2013, Vol. 29
2. 中国科学院地质与地球物理研究所，北京 100029;
3. 西北大学地质学系，西安 710069
2. Institute of Geology and Geophysics, Chinese Academy of Sciences, Beijing 100029, China;
3. Department of Geology, Northwest University, Xi’an 710069, China
华北克拉通是中国最主要的克拉通之一, 记录了最早~3.8Ga的构造历史(图 1a, Liu et al., 1992, 2008a; Song et al., 1996; 万渝生等, 2001；Wu et al., 2008)。华北克拉通的形成经历了三期重要的地质事件：~2.7Ga主要的陆壳生长, ~2.5Ga克拉通化事件和2.0~1.8Ga克拉通的最终形成(程裕淇和张寿广, 1982; 沈其韩等, 1992; 赵宗溥, 1993；程裕淇, 1994； 白瑾等, 1996; 翟明国和卞爱国, 2000; Zhai et al., 2005; Zhai and Liu, 2003; Zhai and Santosh, 2011；Zhao, 2001; Zhao et al., 2001, 2003a, b, 2005; Kusky and Li, 2003; Kusky et al., 2007a, b; Santosh, 2010)。古元古代末-新元古代, 华北克拉通进入稳定的地台发展阶段(赵宗溥, 1993；翟明国和卞爱国, 2000; Zhai and Liu, 2003; 翟明国和彭澎, 2007；Lu et al., 2002, 2008; Kusky and Li, 2003)。华北克拉通有火山岩夹层的典型的大陆裂谷沉积序列被称为长城系(1.8~1.6Ga)、蓟县系(1.6~1.0Ga)和青白口系(1.0~0.8Ga)(高振西等, 1934; 陈晋镳等, 1980; 全国地层委员会, 2001)。近年来在青白口系下马岭组中发现了~1.37Ga的凝灰岩(Gao et al., 2007, 2008)和侵入其中的~1.32Ga的辉绿岩床(李怀坤等, 2009；Zhang et al., 2009, 2012), 因而Qiao et al.(2007)、高林志等(2009)和李怀坤等(2009)等建议建立一个以下马岭组为主的待建系, 时代为1.4~1.0Ga, 将蓟县系的时代划为1.6~1.4Ga。与华南克拉通元古宙沉积地层对比, 除在南缘零星出露一些震旦系, 华北克拉通整体缺乏南华纪(800~630Ma)和震旦纪(630~540Ma)地层(Zhai et al., 2003)。同样, 1.3~0.6Ga的岩浆岩和变质岩在华北克拉通也出露较少, 而在华南克拉通却分布广泛(Li et al., 1995, 1997, 2002, 2003; Li, 1997, 1999; 张传恒等, 2007；Chu et al., 2005；Zhang et al., 2005, 2008；高林志等, 2010a), 也被一些学者认为是区分华南克拉通和华北克拉通的标志之一(Li et al., 2007b; Liu et al., 2008b)。1.3~0.6Ga的岩浆活动和变质作用被认为是与Rodinia超大陆的聚合和裂解相联系的, 尽管对聚合和裂解的具体时间及各大陆的位置仍有争议(Hoffman, 1991; Hoffmann et al., 2004；Dalziel, 1991, 1997; Li et al., 1995, 2002, 2003; Fitzsimons, 2000; Karlstrom et al., 2001; Condie, 2001; Zhai, 2001; Rogers and Santosh, 2004; Lu et al., 2008; Rino et al., 2008；李江海, 1998；李江海和穆剑, 1999；徐备, 2001；陆松年等, 2004, 2005； Condon et al., 2005；Zhang et al., 2005；Chu et al., 2005；Gradstein et al., 2005)。近年对华北东缘和北缘新元古代沉积岩碎屑锆石(Luo et al., 2006；Li et al., 2007b; 高林志等, 2010b；Gao et al., 2011；Hu et al., 2012)及侵入岩中捕获锆石(Yang et al., 2004；张华锋等, 2009)的研究揭示出1.3~1.0Ga的年龄记录, 在北朝鲜也发现了~1.2Ga的花岗岩体(Zhao et al., 2006)。华北地区陆续报道了900~800Ma的基性岩墙群和酸性火山岩(Peng, 2010；Peng et al., 2011a, b; Wang et al., 2011, 2012；柳永清等, 2005; 彭润民等, 2010)。1.3~0.8Ga的岩浆岩或锆石年龄记录在华北克拉通是否普遍存在, 还是具有局部性？华北克拉通有无0.8~0.6Ga的年龄记录？对这些问题的深入研究将对理解华北克拉通元古宙的演化及其与华南克拉通的关系都具有重要意义。碎屑沉积岩是其源区出露岩石的天然混合样品, 是探讨克拉通形成和演化的主要途径之一(Belousova et al., 2009; Wan et al., 2011a, b；Hawkesworth et al., 2010)。沉积岩中的碎屑锆石能够抗风化和磨蚀, 并且能保持U-Pb同位素体系较高的封闭温度, 通常可以保存源区曾经存在的岩石的年龄记录, 因而本文选择位于华北克拉通早前寒武纪基底和中晚元古代盖层发育较完整的燕辽裂陷槽中的北京西山地区为研究区, 对显生宙地层中的碎屑岩进行碎屑锆石U-Pb年代学研究, 目的是揭示华北克拉通前寒武纪地质事件, 特别是现今出露的岩石及中晚元古代沉积岩未能全面揭示的元古宙地质事件。
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图 1 中国大地构造简图(a, 据Zhao et al., 2006修改)和华北克拉通前寒武纪地质简图(b, 据Peng et al., 2011b修改) Fig. 1 Tectonic map of China showing the location of the Tarim, North China and South China Cratons and the main orogens(a, modified after Zhao et al., 2006)and Archean-Paleoproterozoic basement and Late Paleoproterozoic to Neoproterozoic cover of the North China Craton(b, modified after Peng et al., 2011b) |
在华北克拉通前寒武纪结晶基底之上, 不整合覆盖着大面积的古-新元古代沉积盖层, 被划分为长城系(1800~1600Ma)、蓟县系(1600~1400Ma)、待建系下马岭组(1400~1000Ma)和青白口系(1000~800Ma)(全国地层委员会, 2001；乔秀夫等, 2007；高林志等, 2009, 2010a；李怀坤等, 2009, 2010；苏文博等, 2010), 主要分布于南部的熊耳裂陷槽、中部的燕辽裂陷槽、北缘裂谷和东缘裂谷(图 1, 翟明国和彭澎, 2007)。北京西山地区位于燕辽裂陷槽, 出露的地层有中元古代蓟县系雾迷山组-铁岭组、下马岭组和新元古代青白口系、寒武系、奥陶系、石炭系和侏罗系。地层走向由近东西向转近南北向呈弧形展布, 这些地层被中生代花岗质或闪长质岩体或岩脉侵入(图 2)。蓟县系雾迷山组为一套含叠层石的白云岩；洪水庄组主要为灰黑色炭质页岩；铁岭组主要为含叠层石的白云岩。下马岭组主要由灰绿色、灰黑色页岩、粘土岩和铁质粉砂岩组成。青白口系长龙山组主要由砾岩、石英砂岩、长石石英砂岩和钙质、粉砂质页岩组成；景儿峪组为一套中-薄层状微晶灰岩。下马岭组平行不整合于蓟县系铁岭组之上, 又被青白口系长龙山组平行不整合覆盖, 这两个不整合分别代表芹峪运动和蔚县运动(陈晋镳等, 1980)。寒武系平行不整合于青白口系之上, 主要为厚层状含三叶虫的碳酸盐岩, 部分夹薄层细碎屑岩(图 3、图 4b)。奥陶系与寒武系整合接触, 主要由厚层状灰岩和白云岩组成。石炭系清水涧组在本地区出露不全, 平行不整合于奥陶系之上, 主要由含砾砂岩和泥岩组成。侏罗系呈角度不整合覆盖于蓟县系、青白口系、下马岭组、寒武-奥陶系和石炭系之上, 为一套火山-沉积岩, 火山岩以安山岩和玄武岩为主, 沉积岩包括凝灰岩、凝灰质砾岩、砂岩、凝灰质砂岩、杂砂岩、细砂岩、粉砂岩、泥岩和页岩等, 部分地层夹有煤线, 产植物化石。详细的地层组合见图 3。
为研究显生宙沉积岩中碎屑锆石所揭示的前寒武纪地质事件, 本文分别在北京西山地区的侏罗系窑坡组和寒武系徐庄组中选取碎屑岩样品进行锆石U-Pb测年。样品08QY01和08QY03分别采自芹峪北侏罗系窑坡组夹于泥岩中的薄层长石质岩屑细砂岩和粉砂质泥岩(图 4a), 采样位置见图 2, GPS点为N40°03′56.2″, E115°51′16.6″, H607m。样品08QY03的层位在样品08QY01之上, 二者相距大约20cm(图 4a)。长石质岩屑细砂岩样品08QY01的主要组成为：火山岩碎屑45%, 石英30%, 斜长石10%, 基质10%。碎屑矿物呈次圆状-次棱角状, 有两组不同的粒径, 小的为0.1~ 0.2mm, 大的为0.3~0.4mm, 显示较差的磨圆和分选(图 5a, b)。粉砂质泥岩样品08QY03由非常细小(＜0.05mm)的长英质矿物及黑云母、绢云母和粘土矿物等组成(图 5c)。样品08QY06采自芹峪东北寒武系徐庄组泥晶灰岩中夹的薄层紫红色钙质细砂岩(图 2、图 4b), GPS点为N40°03′07.5″, E115°53′03.4″, H286 m。细砂岩碎屑矿物粒度为0.1~0.2mm, 主要矿物有方解石(50%)和石英(30%)以及少量斜长石(10%)和白云母(＜5%)。方解石多呈次圆状-次棱角状, 部分由边缘-中部被蚀变分解而浑浊不清楚；石英和长石多呈棱角状, 显示出较差的磨圆(图 5d)。
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图 2 北京西山雁翅地区地质简图(据北京市地质矿产局地质调查所, 1994①修改) Fig. 2 Sketch geological map of Yanchi area, Western Hills, Beijing |
① 北京市地质矿产局地质调查所. 1994. 1:5万雁翅幅地质图
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图 3 北京西山雁翅地区地层柱状图(据北京市地质矿产局地质调查所, 1994修编) Fig. 3 Integrated stratigraphic column of Yanchi area, Western Hills, Beijing |
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图 4 研究区侏罗系窑坡组(a)、寒武系徐庄组(b)野外露头及采样位置 Fig. 4 Field outcrop of Jurassic Yaopo Formation(a), Cambrian Xuzhuang Formation(b)and the sample location |
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图 5 侏罗系窑坡组长石质岩屑细砂岩08QY01(a、b)和粉砂质泥岩08QY03(c)及寒武系徐庄组钙质细砂岩08QY06(d)的显微照片 (a)为单偏光, (b-d)为正交偏光.Lv-火山岩岩屑；Q-石英；Pl-斜长石；Cc-方解石 Fig. 5 Micrographs of feldspathic lithic fine sandstone sample 08QY01(a, b)and silty mudstone sample 08QY03(c)from the Jurassic Yaopo Formation and calcareous fine sandstone sample 08QY06(d)from the Cambrian Xuzhuang Formation Micrograph(a)is under the plane-polarized light and(b, c and d)are under the cross-polarized light. Lv-volcanic lithic fragment; Q-quartz; Pl-plagioclase; Cc-calcite |
将野外采得的样品洗净泥土并晾干, 粉碎至60目以下, 先用磁选和重液方法粗选锆石, 然后在双目镜下将干净的锆石颗粒逐一挑出。将挑好的锆石颗粒粘在双面胶上, 固定于透明的环氧树脂中, 和树脂一起打磨抛光, 直至露出锆石的内部以适合LA-ICP-MS分析。抛光后的锆石分别进行透射光和反射光照相, 以观察其抛光面和内部结构情况。CL图像用来进一步反映锆石的内部结构特征。
样品的锆石CL图像在中国科学院地质与地球物理研究所扫描电镜实验室用LEO 1450VP扫描电镜拍摄, 锆石U-Pb同位素和元素含量在西北大学大陆动力学国家重点实验室使用带有Geolas 200M激光剥蚀系统的Agilent 7500a ICP-MS同时原位测定。哈佛大学的标准锆石91500作为计算U-Pb同位素的外标, 其参考值加权平均206Pb/238U年龄为1065.4±0.6Ma(Wiedenbeck et al., 1995)；元素含量的计算采用硅酸盐玻璃NIST SRM 610为外标, 29Si为内标。锆石年龄测试用的激光束斑直径为20μm, 剥蚀深度为20~40μm。详细的仪器参数设置及分析技术见柳小明等(2007)。
LA-ICP-MS测得的U-Pb同位素和元素含量原始数据使用GLITTER 4.0软件(Macquarie University)进行处理。由于LA-ICP-MS分析方法不能准确测量204Pb含量, 而且年轻的锆石(＜1000Ma)放射性Pb的积累较少, 普通铅的存在会对测试结果带来很大误差, 因此在分析数据时, 首先剔除了204Pb含量明显高于背景值的数据, 然后在统计中将不谐和度大于10%的测试点剔除, 大部分参加统计的年龄数据是近似谐和的。另外, 由于年轻锆石中放射成因207Pb积累较少, 207Pb的分析结果易存在较大误差, 因此对年轻锆石(＜1000Ma)使用206Pb/238U年龄。较老的锆石(>1000Ma)会存在一定程度的铅丢失, 但是207Pb和206Pb在相同的初始条件和共同的地质构造环境中具有同步变化的特征, 两者的比值保持相对稳定, 因此采用207Pb/206Pb年龄代表锆石的形成年龄(Black et al., 2003)。锆石的U-Pb年龄结果使用Isoplot3.0软件(Ludwig, 2003)计算。
3 锆石U-Pb测年结果 3.1 寒武系钙质细砂岩(样品08QY06)采自寒武系徐庄组的钙质细砂岩样品08QY06中的大部分锆石粒度为50~90μm, 少数超过100μm。锆石外形呈次圆状和次棱角状, 多数保持较自形的棱柱状(图 6a), 指示较差的磨圆和较近的源区。在104颗锆石颗粒上分析了108个点(表 1)。其中76个不谐和度＜10%的分析点被选出进行年龄统计。这些分析点的年龄分布于3556~489Ma, 大部分在1801~489Ma, 产生1460~1281Ma和1246~970Ma两个主要的年龄峰, 加权平均值分别为1378±32Ma(n=15)和1136±36Ma(n=23), 此外还有930~885Ma、843~782Ma、759~715Ma和525~489Ma的年龄组, 加权平均值分别为912±19Ma(n=6)、814±27Ma(n=6)、740±16Ma(n=6)和507±14Ma(n=7)。另外还有少数年龄分布在~1.56Ga和~630Ma(图 7a, b)。锆石的CL图像揭示1460~1281Ma的锆石大部分是具有震荡环带的岩浆锆石(图 6a), 它们的U、Th含量较高, 分别为203×10-6~625×10-6和66×10-6~527×10-6, Th/U除了一个极高的2.31外, 大部分在0.23~1.20(表 1、图 8a)。1246~970Ma的锆石的CL图像显示大部分是具有震荡环带的岩浆锆石, U、Th含量较高, 分别为116×10-6~657×10-6和77×10-6~776×10-6；Th/U为0.44~1.53。其中少数几颗锆石具有均一的内部结构或核边结构, 这些内部均一的锆石或具核边结构的锆石的边部年龄集中在1193~1071Ma之间, 具有较低的Th/U(0.21~0.43), 可能为变质成因的锆石(如图 6a中测点66和67)。930~715Ma的锆石既有具震荡环带的岩浆锆石, 又有内部均一的或补丁状结构的可能为变质成因的锆石, 其中一颗锆石具有1277Ma的核部和809Ma的变质边(图 6a中测点46和47)。930~715Ma具震荡环带结构的锆石的U、Th含量不高, 但是有较高的Th/U, 分别为99×10-6~223×10-6、85×10-6~183×10-6和0.5~1.41；而具均一或补丁状结构的锆石有较高的U含量和较低的Th含量及Th/U, 分别为220×10-6~794×10-6、23×10-6~213×10-6和0.04~0.47(图 6c)。~1.56Ga的三个分析点是两颗锆石测试的结果, 这两颗锆石具有震荡环带结构, U、Th含量和Th/U分别为304×10-6~528×10-6、272×10-6~370×10-6和0.52~1.22。650~489Ma的锆石的CL图像显示它们大部分是具有震荡环带结构的岩浆锆石, 它们的U、Th含量和Th/U分别为123×10-6~432×10-6、120×10-6~585×10-6和0.65~1.60(图 6c)。除此之外, 碎屑锆石还记录了2469Ma、2089Ma及1801~1657Ma的年龄。一颗3556Ma的岩浆锆石是该地区目前发现的最古老的锆石, 它的U、Th含量和Th/U分别为250×10-6、173×10-6和0.69(表 1、图 6a、图 8a)。
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表 1 北京西山地区寒武系徐庄组钙质细砂岩（样品08QY06)锆石LA-ICP-MS U-Pb分析结果 Table 1 LA-ICP-MS zircon U-Pb dating data of Cambrian calcareous fine sandstone (sample 08QY06) from Xuzhuang Formation in the Western Hills of Beijing |
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图 6 北京西山地区寒武系和侏罗系碎屑岩代表性碎屑锆石的CL图像 (a)-寒武系钙质细砂岩样品08QY06；(b)-侏罗系长石质岩屑细砂岩样品08QY01；(c)-侏罗系粉砂质泥岩样品08QY03.括号内为Th/U Fig. 6 CL images of representative detrital zircon grains from Cambrian and Jurassic clastic rocks in the Western Hills of Beijing (a)-Cambrian calcareous fine sandstone, sample 08QY06；(b)-Jurassic feldspathic lithic fine sandstone, sample 08QY01;(c)-Jurassic silty mudstone, sample 08QY03. Data in the brackets are Th/U ratios |
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图 7 北京西山地区寒武系和侏罗系碎屑锆石U-Pb谐和曲线图和年龄分布柱状图 (a、b)-寒武系钙质细砂岩样品08QY06；(c、d)-侏罗系长石质岩屑细砂岩样品08QY01；(e、f)-侏罗系粉砂质泥岩样品08QY03.图上只显示不谐和度小于10%的分析点.＜1000Ma的分析点采用206Pb/238U年龄；>1000Ma的分析点采用207Pb/206Pb年龄 Fig. 7 U-Pb concordia diagrams and age histograms of the detrital zircons from the Cambrian and Jurassic clastic rocks in the Western Hills of Beijing showing their age distributions (a, b)-Cambrian calcareous fine sandstone, sample 08QY06;(c, d)-Jurassic feldspathic lithic fine sandstone, sample 08QY01;(e, f)-Jurassic silty mudstone, sample 08QY03. Results with discordance less than 10% from these samples are shown in these diagrams. Age data of ＜1000Ma are shown by 206Pb/238U age and those of >1000Ma are shown by 207Pb/206Pb age in age histograms |
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图 8 北京西山地区寒武系和侏罗系碎屑锆石的Th/U-年龄图 (a)-寒武系钙质细砂岩样品08QY06；(b)-侏罗系长石质岩屑细砂岩样品08QY01；(c)-侏罗系粉砂质泥岩样品08QY03.图上只显示不谐和度小于10%的分析点.＜1000Ma的分析点采用206Pb/238U年龄；>1000Ma的分析点采用207Pb/206Pb年龄 Fig. 8 Th/U vs. age diagrams of detrital zircons from Cambrian and Jurassic clastic rocks in the Western Hills of Beijing (a)-Cambrian calcareous fine sandstone, sample 08QY06；(b)-Jurassic feldspathic lithic fine sandstone, sample 08QY01;(c)-Jurassic silty mudstone, sample 08QY03. Results with discordance less than 10% from these samples are shown in these diagrams. Data ＜1000Ma are shown by 206Pb/238U age and those >1000Ma are shown by 207Pb/206Pb age in these diagrams |
采自芹峪北侏罗系的长石质岩屑细砂岩样品08QY01中的锆石颗粒大小不均一, 小的粒度约40~60μm, 大的约80~100μm, 最大的可达170μm。锆石外形呈次圆状和次棱角状(图 6b), 显示出较差的分选和磨圆。在67颗锆石颗粒上分析了68个点(表 2)。其中49个不谐和度＜10%的分析点被选出进行年龄统计。这些分析点的年龄分布在2815~247Ma, 集中于2536~2440Ma和1902~1525Ma范围内(图 7c, d)。前者的加权平均年龄为2488±25Ma(n=8), 后者又可细分为两个主要的年龄峰(1806~1662Ma和1638~1525Ma)和一个次要的年龄组(1902~1861Ma), 加权平均值分别为1741±22Ma(n=15)、1596±30Ma(n=9)和1882±48Ma(n=3)。另外, 有少数锆石年龄分布于~2.77Ga、~1.2Ga、488Ma和256Ma(图 7c, d)。CL图像显示, 2536~2440Ma的锆石既有具震荡环带的岩浆锆石, 又有具均一和补丁状结构的变质锆石(图 6b)。这些锆石的U、Th含量不高, 但Th/U较高；分别为55×10-6~353×10-6、55×10-6~325×10-6和0.56~1.61(表 2、图 8b)。1806~1662Ma的锆石内部结构种类较多, 有震荡环带、条带状、补丁状和均一结构的, 大多发光较暗, 但是它们的U、Th含量不高, 而Th/U较高, 分别为61×10-6~163×10-6、32×10-6~156×10-6和0.54~1.38(图 8b)。1638~1525Ma的锆石大多是具震荡环带的岩浆锆石, 但发光较暗。这些锆石大多U、Th含量不高, 但是Th/U较高, 分别为73×10-6~209×10-6、55×10-6~260×10-6和0.64~2.40(图 8b)。3颗~1.88 Ga的锆石CL图像显示出补丁状和均一的内部结构, 发光较暗, 但U、Th含量不高, 而Th/U较高, 分别为66×10-6~182×10-6、63×10-6~241×10-6和0.48~1.33(图 8b)。3颗~2.77Ga的锆石内部结构既有具震荡环带的, 又有均一状的, U、Th含量和Th/U分别为65×10-6~210×10-6、61×10-6~178×10-6和0.5~2.62。两颗~1.2Ga的锆石, 内部结构分别呈均一状和补丁状, 它们的U、Th含量和Th/U分别为137×10-6~472×10-6、90×10-6~154×10-6和0.33~0.66。两颗~488Ma的锆石均具有震荡环带结构, 但是一颗具较高的Th/U(0.81), 另一颗Th/U较低, 为0.04。4颗~256Ma的锆石既有震荡环带结构的岩浆锆石, 又有结构均一的锆石, 它们的U、Th含量较高, 分别为214×10-6~754×10-6和157×10-6~387×10-6, Th/U为0.22~1.81。除这些年龄组外, 碎屑锆石还记录了~2.3Ga、~2.0Ga和848Ma的年龄, 其中848Ma的锆石是一颗具震荡环带的岩浆锆石, 它的Th/U为0.43(图 6b)。
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表 2 北京西山地区侏罗系长石质岩屑细砂岩（样品08QY01)锆石LA-ICP-MS U-Pb分析结果 Table 2 LA-ICP-MS zircon U-Pb dating data of Jurassic feldspathic lithic fine sandstone ( sample 08QY01) in the Western Hills of Beijing |
采自芹峪北侏罗系的粉砂质泥岩样品08QY03中的锆石多呈次棱角状, 其中部分呈长柱状自形晶。锆石颗粒较小, 多为40~70μm, 有些长柱状的锆石, 长轴可达100μm以上(图 6c)。该样品分选出的锆石数量不多, 共在51颗锆石颗粒上测试了54个点, 并且该样品分析点中不谐和的点较多, 因此只有23个不谐和度＜10%的分析点被选出进行年龄统计。尽管统计点不多, 但仍然可以看出该样品的碎屑锆石记录了与长石质岩屑细砂岩样品08QY01相似的年龄信息(图 7)。碎屑锆石年龄主要分布于~1.8Ga和~186Ma。此外, 还有3颗~2.5Ga、1颗~2.0Ga、3颗~1.6Ga、1颗478Ma和2颗~230Ma的锆石(图 7e, f)。除了中生代的年龄组外, 其他年龄分布与粉砂岩样品08QY01基本一致。~1.8Ga的碎屑锆石年龄范围为1819~1790Ma, CL图像显示这些锆石有震荡环带和均一两种结构, 多数发光较暗, 但U、Th含量都不高, 而Th/U比较高, 分别为123×10-6~232×10-6、79×10-6~213×10-6和0.51~1.07(图 8c)。~186Ma的锆石有清晰的震荡环带结构和长柱状外形, 可能是火山岩锆石(图 6c)。这些锆石的U、Th含量和Th/U都较高, 分别为546×10-6~953×10-6、261×10-6~560×10-6和0.31~0.75(图 8c)。~2.5Ga的锆石为具补丁状结构的变质锆石, U、Th含量和Th/U分别为141×10-6~189×10-6、65×10-6~111×10-6和0.42~0.60(图 8c)。~1.6Ga的锆石具有震荡环带结构和条带状结构, 其中有一颗锆石具1790Ma的核部和1610Ma的生长边(图 7c中测点41和42)。除了这个1610Ma的生长边有较高的U含量(507×10-6)和较低的Th/U(0.17)外, 另外两个~1.6Ga的锆石均具较低的U、Th含量和较高的Th/U, 分别为70×10-6~72×10-6、62×10-6~71×10-6和0.88~0.99(表 3、图 8c)。除这些锆石外, 其他年龄的锆石大多是具有震荡环带或扇形结构的岩浆锆石(图 6c)。
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表 3 北京西山地区侏罗系粉砂质泥岩（样品08QY03)锆石LA-ICP-MS U-Pb分析结果 Table 3 LA-ICP-MS zircon U-Pb dating data of Jurassic silty mudstone ( sample 08QY03) in the Western Hills of Beijing |
岩石学研究显示, 北京西山地区侏罗系的长石质岩屑细砂岩中含有45%的火山岩碎屑和10%的基质；寒武系的钙质细砂岩中含有50%的方解石, 体现出较低的成分成熟度。这两种岩石和侏罗系的粉砂质泥岩尽管粒度较细, 但其中的矿物和锆石多呈次圆状-次棱角状, 甚至棱角状, 碎屑矿物粒径大小不均匀, 锆石多为棱柱状或长柱状自形晶(图 5、图 6), 显示出较差的分选及磨圆, 指示这些碎屑岩中的碎屑物质来源于较近的源区。华北克拉通自古元古代末克拉通化完成、中晚元古代发育裂陷槽之后, 于早古生代发育代表稳定的克拉通盆地陆表海环境的以厚层碳酸盐岩为主的沉积, 这一时期的构造和岩浆活动是微弱的(马永生, 1994；梅冥相等, 1997；程裕淇, 1994), 因北京西山地区位于华北克拉通的中部靠北, 可初步推断寒武系钙质细砂岩的碎屑沉积物可能大部分来自华北克拉通内部。寒武系钙质细砂岩样品08QY06中碎屑锆石的主要年龄峰值~1.38Ga和少数~2.5Ga、~2.1Ga、1.8~1.65Ga和~1.56Ga的年龄正对应华北克拉通新太古代-元古宙重要的构造-岩浆-热事件发生的时代(详见下文), 而数量较少的~507Ma的碎屑锆石年龄在华北目前未见报道, 可能是该时期的构造和岩浆活动较微弱的原因。燕山地区的早侏罗世盆地(包括南大岭组和窑坡组)是晚古生代-早中生代地台活化之后的平静期形成的弱伸展盆地(赵越等, 2002；张岳桥等, 2007；马寅生等, 2002；孟庆任等, 2002)。窑坡组的泥岩和粉砂质泥岩组合代表半深水相的湖泊沉积环境(张岳桥等, 2007), 由于窑坡组的碎屑物质组成显示出较低的成分和结构成熟度, 其源区可能是较近的华北克拉通内部或北缘。窑坡组细碎屑岩中碎屑锆石~2.5Ga、~1.8Ga、~1.74Ga和~1.6Ga的年龄峰值及少量~2.77Ga和~1.88Ga的年龄组对应华北克拉通新太古代-古元古代重要的地质事件发生的时代, 华北克拉通应是提供这些碎屑物质的主要源区；少数~256Ma和~233Ma的碎屑锆石可能来自受古亚洲洋俯冲影响的华北北缘的岩浆岩(Zhang et al., 2009a)；~186Ma早侏罗世的碎屑锆石具有清晰的震荡环带结构和长柱状外形, 是火山岩锆石常具有的特征, 它们可能来自窑坡组下伏的194~180Ma的南大岭组火山岩(赵越等, 2002, 2006)。
4.2 碎屑锆石记录的华北克拉通前寒武纪地质事件北京西山地区寒武系和侏罗系中的碎屑锆石大部分来自华北克拉通内部, 少量来自其北缘, 因而这些碎屑锆石年龄可记录华北克拉通的地质事件, 特别是现今出露的岩石中尚未揭示出的前寒武纪地质事件。
4.2.1 最古老的锆石年龄寒武系钙质细砂岩样品08QY06中3556Ma的岩浆型碎屑锆石年龄是北京西山地区目前发现最古老的锆石年龄。华北克拉通最古老的古太古代岩石出露于东北铁架山和冀东曹庄地区, 锆石U-Pb年龄主要为~3.8Ga和~3.3Ga(Liu et al., 1992, 2008a; Song et al., 1996; 万渝生等, 2001；Wu et al., 2008)。研究区沉积岩中3556Ma的岩浆型碎屑锆石年龄以及同属燕辽裂陷槽的北京昌平地区的青白口系长龙山组中3372Ma的碎屑锆石年龄(任荣等, 2011)指示华北克拉通东部的古太古代岩石可能为这些碎屑岩的物源之一。
4.2.2 2.9~2.7Ga的地壳生长和~2.5Ga的克拉通化事件尽管数量不多, 北京西山寒武系和侏罗系碎屑锆石还记录了~2.5Ga的年龄峰值和少量~2.77Ga的年龄(图 7)。CL图像显示, 这些锆石既有具震荡环带结构的岩浆成因的锆石, 又有内部均一和补丁状结构的变质成因的锆石(图 6), 这两种结构的锆石Th/U都比较高, 为0.42~2.62(图 8)。2.9~2.7Ga被认为是华北克拉通大规模陆壳生长的时期(张宗清, 1998；Wu et al., 2005)。该时期的岩石有鲁西地区的绿岩带(Polat et al., 2006; Cheng and Kusky, 2007)以及鲁西、胶东、恒山、阜平、中条山、冀东、河南和内蒙等地的TTG片麻岩(Guan et al., 2002; Liu et al., 2009; Jahn et al., 2008；Wilde et al., 2004；Zhao et al., 2002；Geng et al., 2006; Wan et al., 2011b; 董晓杰等, 2012; Zhu et al., 2013)。除北京西山寒武系和侏罗系碎屑锆石对2.9~2.7Ga事件的记录外, 华北古元古代末-新元古代沉积盆地碎屑锆石年龄分布也形成~2.7Ga的峰, 支持2.9~2.7Ga的岩石曾普遍存在(图 9)。华北克拉通许多正片麻岩, 包括形成于2.6~2.5Ga的TTG和花岗质片麻岩具有2.9~2.7Ga的Hf和Nd模式年龄, 被认为这些岩石的形成时代或原岩岩浆从地幔中抽取的时代是2.9~2.7Ga, 反映华北克拉通在该时期有大规模的大陆地壳形成(Liu et al., 2009; Jiang et al., 2010; Jahn et al., 2008)。~2.5Ga的碎屑锆石年龄峰值对应华北克拉通前寒武纪一期重要的构造-岩浆-热事件发生的时代。~2.5Ga也是华北古元古代末-新元古代沉积盆地碎屑锆石年龄中一个主要的年龄峰值(图 9)。华北克拉通~2.5Ga时发生广泛的变质作用和岩浆岩的侵入, 几乎所有老于2.6Ga的太古宙岩石都经历了~2.5Ga的高角闪岩相-麻粒岩相的变质作用(皮金, 1980；Compston et al., 1983; Jahn and Zhang, 1984; Jahn et al., 1987, 2008；伍家善等, 1991；王楫等, 1995；Song et al., 1996; Kröner et al., 1998), 并有大量TTG、紫苏花岗岩和花岗岩的侵位(Liu et al., 1990；刘敦一等, 1997; 伍家善等, 1991；Kröner et al., 1998, 2005a, b；苏尚国等, 1999；刘树文等, 2000, 2007; 王凯怡等, 2000；张维杰等, 2000；Guan et al., 2002；路孝平等, 2004；简平等, 2005；万渝生等, 2005； Zhao et al., 2002, 2008a, b; 高林志等, 2005)、镁铁质岩墙群的侵入(毛德宝等, 1999；Guo et al., 2005)以及青龙、五台和固阳等花岗-绿岩带的形成(罗殿文等, 2000；王凯怡等, 2000；Wilde et al., 2004, 2005；陈斌等, 2006)。该时期被认为是华北克拉通发生克拉通化的时期(伍家善等, 1991；Zhai and Liu, 2003; 翟明国和卞爱国, 2000；翟明国, 2004；Zhai et al., 2005；Zhai, 2011)。
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图 9 华北克拉通古元古代末-新元古代沉积岩碎屑锆石207Pb/206Pb年龄分布图 碎屑锆石数据据Darby and Gehrels, 2006; Li et al., 2007a, b; Luo et al., 2006; Zhou et al., 2008; Wan et al., 2011a, b; Gao et al., 2011; Zhu et al., 2011; 万渝生等, 2003；第五春荣等, 2011；任荣等, 2011；胡波等, 2009； Hu et al., 2012 Fig. 9 207Pb/206Pb age histogram of detrital zircons from Late Paleoproterozoic to Neoproterozoic sedimentary rocks in the North China Craton Data after Darby and Gehrels, 2006; Li et al., 2007a, b; Luo et al., 2006; Zhou et al., 2008; Wan et al., 2003, 2011a, b; Gao et al., 2011; Zhu et al., 2011; Diwu et al., 2011；Ren et al., 2011；Hu et al., 2009, 2012 |
北京西山寒武系和侏罗系碎屑锆石U-Pb年龄分布显示1.88~1.8Ga的年龄峰和少量2.1~2.0Ga的年龄。1.88~1.8Ga的碎屑锆石CL图像显示出既具有震荡环带, 又有补丁状和均一的内部结构, 发光较暗, 具较高的Th/U比(0.48~1.33), 分别指示锆石的岩浆和变质成因；2.1~2.0Ga的碎屑锆石都具有震荡环带结构, 指示其岩浆成因。这两组年龄分布特征与华北古元古代末-新元古代沉积盆地碎屑锆石U-Pb年龄分布相似, 后者具有中心为~1.85Ga的主要年龄峰和少量2.3~2.0Ga的岩浆成因的锆石(图 9)。华北克拉通在~2.5Ga克拉通化之后于2.3~2.0Ga经历了一次陆内拉伸-裂谷事件, 在华北北缘、东缘和中部形成丰镇、胶辽和晋豫三个裂谷带, 已有该时期具有伸展性质的基性岩墙、裂谷型火山岩和壳源A型花岗岩的报道(Zhao et al., 2002；Peng et al., 2005；Wilde and Zhao, 2005；杜利林等, 2010; 赵瑞幅等, 2011；于津海等, 2004；孙大中等, 1991；Li and Zhao, 2007; 路孝平等, 2004；Lu et al., 2006; Liu et al., 2005；Sun et al., 1992)。在1.95~1.8Ga这些裂谷带发生碰撞造山, 被称为丰镇、胶辽和晋豫活动带(翟明国, 2004；翟明国和彭澎, 2007；Zhai et al., 2010; Zhai, 2011)。华北克拉通在1.95~1.8Ga发生的大规模变质事件及与变质作用有关的花岗岩和伟晶岩脉的侵入是对碰撞造山作用的指示。华北克拉通太古宙的TTG片麻岩、花岗片麻岩及其中的基性麻粒岩岩墙和透镜体、绿岩带火山-沉积岩以及古元古代早期的沉积岩和花岗质岩石在1.95~1.8Ga曾普遍发生绿片岩相-麻粒岩相不同程度的变质作用(如Liu et al., 1985, 2006; 卢功一和黄静好, 1987；孙大中等, 1991; 郭敬辉等, 1994；毛德宝等, 1999；王凯怡等, 2000；翟明国和卞爱国, 2000; Wang et al., 2003; 郭敬辉和翟明国, 2000; Guan et al., 2002; Zhao et al., 2002, 2008a；Luo et al., 2004; Guo et al., 2005；Peng et al., 2005；Kröner et al., 2005a, b, 2006; Lu et al., 2006; Xia et al., 2006a, b; Wan et al., 2006a, b; 吴昌华等, 2006；赵兰等, 2006；Tang et al., 2007; 刘树文等, 2007；等), 伴随高级变质作用有深熔紫苏辉石花岗岩、含石榴石S型花岗岩和伟晶岩脉的侵入(郭敬辉等, 1999a, b, 2002；王凯怡等, 2001；耿元生等, 2004；Kröner et al., 2006；Zhao et al., 2008a, b)。
4.2.4 古元古代末-新元古代多期裂谷事件北京西山寒武系和侏罗系碎屑锆石U-Pb年龄除记录~186Ma和~233Ma中生代及~256Ma和488~507Ma古生代的年龄外, 前寒武纪的年龄主要分布于1806~630Ma, 产生~1.74Ga、~1.6Ga、~1.38Ga和1.2~1.14Ga的年龄峰及少数~1.56Ga、~912Ma、~814Ma、~740Ma和~630Ma的年龄组(图 7)。此外, 侏罗系窑坡组下伏南大岭组玄武岩中也有~830Ma的继承锆石(赵越等, 2006)。华北克拉通分布于熊耳裂陷槽、燕辽裂陷槽、北缘裂谷和东缘裂谷的古元古代末-新元古代地层中的碎屑锆石U-Pb年龄除具~2.7Ga、~2.5Ga和~1.85Ga的峰值之外, 还分布在1.8~1.0Ga, 集中于~1.6Ga和~1.2Ga(图 9)。古元古代末-新元古代华北克拉通发育与这些裂谷或裂陷槽的裂解作用相对应的岩浆活动, 如1.78Ga的基性岩墙群和熊耳群火山岩(Wang et al., 2004； Hou et al., 2006； Peng et al., 2005, 2006, 2008, 2012；Peng, 2010; 徐勇航等, 2007；赵太平等, 2002, 2004a, 2005, 2007；Cui et al., 2011)、1.75~1.6Ga的非造山岩浆岩和裂谷型火山岩(Rämö et al., 1995；任富根等, 2000；陆松年和李惠民, 1991；陆松年等, 2003；Lu et al., 2002, 2008；赵太平等, 2004b；杨进辉等, 2005；刘振锋等, 2006；任康绪等, 2006； Zhai et al., 2007; Zhang et al., 2007; 高维等, 2008； Zhao and Zhou, 2009；Jiang et al., 2011；Wang et al., 2013；李怀坤等, 1995, 2011； Li et al., 2007a；高林志等, 2008, 2009)、1.56Ga、1.43Ga、1.37Ga和1.32Ga的火山岩或基性岩床(墙)(高林志等, 2007, 2008, 2009; Gao et al., 2007；李怀坤等, 2009, 2010；Zhang et al., 2009b, 2012；Su et al., 2008；苏文博等, 2010)以及900~800Ma基性岩墙群和酸性火山岩(Peng, 2010；Peng et al., 2011a, b; Wang et al., 2011, 2012；柳永清等, 2005; 彭润民等, 2010)。北京西山寒武系和侏罗系1806~ 1281Ma的碎屑锆石除了部分~1.8Ga的锆石具有条带状、补丁状和内部均一的结构外, 大部分是具有震荡环带的岩浆成因的锆石, 发光较暗, Th/U较高, 多数为0.23~1.38。~912Ma和~814Ma的碎屑锆石既有具震荡环带的岩浆成因的锆石, 也有具补丁状结构或内部均一的变质成因的锆石, 前者Th/U较高, 为0.5~1.41, 后者较低, 为0.04~0.47。为1806~800Ma岩浆型碎屑锆石提供物源区的可能是上述的华北克拉通古元古代末-新元古代的岩浆岩。
一些学者假设华北克拉通参与了Columbia超大陆的演化(Zhao et al., 2002；Wilde et al., 2002；Li and Zhao, 2007), 但是对超大陆裂解的响应时间存在争议, 基于对上述古元古代末-新元古代岩浆活动性质的不同理解, 大体有三种认识：古元古代晚期-中元古代早期(~1.78Ga, 赵太平等, 2004a； Peng et al., 2008)、中元古代中期(~1.62Ga, Zhao et al., 2002)和中元古代中晚期(1.35~1.31Ga, Hou et al., 2008；Zhang et al., 2009b)。另外, 900~800Ma的岩浆活动由于峰期时代与Rodinia超大陆裂解的时限可以对应, 彭润民等(2010)提出这一岩浆活动可能记录了相关过程。该时期狼山地区形成了伸展构造体制下的拉张盆地, 并有酸性火山岩的活动及一些与热水喷流成矿作用密切相关的大型-超大型Pb、Zn、Cu矿床形成(Zhai et al., 2004; 彭润民等, 2000, 2010)。尽管在前寒武纪的沉积岩中尚未发现该时期的锆石年龄记录, 但是北京西山地区寒武系和侏罗系中的碎屑锆石以及侏罗系火山岩中的继承锆石却对该时期的岩浆和变质事件信息有很好的保存。古元古代末-新元古代的岩浆活动和碎屑锆石年龄的记录, 指示华北克拉通在古元古代末-新元古代可能经历了一个多期、持续的裂谷事件, 并有一些与大陆裂谷和非造山岩浆有关的成矿记录, 如大庙大型钒钛磁铁矿、白云鄂博超大型稀土矿床和狼山铅锌铜铁硫化物矿床等(翟明国, 2010；Zhai and Santosh, 2013)。
值得指出的是, 北京西山寒武系和侏罗系碎屑锆石还记录了1.2~1.14Ga以及~740Ma和~630Ma的年龄信息。钙质细砂岩样品08QY06中1246~970Ma的锆石大部分是具有震荡环带的岩浆锆石, Th/U含量较高, 为0.44~1.53；少数具均一的内部结构, 或者为具核边结构的锆石, 具均一结构的边部(图 6a), 年龄多集中在1193~1071Ma之间, 其Th/U相对较低, 为0.21~0.43, 可能为变质成因。而长石质岩屑细砂岩样品08QY01中两颗~1.2Ga的锆石, 内部结构分别呈均一状和补丁状, 其Th/U含量与08QY06中变质成因锆石的Th/U接近, 为0.33~0.66, 可能为变质成因。因而, 在寒武系和侏罗系的碎屑锆石中, 1.2~1.14Ga的锆石可能既有岩浆成因、又有变质成因的。华北克拉通目前发现的1.3~1.0Ga的岩石很少, 只有北朝鲜Nangrim地块北部的一个结晶年龄为1195Ma的含角闪石的花岗岩体(Zhao et al., 2006)。1.3~1.0Ga的年龄记录多出现在华北东缘和北缘的沉积岩碎屑锆石中(Luo et al., 2006；Li et al., 2007b; 高林志等, 2010b；Gao et al., 2011；Hu et al., 2012)和侵入岩的捕获锆石中(Yang et al., 2004；张华锋等, 2009)。在华北中部燕辽裂陷槽青白口系的碎屑锆石中也未发现该时期的年龄记录(Wan et al., 2011a; Gao et al., 2011; 第五春荣等, 2011； 任荣等, 2011；Sun et al., 2012)。1.3~1.0Ga的地质事件通常被认为是与Rodinia超大陆聚合有关的格林威尔造山期的事件(Hoffman, 1991; Dalziel, 1991, 1997; Li et al., 1995, 2002, Fitzsimons, 2000; Karlstrom et al., 2001; Condie, 2001; Zhai, 2001；李江海, 1998；李江海和穆剑, 1999；徐备, 2001；陆松年等, 2004；Lu et al., 2008)。在华南克拉通, 大量地质体对该事件过程的记录较为完整, 大量岩浆作用(Li et al., 1995; Li, 1999; 张传恒等, 2007)、俯冲洋壳残块(Li, 1997; Li et al., 1997)以及变质作用(Li et al., 2002)共同见证了华夏与扬子板块的碰撞拼合过程。华北克拉通却因长期缺乏可信的年代学资料, 导致其是否参与过Rodinia超大陆的汇聚及在超大陆的位置等问题仍存疑问(Lu et al., 2008; 陆松年等, 2004)。北京西山寒武系和侏罗系碎屑锆石以及华北北缘及东缘新元古代沉积岩中显著的1.3~1.0Ga年龄峰(图 7、图 9)指示在华北克拉通可能存在该时期的岩石为这些碎屑锆石提供来源, 虽然其位置、规模和性质尚不清楚。这些可能存在的1.3~1.0Ga的岩石是华北克拉通与其他陆块拼合事件的反映还是华北克拉通中-新元古代多期裂谷某些阶段的反映, 尚需进一步研究, 但至少能为讨论华北克拉通在全球超大陆中的位置和演化提供线索。
寒武系钙质细砂岩样品08QY06中~740Ma的碎屑锆石部分具有震荡环带结构和较高的Th/U(0.5~1.41), 指示其岩浆成因；部分具补丁状或均一的内部结构, 并具较低的Th/U(0.04~0.47), 指示其变质成因。~630Ma的锆石CL图像显示它们是具震荡环带结构的岩浆锆石, 具较高的Th/U(0.65~ 1.6)。碎屑锆石记录的这两个时期的岩浆岩或变质岩目前在华北克拉通未见报道, 也未见同时期的地层(相当于南华-震旦系)。而这两期事件在华南克拉通较为发育, ~740Ma被认为是与Rodinia超大陆裂解相关的火山岩和侵入岩活动的时期(Li et al., 2003)；~630Ma的火山岩在南沱组中发育, 并被界定为南华系与震旦系的界限(Chu et al., 2005；Zhang et al., 2005, 2008；高林志等, 2010a及其中的文献), 也是国际地层成冰系(Cryogenian)的顶界(Hoffmann et al., 2004；Condon et al., 2005；Zhang et al., 2005；Chu et al., 2005；Gradstein et al., 2005；陆松年等, 2005)。华北克拉通~740Ma和~630Ma碎屑锆石的发现可为在华北克拉通寻找南华-震旦纪的地层及探讨华北克拉通和华南克拉通的关系提供依据。
5 结论北京西山寒武系徐庄组的钙质细砂岩中碎屑锆石年龄峰值主要集中在~1.38Ga和~1.14Ga。此外, 还有~1.56Ga、~912Ma、~814Ma、~740Ma、~630Ma和~507Ma的年龄组。侏罗系窑坡组长石质岩屑细砂岩和粉砂质泥岩中碎屑锆石年龄峰值主要集中在~2.5Ga、1.88~1.8Ga、~1.74Ga、~1.6Ga和186Ma。此外, 还有~2.77Ga、~2.0Ga、~1.2Ga、~488Ma、~256Ma和~233Ma的年龄组。这些碎屑物质大部分来源于华北克拉通内部或北缘。寒武系和侏罗系中的碎屑锆石年龄记录了华北克拉通前寒武纪重要的地质事件。~2.77Ga、~2.5Ga、2.1~2.0Ga和1.88~1.8Ga的年龄组分别对应华北克拉通早前寒武纪发生地壳生长、克拉通化、裂谷和造山等重要地质事件, ~1.74Ga、~1.6Ga、~1.56Ga、~1.38Ga、~912Ma和~814Ma的年龄组记录了华北克拉通最终克拉通化后开始的古元古代末-新元古代的多期裂谷事件。与1.3~1.0Ga、~740Ma和~630Ma的年龄组相对应的岩石在华北克拉通出现甚少, 而该时期的岩浆岩和变质岩在华南克拉通广泛发育, 且可能与Rodinia超大陆的汇聚和裂解的不同阶段相对应。华北克拉通显生宙碎屑岩中碎屑锆石保存的古元古代末-新元古代地质事件的记录对探讨华北克拉通在元古宙的地质演化及华北克拉通与华南克拉通的关系可提供重要的依据。
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