2019, Vol. 35
2. 中国地质科学院地质研究所, 北京 100037;
3. 中国地质调查局天津地质调查中心, 天津 300170
2. Institute of Geology, Chinese Academy of Geological Sciences, Beijing 100037, China;
3. Tianjin Institute of Geology and Mineral Resources, China Geological Survey, Tianjin 300170, China
华北克拉通作为中国三大古老克拉通之一，经历了漫长的、复杂的、多阶段构造演化过程，是研究地球早期形成和演化历史的重要场所。Zhao et al. (1998)在华北克拉通中部识别出一条重要的碰撞造山带，称之为“华北中部造山带”(the Trans-North China Orogen, 图 1)。该造山带以两条深大断裂为界、总体呈南北向展布，形成于古元古代末期，其内部杂岩普遍记录了顺时针型、含近等温降压片段的变质作用P-T轨迹，所记录的主要区域变质作用与碰撞造山带有关。Zhao et al. (1998)据此以华北中部造山带为界，将华北克拉通前寒武纪基底划分为东部陆块(the Eastern Block)和西部陆块(the Western Block)两部分。在1.85Ga左右，西部陆块发生东向俯冲，继而与东部陆块沿华北中部造山带发生碰撞拼合，导致华北克拉通早前寒武纪统一基底的最终形成。东、西部陆块与华北中部造山带的变质演化特征存在明显差异，大部分变质杂岩拥有逆时针型、含近等压降温片段的P-T轨迹，其形成与25亿年左右大规模地幔岩浆底侵作用有关(Zhao et al., 1998, 2001b, 2005)。
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图 1 华北克拉通前寒武纪地质简图(a, 据Zhao et al., 2005)、左权变质杂岩构造位置图；(b, 据Zhao et al., 2001b)和地质简图(c, 据杨崇辉等，2011和河北省地质局，1968①及山西省地质局，1972②等资料编制)及采样点 1-古生代地层；2-中元古代地层；3-新太古代TTG片麻岩；4-采样点；HS-恒山杂岩；WT-五台杂岩；FP-阜平杂岩；LL-吕梁杂岩；ZH-赞皇杂岩；ZQ-左权杂岩 Fig. 1 Geological sketch map of the North China Craton (a, after Zhao et al., 2005), showing location of the Zuoquan metamorphic complex in the Trans-North China Orogen (b, after Zhao et al., 2001b), and the geological sketch map of the Zuoquan metamorphic complex, with sample locations (c, after Yang et al., 2011) 1-Paleozoic strata; 2-Mesoproterozoic Changcheng Group; 3-Neoarchean TTG gneiss; 4-sample locations; HS-Hengshan metamorphic complex; WT-Wutai metamorphic complex; FP-Fuping metamorphic complex; LL-Lüliang metamorphic complex; ZH-Zanhuang metamorphic complex; ZQ-Zuoquan metamorphic complex |
① 河北省地质局. 1968. 1：200000高邑幅、邢台幅地质图
② 山西省地质局. 1972. 1：200000左权幅、长治幅地质图和地质图说明书
华北中部造山带内分布的早前寒武纪变质杂岩区，由北向南主要包括：冀北、承德、宣化、怀安、恒山、五台、阜平、吕梁、赞皇、左权、中条、太华和登封等。按变质作用程度不同，华北中部造山带早前寒武纪基底可以进一步分为高级区和花岗-绿岩带。前者变质程度可达高角闪岩相-麻粒岩相，包括太华、阜平、恒山、怀安、宣化、承德等变质杂岩区，花岗-绿岩带的变质程度较低，多为绿片岩相-角闪岩相，包括登封、中条、赞皇、吕梁、五台、冀北等变质杂岩区(Zhao et al., 2003)。前期变质演化研究表明，赞皇杂岩南部经历了高达高角闪岩相至麻粒岩相过渡区的变质作用(肖玲玲等, 2011, 2012; Xiao et al., 2011, 2014)；吕梁变质杂岩局部地区也有典型基性麻粒岩出露(Xiao et al., 2017)。
尽管不同变质杂岩区的变质程度存在差异，但华北中部造山带各变质杂岩中均可识别出至少三个变质作用阶段，拥有类似的变质演化历史，反映与华北克拉通中部发生的俯冲碰撞有关的大地构造环境。然而，华北克拉通早前寒武纪基底的主期拼合时代仍存在较大争议。大量年代学数据显示，华北中部造山带变质杂岩中至少存在1.85Ga、1.95Ga和2.5Ga左右的三组变质年龄，且其所代表的地质含义尚无定论。其中，约1.85Ga的变质年龄占据了主导地位，反映了近峰期或退变质阶段的变质时代；约1.95Ga的变质年龄代表了峰期前的某个进变质片段或峰期变质时代；2.4~2.5Ga的变质年龄目前仅在阜平、承德和赞皇等少数地区有零星报道(程裕淇等，2004；刘树文等，2007a；Xiao et al., 2014)。这些变质年龄的分布范围及所代表的构造意义对认识华北中部造山带乃至华北克拉通的基底早期演化至关重要，尤其是~2.5Ga变质年龄，它在华北中部造山带的分布是否广泛？所代表的变质事件是什么？与华北中部造山带区域变质事件是否同期？这一问题制约着人们对华北中部造山带构造演化历史完整性的认识。
左权变质杂岩向东紧邻赞皇杂岩(图 1)，二者在构造、岩性和变质演化等方面具有明显亲缘性。本文对左权地区多种岩石类型进行了细致的锆石年代学研究，获得了约1.9Ga和2.5Ga两组变质年龄，且~2.5Ga的变质年龄在该地区有广泛分布，这一信息为全面理解华北中部造山带、乃至整个华北克拉通的构造演化提供重要科学依据。
1 区域地质概况左权变质杂岩位于太行山主脉中段西侧，呈细条状、沿北东-南西向展布，主体出露于山西省晋中市和长治市。构造上属华北克拉通中部造山带中南段(图 1)。杂岩区出露以长英质片麻岩为主的多种前寒武纪变质岩石，局部发育黑云斜长片麻岩、(斜长)角闪片麻岩、(斜长)角闪岩和云母片岩等。片麻岩类均以似层状方式产出，局部暗色矿物富集，拥有协调一致的稳定片麻理。(斜长)角闪岩主要以似层状或断续“透镜状”方式产出于长英质(黑云斜长)片麻岩中，大部分地区二者接触关系截然，局部偶见侵入接触关系。石榴石在不同岩石类型中分布不均匀，且发育不同程度的后成合晶反应结构。其中，含榴黑云斜长片麻岩和含榴斜长角闪岩中至少可识别出早期进变质、峰期和峰期降压等多个阶段的变质矿物组合，记录了顺时针近等温降压型的变质作用P-T轨迹，反映与碰撞造山有关的构造过程(肖玲玲等, 2014)。区内分布多个小型沉积变质铁矿床，铁矿石为富含磁铁矿的黑云斜长片麻岩、黑云母片岩、斜长角闪岩和石英岩等。磁铁矿多呈条带状分布，与(长英质)黑云斜长片麻岩相伴产出。长英质浅色体可分为早、晚两期，早期长英质浅色体作为深熔产物，无规则产出于长英质片麻岩、黑云斜长片麻岩、云母片岩或斜长角闪岩中，总体平行于寄主岩石的片麻理；晚期长英质浅色体呈脉体出现，多穿切片麻理，与围岩接触界线截然。
2 岩相学特征本文样品包括采自晋中市左权县碾草渠村的3件样品(ZZ8-2、ZZ8-3和ZZ8-5)和南冶村的1件样品(ZZ9-5)，以及长治市黎城县西井镇彭庄的2件样品(ZZ12-2和ZZ12-6)。
样品ZZ8-2为深熔长英质浅色体，顺片麻理产出于黑云斜长片麻岩中，主要由斜长石和石英组成，与片麻岩接触处含少量细小黑云母(图 2a)。含榴角闪片麻岩样品ZZ8-3和ZZ12-2的主要组成矿物为石榴石、角闪石和石英，含少量磁铁矿和斜长石(图 2b, e)，角闪石强烈定向。样品ZZ8-3中石榴石发生明显变形，长轴方向与片麻理大致平行。石榴石内部的角闪石包裹体定向明显，且矿物总体迹线与片麻理小角度相交(图 2b)。磁铁矿黑云母石英片岩样品ZZ8-5由磁铁矿、黑云母和石英等组成。黑云母定向排列，多发生绿泥石化(图 2c)。磁铁矿角闪片麻岩样品ZZ9-5的主要组成矿物为磁铁矿、角闪石和石英。角闪石呈细小的他形粒状(图 2d)。含磁铁矿石榴黑云斜长片麻岩样品ZZ12-6由石榴石、黑云母、斜长石和石英等组成，含少量磁铁矿(图 2f)。黑云母定向明显。
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图 2 左权杂岩区岩石样品的显微岩相学照片 (a)深熔长英质浅色体样品ZZ8-2；(b)含榴角闪片麻岩样品ZZ8-3；(c)磁铁矿黑云母石英片岩样品ZZ8-5；(d)磁铁矿角闪片麻岩样品ZZ9-5；(e)含榴角闪片麻岩样品ZZ12-2；(f)含磁铁矿石榴黑云斜长片麻岩样品ZZ12-6 Fig. 2 Photomicrographs of representative samples from the Zuoquan metamorphic complex (a) leucosome, Sample ZZ8-2; (b) garnet-bearing hornblende gneiss, Sample ZZ8-3; (c) magnetite-biotite-quartz schist, Sample ZZ8-5; (d) magnetite-hormblende gneiss, Sample ZZ9-5; (e) garnet-bearing hornblende gneiss, Sample ZZ12-2; (f) magnetite-bearing garnet-biotite-plagioclase gneiss, Sample ZZ12-6 |
肖玲玲等(2013)对采自左权变质杂岩区的25件(斜长)角闪岩样品进行详细的岩石地球化学研究，认为其原岩可分为基性火成岩和泥砂质沉积岩两种类型。根据尼格里参数(al+fm)-(c+alk)-Si原岩恢复图解，包括ZZ8-3和ZZ12-2在内的19件样品落入基性火山岩区；元素比值Zr/TiO2-Nb/Y图解中，所有19件变质基性岩样品均落在亚碱性玄武岩附近区域；由AFM图解可知，多数样品(包括ZZ8-3和ZZ12-2)属拉斑系列(肖玲玲等, 2013)。结合野外特征，杂岩区多数(斜长)角闪岩的产状与围岩片麻岩协调一致，推测其原岩为亚碱性玄武岩；部分岩石产状与片麻岩呈侵入接触关系，其原岩应为基性岩墙或岩脉。前期研究表明，杂岩区多数片麻岩在野外产状和岩石组合上无明显差别，且具有一致、稳定的片麻理，原岩类型大体可分为中酸性火成岩和泥砂质沉积岩两种类型(肖玲玲等, 2013)。
3 LA-ICP-MS锆石U-Pb年代学和微量元素地球化学本文在中国地质大学(北京)完成对样品ZZ8-2、ZZ9-5、ZZ12-2和ZZ12-6的LA-ICP-MS锆石U-Pb年代学和稀土、微量元素分析测试；在中国地质调查局天津地质调查中心完成对样品ZZ8-3和ZZ8-5的LA-ICP-MS锆石U-Pb年代学测试。
中国地质大学(北京)使用多接收电感耦合等离子质谱仪Agilent 7500a ICP-MS和激光器Geolas-193 UV。中国地质调查局天津地质调查中心使用多接收电感耦合等离子质谱仪NEPTUNE和准分子激光器NEW WAVE 193-FX ArF。激光束斑直径为35μm。实验分别采用标准锆石91500(中国地质大学(北京)；1065.4Ma，Wiedenbeck et al., 1995)和GJ-1(天津地质调查中心; 609Ma, Jackson et al., 2004)为外部标准校正U-Th-Pb同位素比值；以国际标样NIST610玻璃作为外标、29Si作为内标计算微量元素含量；依据Steiger and Jäger (1977)方法校正普通Pb；利用ICPMSDataCal(Liu et al., 2010)程序进行数据处理，运用ISOPLOT程序(Ludwig, 2003)进行谐和曲线绘制。同位素比值和单个年龄实测误差为1σ，加权平均年龄误差为95%置信度。同位素测试数据见表 1和表 2(稀土和微量元素测试数据未附，如有需要请联系第一作者)。
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表 1 左权变质杂岩区岩石样品锆石U-Pb同位素分析结果(中国地质大学(北京)测试结果) Table 1 Zircon U-Pb analytical data of the samples from the Zuoquan complex (data were analyzed in the China University of Geosciences (Beijing)) |
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表 2 左权变质杂岩区岩石样品的锆石U-Pb同位素分析结果(中国地质调查局天津地质调查中心测试结果) Table 2 Zircon U-Pb analytical data of the samples from the Zuoquan complex (data were analyzed in the Tianjin Institute of Geology and Mineral Resources, China Geological Survey) |
该样品中锆石无色、透明，颗粒较大，直径约200~500μm，呈柱状或浑圆状，个别颗粒含有矿物包裹体。阴极发光(CL)图像中，锆石核部偶见被严重改造的韵律环带，其年龄无意义，未做测试；多数颗粒内部结构较为均匀，为变质重结晶锆石(图 3a)，对19颗该类锆石进行了20个点的同位素年代学和稀土微量元素分析。所有锆石稀土元素配分模式均具有轻稀土亏损、重稀土富集特征，Eu存在明显负异常(图 3c)。锆石Th、U含量分别为49×10-6~240×10-6和202×10-6~503×10-6，Th/U比值为0.23~0.48，207Pb/206Pb年龄介于2426~2528Ma之间(图 3b)。所有点的不一致线上交点年龄为2493±11Ma(MSWD=3.0)、207Pb/206Pb加权平均年龄为2494±8Ma(MSWD=3.6)(图 3d)。
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图 3 深熔长英质浅色体(样品ZZ8-2)的锆石年代学相关图 (a)锆石阴极发光(CL)图像，圆圈代表测试点位；(b)锆石207Pb/206Pb年龄与Th/U相关关系图；(c)锆石的球粒陨石标准化稀土元素配分图(Sun and McDonough, 1989)；(d)锆石的U-Pb谐和曲线图.测试点号参见表 1 Fig. 3 Chronological diagrams for the analyzed zircons from anatectic leucosome (Sample ZZ8-2) (a) CL images, and the circles represent the spots from which LA-ICP-MS measurements were taken; (b) Th/U ratios and 207Pb/206Pb relation diagram; (c) chondrite-normalized REE distribution pattern (Sun and McDonough, 1989); (d) U-Pb concordia diagram. The numbers refer to the analytical data listed in Table 1 |
所有锆石均为浅色，样品ZZ8-3和ZZ12-2中锆石颗粒较小，粒径约为20~100μm，柱状或浑圆状。样品ZZ9-5中锆石粒度较大，约200~500μm，多呈浑圆状。CL图像显示，锆石内部结构一致，无韵律环带，为变质成因锆石，部分颗粒见白色增生边(图 4a、图 5a和图 6a)。
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图 4 含榴角闪片麻岩(样品ZZ8-3)的锆石年代学相关图 (a)锆石阴极发光(CL)图像，圆圈代表测试点位；(b)锆石207Pb/206Pb年龄与Th/U相关关系图；(c)锆石的U-Pb谐和曲线图.测试点号参见表 2 Fig. 4 Chronological diagrams for the analyzed zircons from garnet-bearing hornblende gneiss (Sample ZZ8-3) (a) CL images, and the circles represent the spots from which LA-ICP-MS measurements were taken; (b) Th/U ratios and 207Pb/206Pb relation diagram; (c) U-Pb concordia diagram. The numbers refer to the analytical data listed in Table 2 |
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图 5 磁铁矿角闪片麻岩(样品ZZ9-5)的锆石年代学相关图 (a)锆石阴极发光(CL)图像，圆圈代表测试点位；(b)锆石的球粒陨石标准化稀土元素配分图(Sun and McDonough, 1989)；(c)锆石207Pb/206Pb年龄与Th/U相关关系图；(d、e)锆石的U-Pb谐和曲线图.测试点号参见表 1 Fig. 5 Chronological diagrams for the analyzed zircons from magnetite-hormblende gneiss Sample ZZ9-5) (a) CL images, and the circles represent the spots from which LA-ICP-MS measurements were taken; (b) chondrite-normalized REE distribution pattern (Sun and McDonough, 1989); (c) Th/U ratios and 207Pb/206Pb relation diagram; (d, e) U-Pb concordia diagram. The numbers refer to the analytical data listed in Table 1 |
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图 6 含榴角闪片麻岩(样品ZZ12-2)的锆石年代学相关图 (a)锆石阴极发光(CL)图像，圆圈代表测试点位；(b)锆石207Pb/206Pb年龄与Th/U相关关系图；(c)锆石的球粒陨石标准化稀土元素配分图(Sun and McDonough, 1989)；(d)锆石的U-Pb谐和曲线图.测试点号参见表 1 Fig. 6 Chronological diagrams for the analyzed zircons from garnet-bearing hornblende gneiss (Sample ZZ12-2) (a) CL images, and the circles represent the spots from which LA-ICP-MS measurements were taken; (b) Th/U ratios and 207Pb/206Pb relation diagram; (c) chondrite-normalized REE distribution pattern (Sun and McDonough, 1989); (d) U-Pb concordia diagram. The numbers refer to the analytical data listed in Table 1 |
含榴角闪片麻岩样品ZZ8-3中19颗锆石的19个点分析表明，锆石U含量变化不大，为74×10-6~235×10-6，17个点的Th/U比值非常小(0.002~0.039)，点No.7和No.17的Th/U比值分别为0.363和0.417(图 4b)。除点No.17(2666±13Ma)外，18个分析点的207Pb/206Pb年龄介于1870~1925Ma之间(图 4b)，207Pb/206Pb加权平均年龄为1903±7Ma(MSWD=1.05)(图 4c)。
对磁铁矿角闪片麻岩样品ZZ9-5中20颗锆石进行了20个点的同位素年代学和微量元素分析。结果表明，多数锆石的稀土元素配分模式具有轻稀土明显亏损、重稀土富集特征，Eu负异常明显；少数锆石轻稀土较为富集，个别颗粒具有Eu正异常或无异常特征(图 5b)。所有锆石Th、U含量分别为94×10-6~230×10-6和185×10-6~381×10-6，Th/U比值为0.48~0.72，207Pb/206Pb年龄介于2469~2524Ma之间(图 5c)。所有点的不一致线上交点年龄为2488±16Ma(MSWD=0.82)、207Pb/206Pb加权平均年龄为2492±6Ma(MSWD=1.08)(图 5d)。13个具有一致稀土配分模式数据点的不一致线上交点年龄为2487±18Ma(MSWD=0.63)、207Pb/206Pb加权平均年龄为2497±8Ma(MSWD=1.03)(图 5e)。图 5d和图 5e中两组年龄在误差范围内一致，但图 5d中有部分锆石的稀土配分模式明显与众不同，故推测相同成因锆石的U-Pb年龄与其稀土配分模式相关性不大。
含榴角闪片麻岩样品ZZ12-2中23颗锆石的23个点分析表明，绝大多数锆石的稀土元素配分模式一致，具有轻稀土明显亏损、重稀土富集特征，Eu存在明显负异常；锆石No.12、No.15和No.19的轻稀土较为富集，后两者Eu正异常(图 6c)。多数锆石Th、U含量很低(除No.15和No.19外)，分别为3×10-6~29×10-6和23×10-6~91×10-6。所有点的Th/U比值为0.16~0.90，207Pb/206Pb年龄介于2441~2572Ma之间(图 6b)。具一致稀土配分模式的20个分析点的207Pb/206Pb加权平均年龄为2507±15Ma(MSWD=3.3)(图 6d)。结合CL图像可知，该年龄应为变质锆石形成年龄。但稀土元素配分模式显示，锆石重稀土并没有表现平坦特征，显然该类锆石的生长并非与石榴石同期，应早于石榴石，故早于岩石峰期矿物组合所代表的变质时代。
3.3 磁铁矿黑云母石英片岩(ZZ8-5)该样品中锆石多浅色，粒度100~200μm不等，呈柱状或浑圆状。阴极发光图像显示，多数锆石发育明显的核边结构(图 7a)，分为两种成因类型。第一类锆石或锆石核部具有明显韵律环带，为典型岩浆成因。第二类锆石内部结构一致，发光性均匀，显示变质成因锆石特征，表现为第一类锆石的边部或独立的锆石颗粒，部分暗色边部外围发育亮白色窄边。
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图 7 磁铁矿黑云母石英片岩(样品ZZ8-5)的锆石年代学相关图 (a)锆石阴极发光(CL)图像，圆圈代表测试点位；(b)锆石207Pb/206Pb年龄与Th/U相关关系图；(c)第一类锆石的U-Pb谐和曲线图；(d)第二类锆石的U-Pb谐和曲线图.测试点号参见表 2 Fig. 7 Chronological diagrams for the analyzed zircons from magnetite-biotite-quartz schist (Sample ZZ8-5) (a) CL images, and the circles represent the spots from which LA-ICP-MS measurements were taken; (b) Th/U ratios and 207Pb/206Pb relation diagram; (c, d) U-Pb concordia diagram. The numbers refer to the analytical data listed in Table 2 |
在20颗第一类锆石上进行了20个点分析，测试点U含量变化非常大，为106×10-6~2385×10-6，Th/U比值为0.14~0.62，207Pb/206Pb年龄分散于2220~2562Ma之间(图 7b)。谐和图中多数点表现出明显Pb丢失，不一致线上交点年龄为2493±41Ma(MSWD=10.4)(图 7c)。这类锆石可能受后期变质作用的强烈影响，U-Pb体系发生明显重置，因此该年龄可能无实际意义。第二类锆石在23个颗粒上进行了23个点分析，结果表明，该类锆石U含和Th/U比值变化均很大，分别为53×10-6~2306×10-6和0.02~1.57。207Pb/206Pb年龄集中在2471~2550Ma(图 7b)，点No.5、No.24、No.28和No.35的U含量相对较高，207Pb/206Pb年龄分别为1841±17Ma、2373±20Ma、2394±14Ma和1643±19Ma(图 7b)。所有点的不一致线上交点年龄为2506±33Ma(MSWD=17)，位于谐和曲线附近的19个分析点的207Pb/206Pb加权平均年龄为2500±9Ma(MSWD=1.5)(图 7d)，代表变质锆石形成年龄。
3.4 含磁铁矿石榴黑云斜长片麻岩(ZZ12-6)该样品中锆石粒度20~300μm不等，形态多为柱状。CL图像显示两类锆石特征。一类锆石内部结构复杂，个别颗粒隐约可见环带，可能受到后期热事件影响，因此未做年龄测试；另一类锆石内部结构均匀(图 8a)，表现变质成因特征，对29颗该类锆石进行了31个点的同位素年代学和微量分析测试。多数锆石的稀土元素配分模式显示轻稀土明显亏损、重稀土富集特征，Eu明显负异常。锆石No.15、No.18和No.31重稀土较为平坦(图 8c)。锆石Th、U含量和Th/U比值分别为2×10-6~280×10-6、80×10-6~388×10-6和0.03~1.01，207Pb/206Pb年龄集中在2427~2551Ma，点No.13和No.17年龄分别为1943±12Ma和2211±29Ma(图 8b)。26个有效数据点的不一致线上交点年龄为2492±14Ma(MSWD=2.5)，谐和线附近的20个分析点的207Pb/206Pb加权平均年龄为2483±9Ma(MSWD=2.6)(图 8d)，表明该岩石同样经历了新太古代末期-古元古代初期的变质事件。与样品ZZ12-2类似，该样品锆石的稀土元素配分模式中，重稀土显示明显富集特征，故推测锆石的生长并非与石榴石同期，而应早于石榴石，即早于岩石峰期矿物组合的代表的变质时代。
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图 8 含磁铁矿石榴黑云斜长片麻岩(样品ZZ12-6)的锆石年代学相关图 (a)锆石阴极发光(CL)图像，圆圈代表测试点位；(b)锆石207Pb/206Pb年龄与Th/U相关关系图；(c)锆石的球粒陨石标准化稀土元素配分图(Sun and McDonough, 1989)；(d)锆石的U-Pb谐和曲线图.测试点号参见表 1 Fig. 8 Chronological diagrams for the analyzed zircons from magnetite-bearing garnet-biotite-plagioclase gneiss (Sample ZZ12-6) (a) CL images, and the circles represent the spots from which LA-ICP-MS measurements were taken; (b) Th/U ratios and 207Pb/206Pb relation diagram; (c) chondrite-normalized REE distribution pattern (Sun and McDonough, 1989); (d) U-Pb concordia diagram. The numbers refer to the analytical data listed in Table 1 |
华北克拉通前寒武纪基底由先存多个微陆块经后期的拼贴作用形成，在拼贴机制和拼贴时代等方面仍存在不同见解：(1)Zhao et al.(1998, 2001b, 2005)提出华北克拉通基底的最终拼合发生在约1.85Ga，是由两个前寒武纪微陆块(东部陆块和西部陆块)沿“华北中部造山带”(the Trans-North China Orogen)发生东向俯冲-碰撞-拼合形成的。(2)李江海等(2000)和Kusky and Li (2003)认为东部陆块和西部陆块的碰撞作用发生在约2.5Ga，且为西向俯冲，并将碰撞带定义为“中央造山带”(the Central Orogenic belt)，该造山带的划分与赵国春等提出的“华北中部造山带”类似，但边界略有不同。(3)Faure et al. (2007a)认为华北克拉通基底的形成是三个微陆块经~2.1Ga和1.9~1.8Ga两次碰撞事件完成的。约2.1Ga时，东部陆块发生西向俯冲，首先与阜平微陆块发生碰撞，形成聚合的东部陆块，而后整体继续俯冲，在1.9~1.8Ga与西部陆块发生再次碰撞，形成最终的华北克拉通基底。(4)Zhai (2011)和Zhai and Santosh(2011, 2013)认为华北克拉通的形成经历了两期克拉通化事件，第一期克拉通化发生在2.60~2.53Ga，七个微陆块被火山-沉积岩系焊接，完成初步克拉通化过程，形成现今规模的华北古陆；第二期克拉通化发生在1.95~1.82Ga，华北克拉通出现了以三条古元古代活动带为代表的裂谷-俯冲-增生-碰撞的陆内造山事件。
近三十年来，不同学者对“华北中部造山带”进行了全面的变质演化历史研究(综述参见肖玲玲和刘福来，2015)，发现该造山带内各杂岩区的变质岩石中普遍保留了早期进变质、峰期、峰后快速降压和晚期冷却等3~4阶段的变质矿物组合，记录了顺时针近等温降压型的变质作用P-T轨迹(王仁民等, 1991; Zhai et al., 1993; 梅华林, 1994; 刘福来, 1995; Guo et al., 1996, 2002; 刘树文, 1996; 王凯怡等, 1996; 郭敬辉等, 1998, 1999; 刘福来和沈其韩, 1999; Zhao et al., 1999, 2000a, b, 2001a, 2010b; 蒋宗胜等, 2011; 肖玲玲等, 2011, 2012, 2014; Xiao et al., 2011, 2014, 2017; Lu et al., 2013, 2014; Qian et al., 2013, 2015; Wang et al., 2014; Chen et al., 2015; Qian and Wei, 2016; Zhang et al., 2016)，这一变质过程显然与造山带的俯冲-碰撞-隆升作用有关。同时，大量的高精度的年代学数据表明，华北中部造山带几乎所有变质杂岩区均存在约1.9~1.8Ga的变质年龄记录，例如宣化(郭敬辉和翟明国, 2000; 郭敬辉等, 2001; Guo et al., 2005)、怀安(郭敬辉等, 1993; Guo et al., 2005; Xia et al., 2006; Zhao et al., 2008, 2010a; Wang et al., 2010; Liu et al., 2012; Santosh et al., 2013)、恒山(Kröner et al., 2006; Faure et al., 2007b; Trap et al., 2007)、阜平(Liu et al., 1985; Guan, 2000; Guan et al., 2002; 吴昌华等, 2000; Zhao, 2000; 孙敏和关鸿, 2001; Zhao et al., 2002; 程裕淇等, 2004; 杨崇辉等, 2004; 赵兰等, 2006; Trap et al., 2008; Zhang et al., 2009; Li et al., 2014)、五台(刘树文等, 2004; Liu et al., 2006; Trap et al., 2007)、吕梁(Liu et al., 2006; 刘树文等, 2007b; Trap et al., 2009b)、赞皇(Wang et al., 2003; Trap et al., 2009a; 肖玲玲等, 2011; 肖玲玲和王国栋, 2011; Xiao et al., 2013, 2014)、中条(刘树文等, 2007b)和太华(王国栋等, 2012, 2013; Wang et al., 2014)等杂岩区。近年来，约1.95Ga的变质年龄在华北中部造山带的怀安(Zhao et al., 2008, 2010a; Santosh et al., 2013)、恒山(Zhang et al., 2013; Qian et al., 2015)、五台(刘树文等, 2004; Liu et al., 2006; Qian et al., 2013)、吕梁(Liu et al., 2006; 刘树文等, 2007b; Trap et al., 2009b; Xiao et al., 2017)、中条(刘树文等, 2007b)和太华(蒋宗胜等, 2011; Huang et al., 2012; 王国栋等, 2012, 2013; Lu et al., 2013, 2014, 2015; 卢俊生等, 2014; Wang et al., 2014; Chen et al., 2015)等杂岩区相继被报道，这些数据支持华北中部造山带发生古元古代变质作用事件的时间至少应提前至约1.95Ga，且变质事件持续达100Myr。
4.2 华北克拉通~2.5Ga构造热事件~2.5Ga构造热事件在全球早前寒武纪地质历史上占据重要地位，为大规模的岩浆作用伴随强烈变质作用事件，岩浆作用与变质作用几乎同时发生。关于华北克拉通~2.5Ga岩浆事件的构造机制，目前存在岛弧岩浆作用和幔源岩浆底板垫托作用两种不同认识。前一观点认为微陆块拼贴作用导致俯冲板片的部分熔融，形成了华北克拉通大规模的岩浆事件(Li et al., 2002; Kröner et al., 2005; Wilde et al., 2005; Nutman et al., 2011)，华北克拉通东部大规模的TTG岩浆岩便形成于该过程。底板垫托观点认为高温的幔源基性岩浆侵入于下地壳或地壳底部，使上覆地壳物质发生部分熔融从而形成了花岗质岩浆(肖庆辉等, 2005; Yang et al., 2008)。
Zhao et al.(1998, 2001b, 2005)从变质作用角度支持地幔柱是新太古代晚期地壳形成和演化的主要构造机制。认为~2.5Ga变质事件主要发生在东、西部陆块，基底岩石拥有近等压降温型的逆时针P-T轨迹，其形成与大规模地幔岩浆底侵作用有关；三条造山带内仅记录1.95~1.80Ga变质事件，岩石普遍拥有近等温降压型的顺时针变质作用P-T轨迹，所记录的主要区域变质作用与大陆碰撞过程有关。然而，近年来的研究陆续发现，造山带内的部分杂岩区高压麻粒岩和角闪岩相变质岩石中同时记录了2.5~2.4Ga和1.95~1.80Ga两期变质事件，例如孔兹岩带中大青山-乌拉山地区(Dong et al., 2013; Wan et al., 2013; Liu et al., 2014)；华北中部造山带的赞皇(Xiao et al., 2014; 杜利林, 未发表数据)、阜平(程裕淇等, 2004)和承德(刘树文等, 2007a)等地区；位于华北克拉通东部陆块西北缘、紧邻中部造山带的建平(卢俊生, 未发表数据)和冀东(魏春景, 2018)杂岩区也有类似年龄记录。另外，关于华北克拉通~2.5Ga变质事件，最近有部分拥有顺时针变质作用P-T轨迹的高压麻粒岩相继在胶东(Liu et al., 2015)、冀东(Lu et al., 2017)和阴山(Wang and Guo, 2017)等地区被报道。由此看来，华北克拉通前寒武基底的构造演化是一个相当漫长且复杂的构造演化过程。
4.3 左权变质杂岩区变质年龄记录及其构造指示本文LA-ICP-MS锆石U-Pb年代学研究表明，左权变质杂岩记录了~1.9Ga和~2.5Ga的两组变质年龄。
第一组变质年龄(1903Ma)仅在1件样品(含榴角闪片麻岩样品ZZ8-3)中有所体现，锆石的207Pb/206Pb加权平均年龄为1903±7Ma，该变质年龄与华北克拉通中部造山带广泛记录的1.95~1.80Ga的变质事件时代一致，且与研究区的区域片麻理同期形成，应代表杂岩区峰期或近峰期阶段变质时代。
第二组变质年龄(2483~2507Ma)具有明显普遍性，同时被多种类型的岩石记录，包括深熔成因的长英质浅色体样品ZZ8-2、磁铁矿黑云母石英片岩样品ZZ8-5、磁铁矿角闪片麻岩样品ZZ9-5、含榴角闪片麻岩样品ZZ12-2和含磁铁矿石榴黑云斜长片麻岩样品ZZ12-6。其中，样品ZZ8-2中锆石的207Pb/206Pb加权平均年龄为2494±8Ma，由于该浅色体与寄主片麻岩具有协调一致的片麻理，故相应变质深熔事件应与片麻理同期或早于片麻理形成。样品ZZ8-5、ZZ9-5、ZZ12-2和ZZ12-6获得了类似的变质年龄，其锆石的207Pb/206Pb加权平均年龄分别为2500±9Ma、2497±8Ma、2507±15Ma和2483±9Ma。稀土配分模式特征表明，变质锆石的生长早于石榴石，而后者为代表的峰期矿物组合定向排列构成了片麻理，故变质锆石的形成应早于区域片麻理(~1.9Ga)。
区域上，与左权邻近的赞皇变质杂岩区岩石中更完整地保留了三个阶段的变质矿物组合，拥有类似的变质作用P-T轨迹(肖玲玲等, 2011, 2012; Xiao et al., 2011, 2014)。但不同的是，赞皇变质杂岩普遍记录了古元古代晚期(1821~1868Ma; Xiao et al., 2013)的变质年龄信息，且该年龄与区域片麻理的形成时间大体一致(Xiao et al., 2013)。另外，赞皇个别长英质片麻岩样品中获得了2507±15Ma的变质年龄(Xiao et al., 2014)，时间早于赞皇地区基底岩石约1.85Ga的大规模变质作用时代。
综上所述，左权变质杂岩2483~2507Ma的变质年龄指示了比区域片麻理更早的一期变质事件，是华北克拉通~2.5Ga构造热事件的反映。但相应岩石是来源于与杂岩区紧邻的华北克拉通东部陆块，还是代表了中部造山带太古宙古老基底？形成于何种构造环境？仍需做进一步工作加以核实。
5 结论本文通过细致的野外地质调查、岩相学、锆石U-Pb年代学和微量元素地球化学研究发现，左权变质杂岩区多种岩石类型中记录了新太古代末期和古元古代晚期两组变质年龄信息。
(1) 在含榴角闪片麻岩样品中获得了1903Ma的变质年龄，该年龄代表了岩石所经历的变质高峰期或近峰期阶段变质时代。
(2) 在深熔成因的长英质浅色体、磁铁矿黑云母石英片岩、磁铁矿角闪片麻岩、含榴角闪片麻岩和含磁铁矿石榴黑云斜长片麻岩共5件样品中获得了2483~2507Ma的变质年龄，相应变质事件早于杂岩区区域片麻理发生，与华北克拉通前寒武纪基底约25亿年大规模构造热事件有关。
致谢 感谢中国地质大学(北京)激光等离子质谱实验室在实验测试过程中给予的帮助；感谢审稿专家给予本文的中肯建议。
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