地壳或富集地幔。哈达庙地区花岗斑岩和闪长岩的εNd(t)值介于-3.92～1.03，ISr值介于0.704803～0.707025，显示出壳幔混源和新生下地壳的特征。哈达庙地区花岗斑岩和闪长岩的εNd(t)值高于Jahnetal. (1999)归纳出的华北克拉通古老下地壳的εNd(t)值(-44～-32)，略小于东北地区和兴蒙造山带显生宙花岗岩类的εNd(t)值(普遍大于0，平均值为+2.0，吴福元等，1997；洪大卫等，2003)。中亚造山带在晚古生代-中生代发育了大规模低ISr值，正εNd(t)以及年轻tDM模式年龄的花岗岩，它们被认为是在成岩过程中，地幔来源的新生物质加入的结果(赵振华等，1996；周泰禧等，1996; Jahnetal., 2000；洪大卫等，2003；Kovalenkoetal., 2004; Wangetal., 2004；张东阳等，2010)，而在一些具有前寒武纪基底的微陆块上显示负εNd(t)以及较老的tDM模式年龄，反映了部分前寒武纪地壳物质在成岩过程中有比较明显加入(Wuetal., 2000; Chenetal., 2000; 洪大卫等，2003；Jahnetal., 2000, 2004; Kovalenkoetal., 2004)。因此，我们认为哈达庙地区高镁闪长岩是受俯冲板片流体交代的地幔楔部分熔融形成的熔体上升过程中受到地壳物质混染的产物，而花岗斑岩很可能是闪长质岩浆结晶分异的产物。

6.2 对晚古生代古亚洲洋俯冲作用的指示

内蒙古中部地区存在南、北两条蛇绿岩带，其间夹有锡林浩特古陆，其中北部贺根山蛇绿岩与南部索伦山-西拉木伦蛇绿岩分别代表两个洋盆体系，贺根山洋闭合早于中二叠世(徐备和陈斌，1997；Robinsonetal., 1999；施光海等，2003；童英等，2010)，而索伦山-西拉木伦缝合带所代表残留古亚洲洋在早二叠世仍处于俯冲状态(李朋武等，2006；李锦轶等，2007；Jianetal., 2010)。哈达庙地区的闪长岩和花岗斑岩均形成于中二叠世，在(Y+Nb)-Rb图解上，花岗斑岩均位于火山弧花岗岩区域(图8a)，在Y-Sr/Y图解上，闪长岩则基本落入岛弧火山岩区域(图8b)。终上所述，我们认为哈达庙地区中二叠世中酸性侵入岩形成于古亚洲洋的板块俯冲环境。

7 结论

(1)哈达庙地区花岗斑岩和闪长岩的锆石SHRIMP U-Pb年龄分别为271±3Ma和267±3Ma，形成于中二叠世。

(2)哈达庙地区花岗斑岩具有低的Mg#、Ni和Cr值，而闪长岩显示了高MgO、Ni、Cr等富镁闪长岩的特征，高镁闪长岩是受俯冲板片流体交代的地幔楔部分熔融形成的熔体上升过程中受到地壳物质混染的产物，而花岗斑岩为闪长质岩浆结晶分异的产物。在中二叠世，古亚洲洋在哈达庙地区发生过板块俯冲事件。

致谢野外工作得到了中国科学院地质与地球物理研究所张宝林研究员的支持；锆石SHRIMP U-Pb定年工作得到了北京离子探针中心石玉若博士、颉颃强博士的帮助；Sr、Nd同位素分析中，北京大学李文博副教授给予了帮助；中国科学院地质与地球物理研究所朱明田博士参与了野外工作和室内部分测试工作，有色金属矿产地质调查中心解洪晶博士参与了室内部分测试工作；在此一并致以诚挚的感谢。

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