2016, Vol. 32
2. 西南石油大学地球科学与技术学院, 成都 610500
2. School of Geoscience and Technology, Southwest Petroleum University, Chengdu 610500, China
夹持于西伯利亚板块与华北-塔里木板块之间的中亚造山带是全球范围内显生宙陆壳增生最显著的地区(Şengör et al., 1993; Jahn et al., 2004; Xiao et al., 2003, 2004a, b, 2010)。中亚造山带的形成被认为与古亚洲洋的演化历史息息相关，具有长期复杂多样的增生历史，并保留了古微陆块、蛇绿杂岩、岛弧岩浆岩、弧前或弧后盆地等证据(Mossakovsky et al., 1993; Şengör et al., 1993; Badarch et al., 2002; Xiao et al., 2003, 2010; Kroner et al., 2007, 2010, 2011; Glorie et al., 2011; Xu et al., 2013)；位于内蒙中部的索伦缝合带被认为是古亚洲洋的最终闭合位置(Xiao et al., 2003; Windley et al., 2007; Chen et al., 2009; Jian et al., 2010)。古亚洲洋始于新元古代-早古生代的南北双向俯冲最有可能在晚二叠世至早三叠世消亡，并导致西伯利亚板块与华北板块拼合形成索伦缝合带(Xiao et al., 2003, 2009; Li, 2006; Shen et al., 2006; Miao et al., 2007; Jian et al., 2008, 2010; Chen et al., 2009; Feng et al., 2013)；但由于这条庞大的增生带组成复杂而存在巨大争议(Xu and Chen, 1997; 徐备等, 2001; Xu et al., 2013；Shi et al., 2013)。
华北板块北缘中段发育大量中亚造山带的增生历史息息相关的晚古生代岩浆岩，它们在形成过程中赋存的信息能够为探索古亚洲洋或中亚造山带南缘的演化历史提供制约。遗憾的是，先前的研究多集中在对侵入体的研究上(章永梅等, 2009; 张拴宏等, 2004; Zhang et al., 2007a, 2009a, b; 柳长峰等, 2010, 2011; Ma et al., 2013; 王挽琼等, 2013)，而较少关注该区的同期火山岩。“苏吉组”为1:25万白云鄂博幅(内蒙古自治区地质调查院，2002①)正式确立的火山岩填图单元，在白云鄂博一带下部为中性安山岩或者安山质凝灰岩，上部为流纹质火山岩；最新的区域地质调查显示，该火山岩带向东延伸至少至化德一代，但岩性略有差异。本文将以内蒙古商都县屯垦队-西井子一带新识别的二叠纪苏吉火山岩为研究对象，通过系统的岩石学、地球化学、锆石年代学及锆石Hf同位素体系的讨论，探索其成因与源区特征，从而对中亚造山带的演化提供约束。
①内蒙古自治区地质调查院. 2002. 1:25万白云鄂博幅区域地质调查报告
2 区域地质内蒙中部自南向北被划分为华北克拉通北缘、白乃庙岛弧、温都尔庙俯冲增生杂岩、索伦缝合带等几个大地构造单元(图 1a，据Xiao et al., 2003)。研究区位于集宁北部商都县西井子镇一带，属华北克拉通北缘，以发育大规模晩古生代岩浆岩为特征(图 1b)。赤峰-白云鄂博断裂(徐尼乌苏断裂)将其与由温都尔庙俯冲增生杂岩和白乃庙岛弧所构成的南部造山带区分开来(Xu et al., 2013)。
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图 1 华北克拉通北缘中段大地构造单元划分简图(a, 据Xiao et al., 2003修改)及晩古生代岩浆岩分布简图(b) Fig. 1 Sketch tectonic map (a, modified after Xiao et al., 2003) and sketch map showing distribution of the Late Paleozoic magmatic rocks (b) in the middle part of northern margin of the NCC |
华北拉通北缘主要由早前寒武纪基底及中新元古界以来的沉积盖层组成，并发育大量海西期岩浆岩。中新元古界白云鄂博群通常被认为是华北克拉通北缘中-新元古代大陆边缘裂谷带的一部分，也是研究区最为发育的前寒武纪沉积地层(Pt2-3B)；早古生界发育一套含动物化石的阿牙登组(∈-O)海相碎屑岩-灰岩建造；晚古生界先后形成了富含植物化石的拴马桩组陆相碎屑岩和苏吉火山岩。详细的地质填图显示，中新元古界白云鄂博群和早古生界阿牙登组并非原地地层，而是呈推覆体形态覆于晚古生界拴马桩组和苏吉火山岩之上，从而在研究区形成构造窗-飞来峰交错产出的构造格局(图 2)。
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图 2 研究区地质简图 Fig. 2 sketch map of the study area |
苏吉火山岩呈近东西向条带状展布，常常整合覆于拴马桩组陆相碎屑岩之上，并被稍晚的花岗岩侵位(图 3a)。苏吉火山岩以爆发相的流纹质凝灰岩、流纹质角砾凝灰岩为主，夹有数层喷溢相的流纹岩；受后期推覆构造影响，部分岩石发生糜棱岩化。除此之外区域上还分布少量同期的安山岩-玄武安山岩。
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图 3 苏吉火山岩的产出及岩石学特征 (a)二叠纪花岗岩侵入苏吉火山岩；(b)流纹质凝灰岩；(c)糜棱岩化凝灰岩；(d)流纹岩. Q-石英; Kfs-钾长石; Pl-斜长石 Fig. 3 Outcrop and petrological characteristics of Suzy volcanic rocks (a) Permian granitic intruded into Suzy volcanic; (b) rhyolitic tuff; (c) mylonitized tuff; (d) rhyolite. Q-quartz; Kfs-K-feldspar; Pl-plagioclase |
流纹质凝灰岩，风化面灰黄至浅肉红色，新鲜面浅灰色-灰白色，晶屑或岩屑晶屑凝灰结构。晶屑主要为石英、钾长石和斜长石，晶屑呈棱角分明的不规则粒状、三角状等(图 3b, c)，晶屑大小1 mm左右，块状构造；局部因受剪切作用改造，而呈现弱定向现象(图 3c)；部分岩石中含有数量不多的同质火山角砾。
流纹岩，风化面浅褐色，新鲜面灰白色，斑状结构，块状构造(图 3d)。斑晶由钾长石、斜长石和石英组成，斑晶含量5%~15%，其中钾长石半自形-自形，粒径2~3 mm；石英多呈浑圆状，常发育熔蚀结构，粒径1 mm左右；基质为微粒长英质矿物或呈玻璃质，局部见球粒结构。
4 分析方法锆石分选在河北省廊坊市区域地质调查所实验室按照标准流程完成，样品机械粉碎之后首先进行重力分选，然后进行磁选，最后在双目镜下将锆石挑选出来。锆石制靶、反射光、透射光、阴极发光图像均在中国地质科学院地质研究所完成。锆石U-Pb定年和Lu-Hf同位素测试是在中国地质科学院矿产资源研究所成矿作用与资源评价实验室的Neptune型多接收等离子质谱和Newwave UP 213激光剥蚀系统上进行的，测定时使用锆石国际标样GJ-1和Plesovice作为参考，Lu-Hf分析点与U-Pb定年分析点为同一位置。具体的测试流程参照侯可军等(2007)。
样品主量元素、微量元素和稀土元素的测定均在广州澳实矿物实验室完成。主量元素采用X射线荧光光谱法(XRF)测定，试样煅烧后加入Li2B4O7-LiBO2助熔物，经充分混和后，置入自动熔炼仪中，使之在1000 ℃以上熔融；熔融物倒出后形成扁平玻璃片，再用X荧光光谱仪分析，相对误差低于5%。微量元素和稀土元素采用等离子体质谱法(ICP-MS)，将试样加入到LiBO2熔剂中混合均匀，在1000 ℃以上的熔炉中熔化。熔液冷却后，用硝酸定容，再用等离子体质谱仪(ICP-MS)分析。
5 分析结果 5.1 地球化学研究区苏吉火山岩的主量、微量元素含量及相关参数见表 1。苏吉火山岩具富硅(SiO2=71.10%~76.01%)，钾(K2O=4.81%~5.97%)含量，低镁(MgO=0.08%~0.27%)、铁(Fe2O3T=1.36%~2.63%)，钛(TiO2=0.09%~0.18%)特征，并具有较低的Mg# (Mg#=8.2~17.9)。在A/NK-A/CNK图解中，落入过铝质岩石范围内(图 4a)；TAS图解中全部落入流纹岩范围内，属钙碱性系列(图 4b)。
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表 1 苏吉火山岩的主量元素(wt%)、稀土和微量元素(×10-6)组成 Table 1 Major (wt%), rare earth and trace element (×10-6) for Suzy volcanic rocks |
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图 4 苏吉火山岩的A/NK-A/CNK图解(a, 据Shand, 1943)和TAS图解(b, 据Le Bas et al., 1986) Fig. 4 A/NK vs. A/CNK (a, after Shand, 1943) and TAS (b, after Le Bas et al., 1986) classification diagrams for Suzy volcanic rocks |
苏吉火山岩的稀土总量中等(∑REE=167×10-6~245×10-6)，轻重稀土分馏较强(LREE/HREE=7.5~11.2)，Eu负异常明显(δEu=0.29~0.57)，具有一致的右倾型稀土配分曲线(图 5a)。在微量元素蛛网原始地幔标准化蛛网图中，所有样品表现出较好的一致性。大离子亲石元素K、Rb、Ba含量较高，而Sr亏损；P元素以及高场强元素Nb、Ta、Ti强烈亏损(图 5b)。
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图 5 苏吉火山岩的球粒陨石标准化稀土元素配分图(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) Fig. 5 Chondrite-normalized REE patterns (a, normalization values after Boynton, 1984) and primitive mantle-normalized trace element spider diagrams (b, normalization values after Sun and McDonough, 1989) for the Suzy volcanic rocks |
我们共采取了3件定年样品，分别为流纹质凝灰岩(P2B8-2)、糜棱岩化流纹岩(P3N2-1)及流纹岩(P28N9-1)(表 2)。
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表 2 苏吉火山岩LA-ICP-MS锆石U-Pb定年分析结果 Table 2 Zircon U-Pb dating results for Suzy volcanic rocks |
流纹质凝灰岩取自屯垦队乡北东约6 km处，采样坐标为：41°49′23.27″N、113°29′15.76″E；糜棱岩化流纹岩采自研究区南部大拉子乡南山，采样坐标为：41°40′41.02″N、113°19′39.50″E；流纹岩采自研究区中部西井子镇南5 km处，采样坐标为：41°45′53.23″N、113°13′49.45″E(图 2)。
3件样品中的锆石具有基本一致的特征，它们普遍呈较自形的短柱状，长轴一般在100~200μm，长宽比在1:1.5~1:2之间。阴极发光图像特征显示(图 6)，它们均发育密集的岩浆震荡环带，暗示它们为岩浆结晶成因。
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图 6 苏吉火山岩的锆石阴极发光图像 红色圆圈代表测试位置，红色数字代表U-Pb测试序号，黄色数字代表Lu-Hf测试序号 Fig. 6 CL images of zircons for Suzy volcanic rocks Red circles are analyses spots of zircon grains, the analytical number of U-Pb age is red and Hf isotope is yellow |
锆石图像特征及较高的Th/U比值都表明我们获得的年龄数据能够反映苏吉火山岩的成岩年龄。样品P28N8-1中含有较多明显偏老的锆石颗粒，应为岩浆运移过程中的捕获锆石。去除其中的捕获锆石后，3件样品的加权平均年龄分别为267±2 Ma，272±2 Ma和270±3 Ma(表 2、图 7)，代表了苏吉火山岩的活动时代。
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图 7 苏吉火山岩的锆石U-Pb谐和图 Fig. 7 U-Pb concordia diagrams of zircon for Suzy volcanic rocks |
3件样品的锆石Hf同位素体系同样具有基本一致的特征。3件样品锆石的176Hf/177Hf比值介于0.282128~0.282449之间，εHf(t)值在-17.3~-5.9之间，它们的单阶段模式年龄(tDM1)和两阶段模式年龄(tDM2)分别为1173 Ma~1649 Ma，1667~2386 Ma (表 3，图 8)。
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表 3 苏吉火山岩的锆石Hf同位素分析结果 Table 3 Zircon Hf isotopic data for Suzy volcanic rocks |
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图 8 苏吉火山岩的锆石εHf(t)-锆石年龄图解 Fig. 8 εHf(t) vs. zircon ages plots for Suzy volcanic rocks |
所测试3件样品中的锆石呈自形柱状，并具有十分发育的岩浆震荡环带和较高的Th/U比值，暗示它们是岩浆结晶成因。因此我们获得的267~272 Ma的年龄结果代表锆石了的结晶年龄，也表明研究区内苏吉火山岩形成于早-中二叠世。
华北克拉通北缘中段晩古生代岩浆活动频繁，自固阳至承德平行于其北缘边界分布着大量石炭-二叠纪侵入体。如：位于承德一带的喇叭沟门闪长岩体(王惠初等，2007)，隆化片麻状花岗闪长岩体及闪长岩体(张拴宏等, 2004; Zhang et al., 2007b)；位于集宁北部的铁砂盖石英闪长岩体和花岗闪长岩体(王挽琼等, 2013)，位于固阳北的银号闪长岩(张维和简平, 2012)，白云鄂博地区的黑云母花岗岩-二长花岗岩等(范宏瑞等, 2009)等。这些侵入体的形成时代多介于晚石炭-二叠纪之间。显然，苏吉火山岩与这些中酸性侵入体是同时代的产物。
苏吉火山岩区域上显示出与晚古生代侵入体密切共生并更靠近华北克拉通北缘边界的特征(图 1b)。苏吉火山岩首先是通过区域地质填图在白云鄂博一带识别出来的(内蒙古自治区地质调查院, 2002)。最近的研究揭示白云鄂博一带苏吉火山岩的形成时代介于278~264 Ma，并可能向东延伸至四子王旗以东地区(Zhang et al., 2016)。最新的区域地质填图成果显示(吉林大学地质调查研究院, 2015①)，沿华北克拉通北缘边界(赤峰-白云鄂博断裂南缘)自白云鄂博以西开始，向东一直延伸至研究区以东的化德境内可能分布着一条数百千米的晩古生代火山岩带。
①吉林大学地质调查研究院. 2015. 1:25万集宁市幅区域地质调查报告
6.2 岩石成因与源区特征研究区内苏吉火山岩具有较高SiO2、Al2O3含量和极低的Mg#，轻稀土元素和大离子亲石元素相对富集，高场强元素Nb、Ta、Ti明显亏损的特征，这些特征表明它们的原始岩浆可能源自地壳物质的部分熔融；其极高的A/CNK比值(1.06~2.11)则暗示他们具有S型花岗岩的特征；Eu和Sr的亏损则暗示岩浆在演化过程中可能出现过长石的分离结晶作用或他们的原始成分就具有这种特征。苏吉火山岩的εHf(t)均呈较高的负值且变化范围较大(-17.9~-5.9)并具有相当古老的Hf二阶段模式年龄(1662~2507 Ma)，与研究区南部集宁一带的华北克拉通早前寒武纪基底岩石形成时代相当(Peng et al., 2010, 2011, 2012; 蔡佳等, 2014)，暗示它们的原始岩浆主要源自古老地壳物质(华北克拉通基底)的部分熔融。最近的研究数据揭示，集宁一带的华北克拉通基底中的花岗质成分的岩石通常也表现出Nb、Ta、P、Ti以及Sr的强烈亏损(Peng et al., 2010, 2012)，进一步证明研究区苏吉火山岩的原始岩浆极有可能源自华北克拉通基底岩石的部分熔融。研究区南侧华北克拉通基底的组成复杂多样(Peng et al., 2010, 2011, 2012；蔡佳等, 2014)，是导致苏吉火山岩εHf(t)变化范围较大的直接原因；而华北克拉通基底中变质沉积岩(孔兹岩系)的部分熔融可能是导致苏吉火山岩具有极高的A/CNK比值的原因。华北克拉通北缘赋存大量具有古老Hf、Nd模式年龄或含有古老锆石残核的晩古生代中酸性火成岩(王惠初等, 2007；Ma et al., 2013; 王惠初等, 2007; Xiao et al., 2003, 2009; Zhang and Zhao, 2013; Zhang et al., 2007a, 2009a, b, 2011, 2016)，暗示古老地壳物质的部分熔融是华北克拉通北缘晚古生代火成岩的主要源区。研究区以北兴蒙造山带(赤峰-白云鄂博断裂以北)内的同期火山岩多具有相对年轻或更复杂的Nd和Hf模式年龄(Zhang et al., 2016)。
6.3 地质意义华北克拉通北缘因大量存在晚古生代以准铝质为主的钙碱性中-酸性侵入体而被认为当时可能存在一个由古亚洲洋向南俯冲形成的活动大陆边缘(Ma et al., 2013; 王惠初等, 2007; Xiao et al., 2003, 2009; Zhang and Zhao, 2013; Zhang et al., 2007a, 2009a, b, 2016; Chen et al., 2015)；又由于其含有大量早前寒武纪同位素地质记录而被倾向于认为是安第斯型的大陆边缘弧(Zhang et al., 2007b, 2009a, b, 2016; Ma et al., 2013; Zhang and Zhao, 2013)。地震影像和地表构造形迹均显示华北克拉通北缘边界发育巨型叠瓦状喜马拉雅型逆冲推覆-褶皱体系(李刚等, 2012, Li et al., 2013; Zhang et al., 2014)，并将其归因于晚二叠纪-早三叠纪中亚造山带同碰撞或后碰撞期地壳的持续收敛(Zhang et al., 2014)。区域地质填图显示，区内的苏吉火山岩呈构造窗形态展布在这套逆冲推覆体系的下盘(图 1)，暗示苏吉火山岩的形成时代早于该逆冲推覆系，即早于同碰撞-后碰撞期。
在Rb-Y+Nb图解中(图 9a)，苏吉火山岩主要落入火山弧花岗岩区域，少许落在火山弧花岗岩与同造山界线附近，进一步指示它们形成于俯冲阶段(大陆边缘弧)或俯冲向同碰撞的转折期。苏吉火山岩古老的Hf二阶段模式年龄指示它们主要源自华北克拉通基底组分的部分熔融，与前述钙碱性中-酸性侵入体特征相似(Ma et al., 2013; 王惠初等, 2007; Xiao et al., 2003, 2009; Zhang and Zhao, 2013; Zhang et al., 2007a, 2009a, b)，表明它们与这些侵入体的源区特征一致，也进一步表明苏吉火山岩是大陆边缘弧成因的。
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图 9 苏吉火山岩的Rb-Y+Nb图解(a, 据Pearce et al., 1984)和形成模型(b, 据Annen et al., 2006; Chen et al., 2016改) Fig. 9 Rb vs. Y+Nb plot (a, after Pearce et al., 1984) and a schematic diagram showing the mechanism in formation (b, modified after Annen et al., 2006; Chen et al., 2016) of the Suzy volcanic rocks |
与之形成鲜明对比的是，赤峰-白云鄂博断裂以北的火山岩多具有相对年轻或多变的Hf模式年龄(Zhang et al., 2016)，指示当时的岩浆作用十分复杂。同样的，这条位于华北克拉通北缘(赤峰-白云鄂博断裂以南)的晩古生代中酸性侵入体中常常含有大量镁铁质微粒包体，这些包体的地球化学参数指示它们很难直接由古老地壳部分熔融而成(章永梅等, 2009；Ma et al., 2013; 王挽琼等, 2013)，暗示当时存在来自不同源区岩浆的混合作用。安第斯型活动陆缘通常具有复杂的岩浆增生机制，俯冲洋壳和沉积物、地幔楔以及陆壳物质等都可以作为其岩浆作用的物质来源；这些性质各异的原始岩浆又在不同的演化条件下形成了不同的岩浆岩组合(Barbarin, 1999; Patiño Douce, 1999; Kay et al., 2005; Haschke et al., 2006; Mamani et al., 2010; Gómez-Tuena et al., 2014)。Annen et al.(2006)建立的地质模型能很好的解释华北克拉通北缘大面积分布的中酸性火成岩的成因(Zhang et al., 2009b, 2016; 图 9b)。首先，由古亚洲洋俯冲形成的富水玄武质岩浆底侵并对下地壳加热引起广泛的地热异常；底侵玄武质岩浆在分离结晶过程中不断的释放水和热从而诱发大规模上覆古老陆壳物质的部分熔融。随后，这些熔体向上迁移并在上地壳汇集；在这一过程中由玄武质岩浆经不完全结晶演化的残余组分会注入到这些陆壳熔体中，进而诱发岩浆不同程度的混合。
7 结论(1) 同位素年代学证据表明苏吉火山岩是早中二叠世岩浆作用的产物，三件样品的锆石U-Pb分别为267±2 Ma、272±2 Ma和270±3 Ma。详细的地质填图显示，平行赤峰-白云鄂博断裂在华北克拉通北缘分布一条晩古生代火山岩带。
(2) 锆石Hf同位素特征显示，苏吉火山岩的原始岩浆主要来源于华北克拉通基底岩系的部分熔融，孔兹岩系在其中起到重要作用。
(3) 苏吉火山岩的形成与古亚洲洋向南俯冲有关，可能形成于安第斯型活动大陆边缘。
致谢 感谢中国地质科学院矿产资源研究所张晗博士、侯可军博士在锆石定年、Lu-Hf同位素测试方面给予的帮助。感谢吉林大学地球科学学院葛文春教授、孙德有教授和天津地质矿产研究所李承东研究员对本文进行了细致的评审并提出了宝贵意见。| [] | Annen C, Blundy JD, Sparks RSJ. 2006. The genesis of intermediate and silicic magmas in deep crustal hot zones. Journal of Petrology , 47 (3) :505–539. |
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