兴蒙造山带前中生代构造单元划分初探*

徐备　赵盼　鲍庆中　周永恒　王炎阳　罗志文

1.北京大学造山带与地壳演化教育部重点实验室，北京大学地球与空间科学学院,北京　1008712.沈阳地质矿产研究所，沈阳　1100341.

1　引言

兴蒙造山带分布于我国内蒙古-东北地区，是东北亚地区的重要构造单元，前人对它及其周边地区已有许多研究成果。例如李春昱等(1982)讨论了我国北方的古板块构造及其与欧亚大陆形成的关系；任纪舜等(1980，1990，1999)提出和阐述了古亚洲洋构造域、古中华陆块群、亲西伯利亚陆块群、萨彦-额尔古纳造山系和天山-兴安造山系以及南蒙古-兴安、温都尔庙和吉黑造山带等各级构造单元；王鸿祯(1981)划分了额尔古纳早加里东褶皱带、兴安海西褶皱带、内蒙晚加里东褶皱带和松辽中间地块，并提出西拉木伦河对接带的概念。何国琦和邵济安(1983)、唐克东等(1983)、唐克东(1992)和邵济安(1991)都对古亚洲洋演化和东亚陆缘构造做了详细的分析。Xu and Chen (1993,1997)根据在苏尼特左旗的1:5万填图提出内蒙地区存在早古生代“双冲造山带”的认识。Xiaoetal.(2003，2009)认为古亚洲洋南部存在多个古生代加积楔，大洋俯冲一直持续到晚古生代末。Li(2006)识别了额尔古纳地块、南戈壁-扎兰屯地块和布列亚-佳木斯古板块，划分出温都尔庙-翁牛特早古生代造山带和索伦山-吉中晚二叠纪造山带。张兴洲等(2012)主张布列亚-佳木斯古板块和华北板块之间在早石炭世之前就连为一体，之后再与额尔古纳-兴安地块(含内蒙西部)拼合形成东北亚大陆板块。王成文等(2009)根据古生物及地层学研究提出东北地区曾存在统一的“佳蒙古陆”，并于晚古生代末或早中生代初沿西拉木伦-长春缝合带与华北板块拼合。刘永江等(2010)认为古亚洲洋向北侧的“佳蒙地块”俯冲，导致晚古生代的弧花岗岩以及贺根山洋的开合。Zhouetal.(2011,2012)根据变质表壳岩的广泛出露，提出东北各地块500Ma时形成以孔兹岩系为特征的统一地块。

近年来更精细的兴蒙造山带构造单元研究集中在东、西部构造单元的识别、造山带结构以及各块体之间拼合带的时空演化等方面。在东部，东北地块群的具体组成及其相互之间的关系是研究和争议的热点问题。例如关于佳木斯地块与松嫩-张广才岭地块在早古生代拼合(Wangetal.,2012; 许文良等,2012)或是中生代拼合(Wuetal.,2011; Zhouetal.,2012; 邵济安和唐克东,1995; 邵济安等,2013)，已经发表了不同的观点；兴安地块是否存在及其与额尔古纳地块拼合带的位置、时代和结构等重要问题得到进一步研究(葛文春等，2007；张丽等，2013)。在西部，一些学者继续阐述索伦-二道井晚古生代加积楔的概念和古亚洲洋晚古生代闭合的观点(Xiaoetal.,2009)；而早古生代“双冲造山带”的构造格局也被进一步扩展(Xuetal.,2013)。

本文根据已有同位素年龄、岩石建造、地层和古生物学等方面的研究成果，结合笔者对兴蒙造山带前中生代构造演化的认识，初步探讨其构造单元划分。

图1　兴蒙造山带构造单元划分Fig.1　Tectonic unit of the Xing-Meng Orogenic Belt

2　中泥盆世之前的构造格局

以前寒武纪微陆块为基本划分单位，以它们之间的缝合带或断裂带为界，将兴蒙造山带中泥盆世之前的构造格局划分为“五块四带”(图1)：从北向南依次为(1)额尔古纳地块；(2)兴安地块；(3)艾力格庙-锡林浩特地块；(4)松辽-浑善达克地块；及(5)佳木斯地块；它们之间的4条边界为：(1)新林-喜桂图缝合带(XXS)；(2)艾力格庙-锡林浩特-黑河缝合带(AXHS)；(3)温都尔庙-吉中-延吉缝合带(WJYS)和(4)牡丹江缝合带(MS)。

2.1　额尔古纳地块

Wuetal.(2011)查明塔河-新林一线西北的满归和碧水等地的侵入岩具有792～927Ma的锆石年龄，Wuetal.(2012)对漠河以南约50km的黑云母斜长片麻岩研究表明其形成于794Ma，通过Hf同位素研究认为其原岩的模式年龄为中太古代，反映中太古代地壳熔融结果。同时在767Ma和1853Ma之间还存在多个碎屑锆石峰值。Zhouetal.(2011a)报道了石榴石夕线石片麻岩496±3Ma的变质年龄和从578±8Ma到1373±17Ma的岩浆事件年龄。Wuetal.(2005)还报道了该地块北缘的504±8Ma和517±9Ma的岩浆事件。Tangetal.(2013)报道了地块中部约737～851Ma的A型花岗岩、辉长岩和辉长-闪长岩，其εHf(t)=+2.5～+8.1，并指出它们产于与Rodinia超大陆裂解有关的伸展环境。张丽等(2013)研究了地块西缘太平林场花岗片麻岩的时代，表明存在840～830Ma、800～780Ma和730～720Ma等3期岩浆热事件。上述特征说明额尔古纳地块具有前寒武纪基底。

2.2　兴安地块

塔河-新林一线东南的前寒武纪地层应属兴安地块。孙立新等(2013a)在十七站地区一带得到花岗质片麻岩的年龄为1854±20Ma，εHf(t)=-8.5～-3.9。本文认为应代表兴安地块存在的古元古代基底。Miaoetal.(2007)报道了韩家园子一带兴华渡口群碎屑锆石最小年龄约为1.0Ga；Zhouetal.(2011b)在韩家园子的兴华渡口群夕线石榴片麻岩中识别了496±3Ma的变质年龄，其锆石核部或碎屑锆石均具有大于6亿年的年龄；李仰春等(2013)报道扎兰屯以西40km处铜矿沟铜山组顶部的最年轻锆石年龄峰值为570±4Ma；周建波等(2014)发现扎兰屯以东约40km的向阳岭地区兴华渡口群中碎屑锆石最小年龄为481±12Ma，并有大量老于530Ma的碎屑锆石；这些资料暗示兴安地块北部韩家园子和南部扎兰屯一带可能有前寒武纪基底。

2.3　艾力格庙-锡林浩特地块

该地块从艾力格庙向东到苏尼特左旗和锡林浩特地区，向西与蒙古境内的Hutag Uul地块相连(Badarchetal.,2002)，向北东是否可与兴安地块相连尚不确定。Yarmolyuketal.(2008)在蒙古境内的Totoshan地区得到片麻状花岗岩中锆石的上交点年龄为952±8Ma，代表原岩形成时代。艾力格庙地区出露的艾力格庙群由石英岩、片麻岩和花岗片麻岩等组成，从石英岩中获得最年轻的碎屑锆石年龄为1151±41Ma(徐备等未发表数据)。孙立新等(2013b)在苏尼特左旗东部发现了年龄为1516±31Ma和1390±17Ma的花岗片麻岩。葛梦春等(2011)报道了锡林浩特地区锡林郭勒杂岩中的表壳岩，并从中获得1005～1026Ma的锆石变质核年龄。上述古老岩石露头东西向断续延伸超过300km，它们代表的前寒武纪地块构成一个重要构造单元。

2.4　松辽-浑善达克地块

该地块代表早古生代AXHS和WJYS两条缝合带之间的稳定地区，东部被松辽盆地、西部被浑善达克沙地所覆盖，呈东宽西窄的三角形，林西县以西到苏尼特左旗南的西半部分急剧变窄。来自松辽盆地东缘的云母片岩显示757±9Ma、843±10Ma的最小年龄峰值(Wangetal.,2014; 权京玉等,2013)；而在南部，裴福萍等(2006)从钻孔岩心中得到的火山角砾岩和变质辉长岩年龄分别为1808±21Ma和1873±13Ma；王颖等(2006)也报道了变质闪长岩SHRIMP锆石年龄为1839±7Ma，这些数据表明松辽地块应存在早前寒武纪基底。在地块东缘铁力地区，Zhouetal.(2012)报道了变质沉积岩约5～23亿年的多组碎屑锆石。在地块西部苏尼特左旗南的浑善达克沙地北缘，温都尔庙群绢云石英片岩的碎屑锆石图谱出现大量5～22亿年的数据(徐备等未发表数据)，提供了地块西部可能具有前寒武纪基底的信息。

2.5　佳木斯地块

目前的研究多限于南部。Wildeetal.(2001,2003)报道了地块南部三道沟及西麻山一带的麻山群具有约500Ma年龄的麻粒岩相变质事件，并根据大量谐合的锆石数据揭示存在1000～1150Ma的重要物源区。颉颃强等(2008)报道了地块南部穆棱地区麻山群混合岩中的岩浆型锆石年龄为843～1004Ma，并认为这些数据指示了新元古代基底的存在。赵海滨等(2009*赵海滨等.2009.佳木斯地块SHRIMP锆石U-Pb年龄的发现及其地质意义.2009年全国岩石学与地球动力学研讨会论文摘要)在黑龙江省太平沟地区获得兴东群斜长角闪岩及侵入的花岗片麻岩锆石SHRIMP年龄分别为913Ma和862Ma。这些研究表明佳木斯地块存在中-新元古代的基底(Zhou and Wilde,2013)。

2.6　新林-喜桂图缝合带(XXS)

该缝合带南西段喜桂图地区的头道桥蓝片岩早有报道(张兆忠等，1986)，最近周建波测定蓝片岩中锆石年龄500～490Ma(未发表资料)，给出了缝合带形成的下限。北东段新林蛇绿岩自下而上主要由变质橄榄岩、层状堆晶岩、辉绿岩席和变玄武岩等组成(李瑞山，1991)。张丽等(2013)发现太平林场花岗片麻岩中变质锆石年龄为494±10Ma，并通过对比额尔古纳和兴安地块花岗岩Hf同位素特征的不同，揭示了缝合带两侧的地球化学差异。近年来有学者据新资料将额尔古纳与兴安地块的边界置于此缝合带，而不再采用德尔布干断裂带作为两者的分界线(Zhou and Wilde,2013)。

2.7　艾力格庙-锡林浩特-黑河缝合带(AXHS)

该缝合带是分隔北部的额尔古纳-兴安地块和南部的松辽-浑善达克地块的界线，经艾力格庙、苏尼特左旗南、锡林浩特南和大石寨地区到黑河一线，以沿线分布的的早古生代岩浆岩、混杂岩和磨拉斯盆地为识别标志。该带以北发育早古生代岛弧岩浆岩带，呈北东向延绵1500余千米(图2)。西段位于艾力格庙-锡林浩特地块的南缘，其发育时间约为490～430Ma(Xu and Chen,1997; Chenetal.,2000; Shietal.,2003; 张炯飞等,2004; 石玉若等,2005; Miaoetal.,2007; Jianetal.,2008; 葛梦春等,2011)。中段见于大石寨地区，以基性火山岩为特征，其形成年龄439±3Ma(Guoetal.,2009)。东段多宝山地区发育以铜山组细碧角斑岩为代表的奥陶纪岛弧火山岩(崔革,1983)和多宝山岛弧花岗闪长岩(485±8Ma,葛文春等,2007; 480±5Ma,崔根等,2008)。该带西段在苏尼特左旗南和艾力格庙地区，分布着由温都尔庙群绢云石英片岩为基质的混杂岩带(Xuetal.,2013; 李瑞彪等,2013)。苏尼特左旗南的色日巴彦敖包组、二连地区泥鳅河组及科尔沁右翼中旗大民山组出现中上泥盆统紫红色粗碎屑岩建造及其与下伏地层的不整合关系，代表造山带内的磨拉斯盆地(图3b-e)。同时这条缝合带也是重要的生物群界线，其北以分布图瓦贝(Tuvaella)动物群为特色，见于多宝山、额尔古纳西、伊尔施和东乌珠穆沁旗等地(内蒙古自治区地质矿产局，1991)。

2.8　温都尔庙-吉中-延吉缝合带(WJYS)

图2　沿主要缝合线发育的早古生代岩浆岩、混杂岩带和磨拉石建造Fig.2　The Early Paleozoic magmatic rocks,ophiolitic mélange and molassic deposition along the main suture zones

这是一条延长1500km以上的早古生代缝合带，从西向东沿图古日格-温都尔庙-正镶白旗-敖汉旗-吉中-延吉一线分布。西段以发育混杂岩和蓝片岩为标志，如在乌拉特中旗以北的图古日格、达尔罕茂明安联合旗北的红旗牧场地区以及著名的温都尔庙地区(唐克东等,1983; 唐克东,1992; 胡骁等,1990; 邵济安,1991; Xuetal.,2013; Shietal.,2013)，蓝闪石和多硅白云母所获39Ar/40Ar年龄为445.6±15Ma，453.2±1.8Ma和449.4±1.8Ma(唐克东,1992; De Jongetal.,2006)。缝合带以南的华北板块北缘发育早古生代岛弧火山岩和深成岩带，从西向东包括图古日格地区包尔汉图群及侵入岩(453～425Ma,Xuetal.,2013)、达茂旗北部(452～446Ma，张维和简平，2008)、温都尔庙地区白乃庙群及侵入岩(474～437Ma,Jianetal.,2008; Zhangetal.,2013)、正镶白旗二长花岗岩(457±11Ma，秦亚等，2013)、敖汉旗地区八当山群火山岩、吉中地区放牛沟火山岩(黄德薰等，1992；476～444Ma，裴福萍等，2011*裴福萍等.2011.华北克拉通北缘东段早古生代陆缘增生带：火成岩年代学与地球化学证据.2011年全国岩石学与地球动力学研讨会摘要集)、张家屯英云闪长岩(443±5Ma，裴福萍等，2014)和延吉地区岩浆岩(裴福萍等未发表资料)。沿缝合带发育晚志留世徐尼乌苏组复理石建造和西别河组砂砾岩，不整合覆于奥陶纪地层或岩浆岩之上(张允平等，2010)，代表早古生代造山带的前陆盆地沉积。

2.9　牡丹江缝合带(MS)

该缝合带位于松辽-浑善达克地块与佳木斯地块之间，尽管目前尚缺乏与碰撞有关的直接证据，但一些学者已经从岩浆作用和沉积作用方面研究了其形成背景和演化过程。许文良等(2012)指出沿松嫩-张广才岭东缘存在南北向展布的早古生代花岗岩，有485Ma、450Ma和425Ma等三个峰期。Wangetal.(2012)识别出缝合带以西存在晚奥陶闪长岩(443～451Ma)、英云闪长岩、流纹岩和中志留世二长花岗岩(424～430Ma)，并据此提出它们可能代表早古生代佳木斯地块向西的俯冲。魏连喜等(2013)报道了晨明地区花岗闪长岩(433±1Ma)和二长花岗岩(432±2Ma)，认为其产生于陆壳加厚环境，与俯冲后的地壳加厚有关。Mengetal.(2010)对松嫩-张广才岭地块汤原地区和佳木斯地块宝清地区下泥盆统碎屑岩的研究也表明，两个地块在413Ma(早泥盆世)之前已经拼合。

根据上述资料，兴蒙造山带各构造单元之间及其与华北板块之间的演化过程有三个重要事件即：500～490Ma时期，由额尔古纳与兴安地块碰撞形成新林-喜桂图缝合带；440～410Ma时期，由松辽-浑善达克地块、华北板块和佳木斯地块碰撞形成温都尔庙-吉中-延吉缝合带和牡丹江缝合带；385～375Ma时期，由松辽-浑善达克地块与额尔古纳-兴安地块碰撞形成艾力格庙-锡林浩特-黑河缝合带。这一过程导致古亚洲洋的消失和兴蒙造山带的形成。

图3　兴蒙造山带泥盆纪沉积盆地及植物化石分布(a)-中晚泥盆世沉积盆地和古植物化石及贺根山蛇绿岩的分布；(b)-泥鳅河组下部巨厚的磨拉斯沉积；(c)-对孤山组复理石地层；(d)-大民山组砾岩；(e)-上泥盆统色日巴彦敖包组砾岩不整合在混杂岩之上；(f)-大民山组植物化石Fig.3　The Devonian sedimentary basins and plant fossils in the Xing-Meng Orogenic Belt(a)-distribution of the Middle-Late Devonian sedimentary basins,plant fossils and Hegenshan ophiolites; (b)-the Niqiuhe Formation molass conglomerate; (c)-the Duigushan Formation flysch; (d)-the Daminshan Formation conglomerate; (e)-the Upper Devonian Seribayanaobao Formation conglomerate overlying mélange; (f)-plant fossil in the Daminshan Formation

3　中泥盆世-石炭纪(400～300Ma)的构造单元

中-晚泥盆世之后，内蒙古及东北地区完成了由古亚洲洋到兴蒙造山带的构造格局转变，开始出现多处陆相及海陆交互相沉积，以含植物化石为标志。石炭纪则广泛分布陆相及滨浅海相碎屑岩和碳酸盐建造，同时发育蛇绿岩、辉长岩、花岗岩及双峰式火山岩等建造，构成多条不同类型的岩浆岩带。根据上述基本特征，可划分陆相盆地、陆表海盆地、蛇绿岩带、侵入岩带等构造单元。

3.1　中晚泥盆世陆相盆地

此类盆地以含植物化石的中-上泥盆统碎屑岩为标志，见于兴蒙造山带西部苏尼特左旗、中部东乌珠穆沁旗、扎鲁特旗、北部海拉尔市、黑河县及东部延寿县及密山县等地。它们虽出露零星，但分布广泛，具重要的构造古地理意义，除前述的色日巴彦敖包组(图3b)、泥鳅河组(图3c)、大民山组(图3d)、那清组之外，还有东乌珠穆沁旗的哈诺敖包组、安格尔音乌拉组、延寿地区的福兴屯组、黑河地区小河里河组等(图3a，内蒙古自治区地质矿产局，1991；黑龙江省地质矿产局，1993)，沉积地层由陆相或海陆交互相砾岩或砂岩组成，含晚泥盆世法门阶植物化石(表1)，向上过渡为滨浅海相。例如在伊敏地区，泥盆系显示紫红色复理石特征(图3f)。在中段科尔沁右翼中旗以北的造山带腹地，大民山组砂岩中新发现了晚泥盆世的植物化石(图3e，王弢等，2012)。

表1兴蒙造山带内晚泥盆世古植物及其分布位置
Table 1Late Devonian plant fossils and their position in the Xing-Meng Orogenic Belt

地区代表性植物分子地层位置时代资料来源苏尼特左旗南①LeptophloeumrhombicumDaw 色日巴彦敖包组晚泥盆世内蒙古区测一队，1965①东乌珠穆沁旗北②Lepidodendropsissp 安格尔音乌拉组晚泥盆世内蒙古区测一队，1973②扎鲁特旗北③Archaeocalamitessp 色日巴彦敖包组晚泥盆世⁃早石炭世王弢等，2012延寿县马鞍山④Protoleptidodendronyanshouense福兴屯组中泥盆世黑龙江省地质矿产局，1993密山县新中⑤Granulatisporitessp 新中组早泥盆世黑龙江省地质矿产局，1993黑河市小河里河⑥Archaeopterissp 小河里河组晚泥盆世黑龙江省地质矿产局，1993鄂温克族自治旗伊敏东⑦Lepidodendropsiscyclostigmatoides对孤山组晚泥盆世黑龙江地质二队，1981③海拉尔市大民山⑧未详细介绍大民山组晚泥盆世内蒙古自治区地质矿产局，1991①②③内蒙古自治区地质局第一区域地质测量队(内蒙古区测一队)．1965．1 20万苏尼特左旗幅区域地质调查报告内蒙古自治区地质局第一区域地质测量队(内蒙古区测一队)．1973．1 20万东乌珠穆沁旗幅区域地质调查报告黑龙江省区域地质调查第二队(黑龙江地质二队)．1981．1 20万塔尔其幅区域地质调查报告

①内蒙古自治区地质局第一区域地质测量队(内蒙古区测一队)．1965．1∶20万苏尼特左旗幅区域地质调查报告
②内蒙古自治区地质局第一区域地质测量队(内蒙古区测一队)．1973．1∶20万东乌珠穆沁旗幅区域地质调查报告
③黑龙江省区域地质调查第二队(黑龙江地质二队)．1981．1∶20万塔尔其幅区域地质调查报告
④内蒙古自治区地质调查院．2004．1∶25万满都拉幅区域地质调查报告

3.2　石炭纪陆相及陆表海盆地

早石炭世兴蒙造山带的锡林郭勒盟北部及兴安盟西北部普遍隆起，其南发育陆相及海陆交互相沉积，见于陈巴尔虎旗-喜贵图旗-额尔古纳右旗一带(如红水泉组)和敖汉旗北部(如朝吐沟组)，局部含砾岩和火山岩，并含植物化石。陆表海盆地分布于苏尼特左旗南部、敖汉旗北部、塔河-沐河地区和吉林省北部，发育陆缘碎屑沉积建造，含大量腕足及珊瑚类化石，沉积不整合覆盖于早古生代造山带之上。晚石炭世兴蒙造山带北部发育陆相盆地，在二连浩特北-白音乌拉-东乌珠穆沁旗-科尔沁右翼中旗一线，以宝力高庙组陆相沉积-火山岩系为代表，向东北延伸至额尔古纳右旗及黑龙江省大部，以类磨拉斯建造不整合超覆在前寒武纪变质基底、早古生代沉积地层及蛇绿岩之上(鲍庆中等，2006)，并出现华夏植物群与安加拉植物群的混生现象(辛后田等，2011)。晚石炭世兴蒙造山带中部则仍发育陆表海盆地，沉积建造以浅海相碳酸盐岩和碎屑岩为主(如本巴图组和阿木山组)，其范围从乌拉特中旗经苏尼特右旗、西乌旗、乌兰浩特等地延伸到吉林省北部。在造山带西缘满都拉地区、南缘敖汉旗至吉林南部一线，发育海陆交互相或陆相盆地，局部出现含煤岩系(如酒局子组)，含华夏植物群化石Calamites(内蒙古自治区地质调查院，2004*内蒙古自治区地质调查院.2004.1:25万满都拉幅区域地质调查报告)。

晚石炭世盆地内火山岩多与局部陆内伸展作用有关，如嫩江地区宝力高庙组中流纹岩为307±2Ma，大石寨组中晶屑凝灰岩为308±2Ma， 并被认为处于陆相伸展背景 (赵芝等，2010a)；曾维顺等(2011)获得大石寨地区大石寨组火山岩年龄为314±1Ma，据此提出晚石炭世应为裂陷盆地；辛后田等(2011)将东乌珠穆沁旗宝力高庙组厘定为320～303Ma的陆相火山-碎屑岩建造；汤文豪等(2011)在苏尼特右旗本巴图组中识别了313～308Ma的双峰式火山岩，并认为研究区应处于裂谷构造环境。在蒙古南部，Yarmolyuketal.(2008)已报道同时代的双峰式火山岩和碱性花岗岩带，可向东延入内蒙古西部地区。

总之，石炭纪地层发育于更为广阔的陆相-海陆交互相-滨海相沉积盆地(内蒙古自治区地质矿产局，1991；黑龙江省地质矿产局，1993)，这类盆地不整合于早古生代造山带之上，属上叠型沉积古地理单元(图4)。

3.3　早石炭世蛇绿岩

见于二连东、贺根山和迪彦庙等地，形成时代为356～333Ma(Jianetal.,2010; 张志诚、宋述光待发表资料)。地球化学分析表明贺根山蛇绿岩形成与软流圈上涌和岩石圈伸展有关的构造背景(Jianetal.,2010)。需要指出的是，早在晚泥盆世，这些蛇绿岩附近已经出现陆相磨拉斯建造，如二连以北的泥鳅河组和苏左旗、阿巴嘎旗一带含植物化石的色日巴彦敖包组(图3)，暗示晚泥盆世之后出现的陆相环境。因此，区域地质背景限定贺根山等地的早石炭世蛇绿岩应发育在陆壳基底之上，代表造山后的一次伸展过程。

3.4　石炭纪侵入岩

这类侵入岩呈面状分布(图4)，包括花岗岩、花岗闪长岩、辉长岩等，其同位素年代约300～330Ma。例如佘宏全等(2012)报道了大兴安岭中北段广布于龙镇、扎兰屯以西和原林以西的二长花岗岩、正长花岗岩、石英闪长岩和黑云母花岗岩等多个岩体。类似的还包括牙克石花岗闪长岩(331±4Ma，赵芝等，2010b)、塔源辉长岩和花岗岩(331～329Ma，冯志强等，2014)、塔河辉长岩(333±8Ma，周长勇等，2005)、内蒙东部锡林浩特地区白音高勒石英闪长岩(313～323Ma，鲍庆中等，2007)、石榴石花岗岩(316±3Ma，施光海等，2003)、内蒙苏尼特左旗巴音宝力道石英闪长岩(309±8Ma,Chenetal.,2000)以及内蒙西部四子王旗辉长岩(331±4Ma，周志广等，2009)等。有些学者已经提出它们产于张性构造环境(鲍庆中等，2007；冯志强等，2014)。根据本文对泥盆-石炭纪古构造格局的认识，它们应与造山后的伸展作用有关。

图4　兴蒙造山带晚古生代岩石-构造单元示意图Fig.4　Late Paleozoic litho-tectonic units of the Xing-Meng Orogenic Belt

4　二叠纪(300～250Ma)的岩石-构造单元

在兴蒙造山带范围内，二叠纪伸展作用形成了多种岩石-构造单元，包括被动裂谷带、主动裂谷带、蛇绿岩带和碱性岩带等。

4.1　早-中二叠世被动裂谷带

早-中二叠世陆内裂谷建造具有三个鲜明特点，一是沉积类型多变，同时期可出现陆相、海相和海陆交互相沉积岩系，二是普遍含植物化石和滨浅海相动物化石，暗示沉积基底具有明显的深度变化、陆相或陆源沉积物丰富和不存在大范围洋壳；三是具有大量双峰式火山岩，说明与伸展背景有关(图4)。据此可将这种沉积建造与火山岩建造均发育的组合归为被动裂谷。

作为该时期火山岩的典型代表，大石寨组(290～270Ma)火山岩广泛分布，从西向东见于西部满都拉、中部林西到东部大石寨等地，构成3条火山-沉积岩带(邵济安等，2014)，其中火山岩显示为双峰式。例如在满都拉地区(图5)，早二叠世火山岩呈近东西向分布，基性岩见于满都拉南部呼吉尔特以北和查干哈达庙，其年龄为279±3Ma和274±1Ma，19个样品SiO2为47%～55%(晨辰等，2012)；酸性岩见于行格宝木太以东，8个样品SiO2为64%～76%(Jianetal.,2010)。鲍庆中等(2006)报道了西乌珠穆沁旗大石寨组的双峰式火山岩并认为与裂谷环境有关。Zhangetal.(2011)根据地球化学研究确定苏尼特左旗西北部的大石寨组为双峰式火山岩并具有高钾钙碱性岩浆特征。

图5　索伦山-满都拉地区地质图(据内蒙古自治区区域地质调查院，2004)Fig.5　Geological map of Suolunshan-Mandula area

沉积环境分析表明该时期陆相沉积和海相沉积交替出现，组成同期异相的古地理面貌。例如晚石炭世-早二叠世宝力高庙组、格根敖包组为陆相地层且均含安加拉植物化石(李文国等，1996; Shenetal.,2006)；而吉林北部发育寿山沟组滨浅海相碎屑-碳酸盐岩沉积，出现北方冷水型和南方暖水型化石的共生(吉林省地质矿产局，1988)。又如内蒙古中部早二叠世额里图组和哲斯组，前者为含植物及淡水动物化石的湖湘沉积，后者则为含“哲斯动物群”的滨浅海相碳酸盐-碎屑岩系(内蒙古自治区地质矿产局，1991；李文国等，1996)。

值得注意的是，在东乌珠穆沁旗东北满都胡宝拉格地区最新发现早-中二叠世华夏植物群分子(周志广等，2010)，这不但暗示此时该区为陆相沉积，而且证实了晚石炭世华夏植物群在该区的衍生(辛后田等，2011)，说明从晚石炭世以来兴蒙造山带北部已经出现华夏植物群与安加拉植物群的混生。

4.2　碱性岩带

已有研究表明，兴蒙造山带内发育南、北两条二叠纪碱性岩带(图4)。北带从额尔古纳地区沿中蒙边界向西到二连浩特北部，由大量早二叠世碱性花岗岩(洪大卫等,1994; Wuetal.,2002)和双峰式火山岩(Zhangetal.,2011)组成。该带向西延至蒙古国南部，与Yarmolyuketal.(2008)所划分的裂谷岩浆岩带连通。南带位于达茂旗-温都尔庙-镶黄旗一线，已报道达茂旗北部花岗岩时代为270～257Ma(范宏瑞等，2009)；镶黄旗南部毕力赫钾长花岗岩时代为264Ma(路彦明等，2012)；克什克腾旗南部碱性岩时代为264～263Ma(江小均等，2011)。另外该带包含大量中二叠世花岗岩、花岗闪长岩及辉长-辉绿岩，共同组成兴蒙造山带南部中二叠世岩浆岩带(图4; Liuetal.,2010; 章永梅等,2009; 王子进等,2013; Caoetal.,2013)。

4.3　索伦山Ligurian型蛇绿岩

索伦山蛇绿岩沿中蒙边界线分布，在我国境内东西向延伸约百余千米，被夹持于早古生代南造山带与北造山带之间的晚石炭世滨海相沉积层序内，变形及变质程度低，未见蛇绿混杂带或高压低温变质带。笔者的地质填图工作显示，索伦山地区的上古生界是一个总体向北推覆的逆冲体系(图5)，由石炭纪本巴图组滨海相碎屑岩岩片(图6a)、二叠及滑塌堆积和浊积岩片及蛇绿岩岩片等组成。蛇绿岩岩片有三类：(1)超基性岩岩片，呈黄褐色外表，碳酸盐化和硅化强烈；(2)玄武岩岩片，见于乌珠尔少布特，具有连续层序，并常被辉长岩脉所穿插(图6b)；(3)含放射虫硅质岩岩片，内部具连续层序，有粗砂岩和玄武岩夹层(图6c)，放射虫化石的时代为中二叠世早期(王惠等，2005)。这些岩片与本巴图组滨海相或晚二叠世浊积岩呈断层关系(图6d)。上述成分、层序和构造侵位特征与西阿尔卑斯的Ligurian型蛇绿岩非常相似(Bernoullietal.,2003)，而后者缘于Adriatic-Iberian大陆板块的伸展作用(Borsietal.,1996)，属陆缘型蛇绿岩，其构造就位与推覆过程有关而与洋壳俯冲无关(Dilek,2003; Dilek and Furnes,2011; Furnesetal.,2013)。综上，索伦山蛇绿岩应代表中二叠世的伸展环境，反映了继早二叠世大石寨期伸展过程之后的又一次岩浆作用。

图6　索伦蛇绿岩及其与围岩关系(a)-石炭纪本巴图组紫红色厚层粗砂岩；(b)-玄武岩被辉长岩脉所侵入；(c)-硅质岩中的砂岩夹层；(d)-蛇绿岩与本巴图组断层接触Fig.6　Suolun ophiolites and relationship with country rocks(a)-the Benbatu Fm.red thick sandstone; (b)-basalt intruded by gabbro vein; (c)-sandstone band in siliceous rock; (d)-fault between the Benbatu Fm.and ophiolite

4.4　晚二叠世主动裂谷带

近年来陆续发现兴蒙造山带内存在246～260Ma的基性岩层序，例如Miaoetal.(2007)报道了造山带西段温都尔庙附近约260Ma的枕状玄武岩和林西地区半拉山256±3Ma的辉长岩；初航等(2013)从温都尔庙以北乌兰沟枕状玄武岩中获得246～261Ma的锆石年龄。从已发表的数据看，基性火山岩的地球化学特征接近E-MORB，并且有向OIB演化的趋势(张晋瑞等，2014)；同时这类基性岩具有较多的继承性锆石，其时代从400Ma到元古代，表明锆石可能源于陆壳基底或早古生代造山带的混染(初航等,2013)。王子进等(2013)报道了造山带东段263～246Ma的镁铁质侵入岩，指出其原始岩浆在岩浆源区或岩浆演化过程中遭受了古老陆壳物质的混染，并与同时代的花岗岩组成双峰式火成岩组合，反映伸展环境。综上，在晚二叠世兴蒙造山带已转为陆相为主的背景下，这些以火成岩组合为主的建造可能代表软流圈上涌形成的主动裂谷带。

综上所述，二叠纪时期兴蒙造山带具有伸展作用多次发生、伸展构造复杂多样的特征，这与更大范围的构造背景一致，例如Jahnetal.(2009)在中亚造山带范围内划分了3条巨型岩浆岩带，横跨新疆、蒙古南部、内蒙古和东北地区，由约300～260Ma的花岗岩及双峰式火山岩组成，用以描述早-中二叠世广泛的伸展作用。

5　讨论

5.1　放射虫代表的沉积环境

该区一个值得澄清的问题是放射虫所代表的古地理环境。有学者把兴蒙造山带内放射虫的出现作为二叠纪古亚洲洋存在的关键性证据(王玉净和樊志勇，1997；尚庆华，2004；王惠等，2005)，例如用毛登牧场和哲斯敖包地区的放射虫化石推测内蒙古中、东部中二叠世仍存在古亚洲洋。这种认识得到广泛引用。但最近方俊钦等(2014)在毛登牧场地区原放射虫化石赋存层位找到宏体螺类化石，而且《内蒙古自治区地质志》(第195页)早已报道过毛登牧场下二叠统有Paracalamitessp.,Noeggerathiopsissp.等安哥拉植物群化石(内蒙古自治区地质矿产局，1991)。在哲斯敖包地区，以丰富的腕足、珊瑚和化石为特色的哲斯生物群产于厚层生物碎屑灰岩中，显然代表生物产率极高的滨海环境。因此，兴蒙造山带二叠纪放射虫化石并非代表深海远洋环境，不能作为早-中二叠世古亚洲洋存在的证据。在世界范围内，论述放射虫化石产于滨浅海相的研究实例屡见不鲜(见方俊钦等,2014的文章及其参考文献)。

5.2　古地磁研究成果的启示

在研究古亚洲洋闭合、兴蒙造山带形成过程中，华北板块与古亚洲洋内各微板块的位置关系显得尤为重要，一些学者的研究成果给出了新的启示。Xuetal.(1997)通过对俄罗斯赤塔地区石炭-二叠系地层的古地磁研究，认为在石炭-二叠纪赤塔地区与华北板块具有相似的纬度，而距离西伯利亚板块很远。Pruner (1987)通过对蒙古国中部的古地磁研究，认为蒙古国中部地区在二叠纪已成为华北板块一部分。Chenetal.(1997)通过对东乌旗地区上石炭统地层的古地磁研究，认为晚石炭世乌里雅斯台大陆边缘非常接近华北板块。李朋武等(2012)对苏尼特左旗北部白音乌拉及敖汉旗安庆沟乡晚石炭世地层的古地磁研究显示二者具有相似的古地磁方向，据此认为内蒙古中部在晚石炭世-早二叠世可能已属华北地块。根据Zhaoetal.(2013)对内蒙古中部地区泥盆纪-二叠纪地层的最新研究，该区自晚泥盆世之后已与华北板块处于同一纬度，可能说明二者此时非常接近。以上古地磁研究结果说明：华北板块与古亚洲洋内的几个陆块最晚在晚石炭世已成为统一块体，代表古亚洲洋的闭合。

6　结论

(1)中泥盆世之前兴蒙造山带的构造单元可划分为“五块四带”：从北向南依次为额尔古纳地块、兴安地块、艾力格庙-锡林浩特地块、松辽-浑善达克地块及佳木斯地块；它们之间的4条边界为：新林-喜桂图缝合带、艾力格庙-锡林浩特-黑河缝合带、温都尔庙-吉中-延吉缝合带和牡丹江缝合带。

(2)中-晚泥盆世内蒙古及东北地区完成了由古亚洲洋到兴蒙造山带的构造格局转变，开始出现多处陆相及海陆交互相沉积。石炭纪则广泛分布陆相及滨浅海相碎屑岩和碳酸盐建造，同时发育蛇绿岩、辉长岩、花岗岩及双峰式火山岩等建造，可划分陆相盆地、陆表海盆地、蛇绿岩带、侵入岩带等构造单元。

(3)二叠纪时期兴蒙造山带具有伸展作用多次发生、伸展构造复杂多样的特征，形成了多种岩石-构造单元，包括被动裂谷带、主动裂谷带、索伦山Ligurian型蛇绿岩带和碱性岩带等。早-中二叠世沉积类型多变，普遍含植物化石和滨浅海相动物化石，有大量双峰式火山岩，这类沉积建造与火山岩建造均发育的组合应属被动裂谷，而晚二叠世发育的以火成岩组合为主的建造可称为主动裂谷。

7　结语

目前关于兴蒙造山带的研究存在多个尚待解决的重要问题，例如东部地区有几个地块？它们之间的构造关系如何？兴蒙造山带东、西部如何对比与衔接？晚古生代岩浆活动的构造背景及其意义？古亚洲洋最终闭合的位置、时代及过程？蒙古-鄂霍茨克洋和古太平洋俯冲过程对古亚洲洋构造域的影响等。显然，解决这些问题需要进行长期的、大量的工作。兴蒙造山带构造单元的划分争议颇多，虽然本文按照古亚洲洋早古生代闭合、晚古生代伸展的观点初步建立了兴蒙造山带早、晚古生代的构造单元，但限于篇幅，未能对不同观点展开讨论，对已有研究资料的阅读和引用也难免挂一漏万。另外，虽然本文提出了晚古生代伸展构造的类型和实例，但据目前的研究程度还不能在兴蒙造山带范围内进行完整划分，也没有讨论伸展作用之后的挤压过程。

致谢在成文过程中，与任纪舜、何国琦、邵济安、韩宝福、魏春景、宋述光、邵积东、许文良、刘永江、周建波、葛文春、孙立新等同行进行了有益的讨论，特此致谢！

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