岩石学报  2014, Vol. 30 Issue (7): 2041-2054   PDF    
引用本文
李可, 张志诚, 冯志硕, 李建锋, 汤文豪, 罗志文. 2014. 内蒙古中部巴彦乌拉地区晚石炭世-早二叠世火山岩锆石SHRIMP U-Pb定年及其地质意义. 岩石学报,30(7): 2041-2054  
Li K, Zhang ZC, Feng ZS, Li JF, Tang WH, Luo ZW. 2014. Zircon SHRIMP U-Pb dating and its geological significance of the Late-Carboniferous to Early-Permian volcanic rocks in Bayanwula area, the central of Inner Mongolia. Acta Petrologica Sinica,30(7): 2041-2054 (in Chinese with English abstract)  
内蒙古中部巴彦乌拉地区晚石炭世-早二叠世火山岩锆石SHRIMP U-Pb定年及其地质意义
李可, 张志诚, 冯志硕, 李建锋, 汤文豪, 罗志文    
北京大学造山带和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 100871
2013-9-10 收稿, 2013-12-13 改回.
基金项目：本文受国家重点基础研究发展计划项目（2013CB429801）和中国地质调查局项目（1212010050503）联合资助.
第一作者简介：李可，女，1988年生，博士生，构造地质学专业，E-mail：michealliker@126.com
摘要：内蒙古巴彦乌拉地区广泛出露宝力格组火山-沉积地层。其中流纹岩样品的锆石SHRIMP U-Pb年龄分别为307.1±6.3Ma和308.9±1.8Ma，结合前人研究结果，宝力格组火山岩确切喷发时间应为晚石炭世到早二叠世。样品位于碱性-钙碱性系列岩石过渡区域，在TAS图中，中基性火山岩落入玄武质粗安岩、粗安岩和安山岩区，REE分馏明显，LILE富集，HFSE明显亏损，Nb、Ta、Ti、P负异常，Zr、Hf正异常，形成于岩石圈地幔部分熔融作用；流纹岩LILE（Rb、Th、U）富集，HFSE（Nb、Ta、Ti）明显亏损，具有高正εNd（t）和年轻tDM1值，是新增生的陆壳部分熔融的结果，并具有I型和A型两类花岗岩的地球化学属性。综合区域地质特征和前人研究资料表明，宝力格组火山岩形成于后造山构造环境。
关键词： 晚古生代火山岩     锆石SHRIMP U-Pb定年     后造山环境     古亚洲洋    
Zircon SHRIMP U-Pb dating and its geological significance of the Late-Carboniferous to Early-Permian volcanic rocks in Bayanwula area, the central of Inner Mongolia
LI Ke, ZHANG ZhiCheng, FENG ZhiShuo, LI JianFeng, TANG WenHao, LUO ZhiWen    
MOE Key Laboratory of Orogenic Belts and Crustal Evolution, School of Earth and Space Sciences, Peking University, Beijing 100871, China
Abstract: The Inner Mongolia-Da Hinggan Orogenic Belt (IMDOB), located in the east of Central Asian Orogenic Belt (CAOB), records the boundary between the North China Craton and the Siberian Craton, and is the key area to reconstruct the tectonic history of the CAOB. However many essential issues still remain uncertain at present, such as the evolution of the tectonic environment, especially during Paleozoic period, and the final closure time of the Paleo-Asian Ocean. The Bayanwula area, situated in the northwest of Sonid Zuoqi, the west of the IMDOB, is characterized by the volcano-sedimentary strata of the Baolige Formation. The strata formed in the Late Paleozoic period is represented by typical intermediate-basic, felsic volcanic rocks and pyroclastic rocks. Some people consider these volcanic rocks display a bimodal geochemical distribution. They constitute one part of the Late Paleozoic magma in the IMDOB. So knowing the characteristics of the volcanic rocks is very important and helpful for understanding the tectonic setting and the evolution of the Paleo-Asian Ocean in Paleozoic. Therefore the geochronological and geochemical study has been done in order to solve these problems. By means of SHRIMP zircon U-Pb dating, the ages of two rhyolite samples are 307.1±6.3Ma and 308.9±1.8Ma, which are consistent with the ages of the Baolige Formation in the eastern area and about 20Myr earlier than the intrusive alkaline granite around Bayanwula village in the south. Combined with previous research results, it is suggested that the Baolige Formation was not erupted during Early Permian, but between Late Carboniferous and Early Permian. By the geochemical analysis, the intermediate to mafic rocks fall into basaltic trachyandesite, trachyandesite and andesite field and locate in the transition area between alkaline and subalkaline rock series in the TAS diagram. In the chondrite-normalized REE and primary mantle-normalized trace element fractional diagrams, they all exhibit enrichment in LILE and LREE, depletion in HREE and HFSE, obviously negative in Nb, Ta, Ti, P, and positive in Zr, Hf. The ratios of La/Nb (3.08~5.18) and Nb/U (1.58~6.15) are closer to the values in the crust components than in the mantle components. In the La/Nb vs. La/Ba diagram, the distribution trend of samples is near to the continental lithospheric mantle transformed by the subduction. These characters suggest the intermediate to mafic rocks may be originated from partial melting of the lithosphere materials. Otherwise, the felsic rocks fall into rhyolite area in the TAS diagram with the geochemical characteristics of I-and A-type granite in the granite classification figures. Moreover these rhyolites are enrichment in LREE and LILE (Rb, Th, U), depletion in HREE and HFSE (Nb, Ta, Ti), and have strongly depletion in Ti, Sr, Ba. The isotope geochemical characteristics of them are similar to those of the Late Paleozoic granites widely distributed in the Da Hinggan and Northeast China areas with positive εNd(t) (0.5124~0.5125) and young tDM1 ages (769~595Ma), which document the juvenile continental crustal formation. With the changes of SiO2 content, there are some different variational characteristics in the constant and trace elements between mafic and felsic rocks that imply their different source regions. Possibly the felsic volcanic rocks derived from the partial melting of newly accreted crustal components induced by the intermediate-basic magma underplating. These volcanic rocks constitute a calc-alkaline to alkaline magmatic suite. In the diagrams of tectonic environment discrimination, the intermediate to mafic rocks are located in the within-plate basalts areas and the felsic rocks mostly fall into the post-collision or post-orogenic areas, implying that they belong to the post-orogenic magmatic rocks. In the adjacent areas, some magma related to the subduction process are formed in 490~422.8Ma. The metamorphic age of Xilin Gol complex (337Ma) forming at the peak stage of orogeny is about 30Myr earlier than the volcanic rocks of the Baolige Formation. Zircons from a microgabbro and a plagiogranite in Hegenshan ophiolite yielded ages of 354Ma and 333Ma, and the ages of Erenhot ophiolite was obtained in 354.2~344.8Ma. Meanwhile some cotemporaneous magma (330~313Ma) standing for post-orogenic environment were reported around Xiwuqi and Xilinhot regions, and a wide range of alkaline granites emplaced during 295~270Ma in the CAOB which indicate a geodynamic regime of regional extension. In addition, the widespread extensional setting can be further confirmed by the emplacement of bimodal volcanic rocks of Early Permian in the adjacent regions. Taken together, the Paleo-Asian Ocean closed before the Late Carboniferous epoch, and the volcanic rocks of the Baolige Formation developed in a post-orogenic extensional regime.
Key words: Late Paleozoic volcanic rocks     Zircon SHRIMP U-Pb dating     Post-orogenic setting     Paleo-Asian Ocean    
1 引言

兴蒙造山带位于西伯利亚板块与中朝板块之间，是全球显生宙时期增生最为强烈的地区之一(Sengör and Natal’in，1996; Kovalenko et al., 2004; Windley et al., 2007)。自早古生代以来该地区经历多期次大洋板片俯冲、地壳增生、多块体聚合过程，最终完成了华北板块与西伯利亚板块的碰撞(Jahn et al., 2004; 郭锋等，2009)。古亚洲洋复杂的演化过程，一直是地学界关注的焦点(Tang，1990; 邵济安，1991; 唐克东，1992; Xu and Chen， 1997; Xiao et al., 2003; Chen et al., 2012; 晨辰等，2012; Xu et al., 2013; Ma et al., 2013; Shi et al., 2013; Zhang et al., 2013，2014)。但目前，洋盆最终关闭时限问题仍存在不同观点(邵济安，1991; 唐克东，1992; 包志伟等，1994; Sengör and Natal’in，1996; Chen et al., 2000; 张臣和吴泰然，2001; Shi et al., 2004; Miao et al., 2008; Xiao et al., 2009)。

兴蒙造山带北缘大范围发育晚古生代火山岩浆活动，是研究造山带构造演化、古亚洲洋闭合过程的重要地区之一。近年来，随着研究的不断深入，对该区域晚古生代岩浆活动的研究取得了一定的成果，但其形成的构造背景仍存在两种主要的认识：(1)古亚洲洋闭合造山后伸展或者类似于弧后盆地背景(Zhang et al., 2008，2011; 汤文豪等，2011; Chen et al., 2012)；(2)安第斯型活动大陆边缘岛弧成因环境(Xiao et al., 2003，2009; 陶继雄等，2003; 卿敏等，2012)。这些不同的观点，主要受到缺乏精确定年代学资料建立晚古生代火山岩的时空格架影响。

为了更好地解决内蒙古中部地区晚古生代的构造演化问题及其与古亚洲洋闭合的关系，本文对苏尼特左旗北部巴彦乌拉地区晚古生代火山岩进行精确锆石SHRIMP U-Pb年龄测定，并结合地球化学特征，系统研究该地区晚古生代火山岩成因及大地构造环境，为华北板块与西伯利亚板块拼合的时间以及碰撞演化历史提供新的依据。

2 地质背景

巴彦乌拉地区位于苏尼特左旗北，紧邻索伦缝合带北部北造山带(早中古生代造山带)(图 1a)，该地区长期以来是研究古亚洲洋演化的关键区域。研究区主要出露晚泥盆世，晚石炭世-早二叠世、晚侏罗世、早白垩世和新生代地层(图 1b)。其中，最发育的为晚古生代宝力格组火山-沉积地层。根据岩性组合特征的不同，宝力格组地层被划分为三个岩段：第一岩段由硬砂岩、含粉砂质板岩和砾岩组成，零星分布在研究区东北和西北部；第二岩段地层主要由灰绿色安山岩、玄武粗安岩、流纹岩等组成，中间夹有含角砾流纹质熔结凝灰岩、晶屑凝灰岩等火山碎屑岩层，火山岩主体为酸性岩浆，区域上具有下部以中基性火山岩浆为主，上部以酸性岩浆为主的特征，广泛分布于研究区巴彦乌拉苏木至阿尔善宝拉格，西部萨音温多尔音敖包及东北部锡林哈敖包一带，厚度大于3323m(内蒙古自治区地质矿产局，1991)；第三段为灰绿色英安岩、玄武安山岩组成，局部夹凝灰岩、粉砂岩及灰岩透镜体，主要出露在研究区北部花敖包特一带。此外，宝力格组地层被晚古生代和中生代花岗岩岩体侵入。在巴彦乌拉苏木地区，早二叠世碱性花岗岩体侵入到宝力格组地层中，部分与宝力格组呈断层接触，构成北东向构造岩浆带。另外，研究区还有石英斑岩、花岗斑岩和正长斑岩脉产出。

图 1 内蒙古巴彦乌拉地区地质图

(a)-大地构造缩略图(据Jian et al., 2010)；(b)-巴彦乌拉地区地质简图(据内蒙古自治区地质局，1980①)；(c)-研究区地质剖面图

Fig. 1 Geological sketch map of the Bayanwula area in Inner Mongolia

(a)-tectonic geological setting(after Jian et al., 2010);(b)-simplified geological map of the Bayanwula area in Inner Mongolia;(c)-cross-section of the study area

①内蒙古自治区地质局. 1980. 白音乌拉幅1︰20万地质图与区域地质调查报告

本次研究沿着巴彦乌拉公路采集了37件宝力格组火山岩样品(图 1c)，采样点GPS见表 1。其中以第二岩段样品为主，并采有少量第三段岩样进行对比。薄片研究表明，玄武质粗安岩中，碱性长石斜长石颗粒自形完好，杂乱分布的长石格架中充填有它形辉石和磁铁矿物。安山岩样品长条状斜长石微晶呈定向或半定向排列，其间分布少量辉石和磁铁矿，具有交织结构特征。流纹岩样品斑状结构，斑晶以长石石英为主，基质主要是微晶质的长石石英，流纹构造明显，部分样品中可见晶形完好的石榴石斑晶。

表 1 采样点GPS坐标位置 Table 1 The GPS data of all the samples
3 SHRIMP锆石U-Pb定年 3.1 分析方法

对宝力格组二段NM08-140和三段NM10-25流纹岩样品进行SHRIMP U-Pb定年。样品的分选工作在廊坊诚信地质技术服务公司完成：将原岩样品破碎至100μm左右，先用磁法和重液分选，在双目镜下手工挑纯；然后将锆石与数粒标准锆石TEMORA置于环氧树脂中，研磨至1/2，暴露新鲜面后制靶，进行抛光、超声波处理和镀金；测试前在北京大学造山带地壳演化重点实验室和环境扫描电子显微镜实验室完成反射光和阴极发光(CL)照片；最后再在中国地质科学院北京离子探针中心完成SHRIMP锆石U-Pb定年测定。测试过程中，使用标样SL13(572Ma)标定所测样品的锆石U、Th、Pb含量，再用标样TEMORA(417Ma)进行元素间的分馏校正，样品分析流程见Compston et al.(1992)，使用ISOPLOT和Squid程序(Ludwig，2003)进行实验数据处理以及谐和图绘制，置信度为95%。

3.2 锆石特征及定年结果

样品NM08-140中挑选出来的锆石颗粒具有完好的晶形结构(图 2a)，锆石的长宽比在11~31，内部普遍发育环带结构。13颗锆石的离子探针测试结果见表 2，U、Th含量变化范围分别为118×10-6~514×10-6和70×10-6~602×10-6，锆石Th/U比值在0.46~1.21之间，基本都大于0.5，属岩浆成因锆石(Hanchar and Miller， 1993; Claesson et al., 2000; Belousova et al., 2002)。样品的13颗锆石定年数据点几乎都落在谐和线及其附近(图 2b)，锆石颗粒的年龄测定值均很稳定，集中分布在307Ma附近，其加权平均年龄为307.1±6.3Ma(MSWD=0.63)，代表火山岩的喷发年龄。

图 2 流纹岩(NM08-140)锆石阴极发光照片及SHRIMP测点位置(a)和锆石U-Pb年龄谐和图(b) Fig. 2 CL images and dating spots(a) and SHRIMP U-Pb concordia diagrams(b)for zircons of rhyolite(sample NM08-140)from the Baolige Formation

表 2 宝力格组流纹岩锆石SHRIMP U-Pb分析结果 Table 2 SHRIMP U-Pb data of zircons from rhyolites in the Baolige Formation

样品NM10-25中挑选出来的锆石颗粒具有长柱状或短柱状特征(图 3a)，长宽比在1.51~31，晶面整洁光滑。在阴极发光照片上，未见有明显核部特征，大多数锆石都具有清晰的结晶环带，表明是岩浆结晶过程形成的。U、Th含量变化范围分别为58×10-6~438×10-6和48×10-6~491×10-6，锆石Th/U比值在0.61~1.31之间，属岩浆成因锆石。13颗锆石分析点给出了狭窄的年龄范围，在一致曲线上，这些数据点集中分布(图 3b)，加权平均年龄为308.4±5.4Ma(MSWD=0.89)，同时13个点还给出非常好的谐和年龄308.9±1.8Ma，解释为火山岩的喷发年龄。

图 3 流纹岩(NM10-25)锆石阴极发光照片及SHRIMP测点位置(a)和锆石U-Pb年龄谐和图(b)

Fig. 3 CL images and dating spots(a) and SHRIMP U-Pb concordia diagrams(b)for zircons of rhyolite(sample NM10-25)from the Baolige Formation

4 岩石地球化学特征

样品主量元素的测定在北京大学造山带与地壳演化教育部重点实验室利用X光荧光光谱(XRF)分析完成，精度达1%。微量稀土元素测定在核工业北京地质研究院利用电感耦合等离子质谱仪(ICP-MS)测定完成，除Nb、Ta测试精度稍低在9%外，其余都在5%以内。同位素测定在核工业北京地质研究院分析测试中心利用ISOPROBE-T热电离质谱仪完成测定。 4.1 主量元素

本区岩石样品的SiO2含量变化范围较大，从50.38%~78.15%(表 3)。其中，绝大多数样品的SiO2含量在69.07%~78.15%之间，属典型的酸性岩，在TAS图解中(图 4a)投影在流纹岩区；其他岩石样品SiO2含量50.38%~64.34%，属中基性火山岩，在TAS图解中，1件样品落入粗安岩区、3件样品落入安山岩及其向英安岩过渡区，其余样品落入玄武质粗安岩区。所有样品均落于碱性和亚碱性系列过渡区域，在K2O-SiO2图解(图 4b)中，岩石样品具有钙碱性及高钾钙碱性岩石系列特征。

表 3 宝力格组火山岩地球化学分析结果(主量元素: wt%；微量和稀土元素: ×10-6 ) Table 3 The geochemical composition of volcanic rocks in the Baolige Formation(major element: wt%; trace element: ×10-6)

图 4 宝力格组火山岩TAS图解(a)和SiO2K2O图解(b)（据Le Maitre, 1989; Peccerillo and Taylor, 1976）

Fig. 4 TAS (a) and SiO2 vs K2O (b) diagrams of volcanic rocks in the Baolige Formation (after Le Maitre, 1989; Peccerillo and Taylor, 1976)

中基性岩石样品中TiO2含量低，变化在0.57%~1.54%；Al2O3含量变化在15.43%~19.25%，MgO为2.57%~5.93%，CaO为2.84%~5.41%，Na2O+K2O为5.08%~8.26%，P2O5为0.20%~0.73%；Mg#介于42.8~58.4之间。酸性岩石样品中TiO2含量低，变化在0.15%~0.63%之间；Al2O3为11.16%~15.62%，MgO为0.01%~0.94%，CaO为0.17%~2.35%，Na2O+K2O为6.65%~10.38%，P2O5为0.01%~0.21%。 4.2 稀土元素

稀土元素组成测试结果见表 3。中基性岩石样品∑REE介于92.20×10-6~169.3×10-6之间，(La/Yb)N在3.50~7.65之间；样品稀土元素配分模式都呈现LREE富集，HREE亏损的右倾型。δEu变化范围0.87~1.20，未出现明显的铕异常现象(图 5)。

图 5 宝力格组中基性火山岩球粒陨石标准化REE图解和微量元素蛛网图（标准化值据Sun and McDonough, 1989）

Fig. 5 Chondritenormalized REE and primary mantlenormalized trace element spider diagrams for intermediate to mafic rocks from the Baolige Formation (normalization values after Sun and McDonough, 1989)

酸性流纹岩样品∑REE介于89.49×10-6~271.4×10-6之间，稀土含量较高，(La/Yb)N在1.23~9.07之间；多数样品的稀土元素配分模式具有LREE富集，HREE相对亏损的右倾型特征，个别样品轻重稀土分馏不明显(图 6)。δEu变化范围0.44~0.87，有较弱的铕负异常现象。

图 6 宝力格组酸性火山岩球粒陨石标准化REE图解和微量元素蛛网图(标准化值据Sun and McDonough， 1989)

Fig. 6 Chondrite-normalized REE and primary mantle-normalized trace element spider diagrams for acid rocks from the Baolige Formation(normalization values after Sun and McDonough， 1989)

4.3 微量元素

原始地幔标准化蛛网图中，大多中基性岩石样品微量元素含量变化趋势基本一致(图 5)，普遍都富集LILE(Rb、Ba、Th、Sr、U)，明显亏损HFSE(Nb、Ta、Ti)，Zr、Hf相对富集。酸性流纹岩样品除Ba，Sr变化较大外，其他微量元素一致表现为LILE(Rb、Th、U)高度富集，HFSE(Nb、Ta、Ti)明显亏损，Zr、Hf富集的特征(图 6)。 4.4 Sr、Nd同位素特征

对4件流纹岩样品进行同位素测定，测定结果见表 4。样品的87Rb/86Sr值相差较大，变化在1.1642~3.4376，147Sm/144Nd为0.1086~0.1215，计算得(87Sr/86Sr)i为0.702556~0.707645，(143Nd/144Nd)i为0.512421~0.512528，εNd(t)为3.46~5.54，tDM1为595~769Ma。

表 4 宝力格组流纹岩样品Sr-Nd同位素组成 Table 4 Sr-Nd isotopic compositions of the rhyolite samples from the Baolige Formation
5 讨论 5.1 时代框架

长期以来，宝力格组地层的时代划分存在较大的争议。1961年内蒙古地质局对其定名以及在1980年巴彦乌拉地区120万区域地质图中(内蒙古自治区地质局，1980)，都将宝力格组划分到早二叠世；而1963年谢同伦根据腕足类化石碎片，将其归属于晚石炭世(转李文国，1981)；1981年李文国从岩相学和生物群面貌特征入手，将该套地层划分为中石炭世(李文国，1981)。最近，Zhang et al.(2011)等对该地层中玄武安山岩及流纹岩样品锆石U-Pb定年结果为289Ma和287Ma，属早二叠世，并认为该套火山岩具有双峰式地球化学特征。

本次研究重新对宝力格组第二三岩段火山岩中流纹岩样品进行了锆石SHRIMP U-Pb定年，采样尽可能避开后期花岗岩侵入体。样品的锆石颗粒结晶较好，均具有岩浆锆石的特点，实验最终获得了精确的锆石U-Pb年龄307.1±6.3Ma和308.9±1.8Ma，两岩段样品的锆石年龄在误差范围内非常一致。由于研究区野外露头差，很难建立火山岩序列的喷出期次，但火山岩的地球化学特征与Zhang et al.(2011)测得的结果十分相似，因此推测两次研究选择的火山岩应属同一期火山活动的产物。尽管本次未对中基性火山岩定年，但现已获得的研究区东部阿尔善宝拉格地区宝力格组安山岩样品锆石LA-ICP-MS年龄为310Ma(未发表)，与本次所获流纹岩样品年龄吻合。巴彦乌拉苏木附近侵入于宝力格组中的碱性花岗岩锆石U-Pb年龄为289±2Ma(韩宝福，未发表数据)，也表明该组形成时代应早于早二叠世。由此判定，本区宝力格组火山岩形成于308Ma，结合前人结果，宝力格组地层形成时代应介于晚石炭世到早二叠世间。 5.2 岩浆源区特征

薄片研究显示，大部分岩石样品新鲜，蚀变程度较低(LOI<3%)，集中在0.5%~2.5%，仅有2个样品达4%，火山岩地球化学元素信息可以用来表征原始岩浆特征。

中基性火山岩源区一般为软流圈或岩石圈地幔(Zhang et al., 2005)。研究区中基性岩LREE富集，HREE亏损，La/Yb=3.50~7.65，轻重稀土元素分异明显，Mg#为42.8~58.4。参考前人研究结果，该组中基性火山岩同位素具有亏损地幔性质(Zhang et al., 2011)。微量元素分析结果显示，样品相应富集LILE，亏损HFSE，Nb、Ta、Ti、P等元素负异常，Zr、Hf正异常，不符合软流圈地幔地球化学特征；另外La/Nb值3.08~5.18，更接近于陆壳La/Nb值(2.2)而非原始地幔(0.98~1)(Dungan et al., 1986)；Nb/U值通常在MORB(47±11)和OIB(52±15)中比较稳定(郭锋等，2001)，而所测样品的Nb/U值为1.58~6.15远小于原始地幔组分中比值；在La/Nb-La/Ba图解中(图略)，样品的分布偏向于受俯冲改造的大陆岩石圈地幔，在La/Sm-La图解中(图略)，所有中基性岩样品更趋向于部分熔融的演变趋势。综合以上考虑，宝力格组中基性火山岩可能形成于岩石圈地幔部分熔融作用。

研究区酸性火山岩LREE和LILE(Rb、Th、U)富集，HREE和HFSE(Nb、Ta、Ti)亏损，相对于中基性火山岩具有明显Eu负异常，及Ti、Sr和部分Ba元素强烈亏损的特征。在SiO2对Al2O3、CaO、TiO2及Sr图上(图略)，酸性火山岩呈一致的线性分布，中基性火山岩分布零散；而在SiO2对MnO及Rb图中(图略)特征正好相反，反应两者可能具有不同的源区性质。流纹岩样品具有正εNd(t)值和低tDM1值，表现出增生陆壳的性质，和大兴安岭及我国东北部晚古生代花岗岩同位素特征相似(Wu et al., 2002，2003; Jahn et al., 2009; Meng et al., 2011)。另外，大部分岩石样品A/CNK<1.1，A/NK>1.0，在花岗岩分类图(图 7)中，样品数据点集中在过渡区域及附近，同时还具有I型花岗岩趋势演化特征而非S型(图 8)，可见酸性火山岩兼有A和I型两类花岗岩的地球化学属性。宝力格组酸性火山岩的SiO2含量较高，不太可能直接由分离结晶作用形成(张旗等，2008)，在La/Sm-La图(图略)中，更多的样品趋向于部分熔融的演变趋势分布。因此酸性火山岩可能为中基性岩浆底侵导致增生陆壳部分熔融作用的结果，与中亚造山带内古生代花岗质岩浆的成因特征类似(Wu et al., 2002，2003; Jahn et al., 2004，2009; Meng et al., 2011)。

图 7 花岗岩类判别图(据Whalen et al., 1987)

Fig. 7 Classification diagrams of granitoid(after Whalen et al., 1987)

5.3 地质意义

近年来，通过对兴蒙造山带北缘火山岩浆活动研究发现，该地区晚古生代主要存在两类岩浆，早期以钙碱性-高钾钙碱性系列为主，晚期以碱性系列岩浆为主，并在北造山带及其以北地区形成早期I型花岗质岩浆为主的岩浆岩带和晚期A型碱性花岗质岩浆带(洪大卫等，1994; Jahn et al., 2009)。但目前，对这些晚古生代岩浆构造背景的解释仍不统一，Chen et al.(2009)认为苏左旗地区存在310Ma左右的弧岩浆事件；Liu et al.(2013)报道了西乌旗地区与俯冲相关的岩浆年龄为314Ma和318Ma；然则另一些学者认为该期间已经进入造山后演化阶段(洪大卫等，1994; 鲍庆中等，2007; 周文孝，2012)。

图 8 宝力格组流纹岩SiO2对P2O5及Pb图解(据Chappell and White， 1992)

Fig. 8 SiO2 vs. P2O5 and Pb variation diagrams of acid volcanic rocks from the Baolige Formation(after Chappell and White， 1992)

本次研究选取的宝力格组酸性火山岩样品兼有I-A型两类花岗岩的地球化学属性，与同时产出的中基性火山岩样品一样，有碱性、钙碱性和高钾钙碱性系列特征。Liegeois et al.(1998)指出高钾钙碱性岩浆出现，并向安粗质岩浆过渡是造山演化到最后阶段的标志；多数造山带后碰撞花岗岩以中-高钾钙碱性I型花岗岩为主(韩宝福，2007)，而A型及其相关碱性花岗岩的出现预示着进入后造山伸展阶段，因此在造山带演化后期，常伴有I-A型花岗岩产出(Wu et al., 2003)。邻区蒙古南部、内蒙古西部等地也广泛发育晚石炭世I-A型花岗岩(韩宝福等，2010)，均指向后碰撞环境。在构造判别图中，中基性火山岩样品落入板内玄武岩区域(图 9a)，酸性火山岩落入后碰撞花岗岩区域(图 9b-d)。由此推测，308Ma古亚洲洋已经闭合并处于造山后演化阶段。

图 9 宝力格组火山岩构造环境判别图(据Pearce，1984; Batchelor and Bowden， 1985; Maniar and Piccoli， 1989)

Fig. 9 Tectonic discriminant diagrams of the volcanic rocks in Baolige Formation(boundaries of rock type after Pearce，1984; Batchelor and Bowden， 1985; Maniar and Piccoli， 1989)

区内更多的、与俯冲作用有关属于前碰撞的岩浆侵位时代多数介于490~422.8Ma(石玉若等， 2004，2005; Jian et al., 2008)；与挤压相关的蚀变花岗岩年龄为418~326Ma(张臣和吴泰然，2001)；近来，Jian et al.(2012)获得贺根山蛇绿岩中辉长岩和花岗岩可靠年龄值分别为354Ma和333Ma；Zhang et al.(2014)获得二连浩特地区蛇绿岩年龄为354.2~344.8Ma，与贺根山蛇绿岩形成时代基本一致；锡林郭勒杂岩中与碰撞造山相关的重要变质事件为337Ma(薛怀民等，2009)，这些年龄证据说明晚石炭世时期本区可能已经处于后碰撞环境。同时，区域上还存在与晚石炭世火山岩同时期的大量岩浆活动，包括西乌旗地区323~313Ma的石英闪长岩(鲍庆中等，2007)及锡林浩特地区330~317Ma的花岗质岩浆(周文孝，2012)，都被认为形成于后造山阶段。而后期巴彦乌拉-东乌珠穆沁旗带及整个中亚造山带内大范围的碱性花岗岩侵位时间在295~270Ma(洪大卫等，1994; Shi et al., 2004; Jahn et al., 2009)；锡林浩特地区双峰式火山岩年龄为279Ma和281Ma(Zhang et al., 2008)。综上考虑，古亚洲洋在晚石炭世之前发生闭合，晚石炭世-早二叠世时期已经进入后造山阶段，并逐步向广泛的伸展构造环境转化。

6 结论

综上所述，巴彦乌拉地区宝力格组火山岩的成因可能为后碰撞背景下岩石圈地幔部分熔融，并在上涌底侵过程中，造成增生陆壳物质熔融作用的结果。SHRIMP U-Pb定年结果为307.1±6.3Ma和308.9±1.8Ma，表明晚石炭世时期，研究区已进入后造山演化阶段，并逐步向早二叠世广泛伸展环境转化。

致谢 两位审稿人和编辑详细审阅了全文，并提出了宝贵的修改意见和建议，在此表示衷心的感谢。

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