2018, Vol. 34
华北克拉通是我国面积最大、唯一保存有始太古代3.8Ga岩石的陆块，初始陆核至少在3.8Ga已形成(Liu et al., 1992；John et al., 2008；Wan et al., 2015)。此后，不断有小规模陆壳增长，形成多个小陆块，在新太古代2.7Ga左右出现一次大规模陆壳生长，于~2.5Ga这些太古代微陆块拼合焊接、发生强烈的陆壳改造和增生(Diwu et al., 2011; Zhai and Santosh, 2011; 翟明国, 2011; Zhai, 2014)，形成大量TTG和壳源花岗岩(沈其韩等，2005；耿元生等，2010)，代表一次重要的克拉通化(翟明国, 2011)。然而，华北克拉通并未像世界其它克拉通一样完全稳定，并在古元古代仍有小规模陆壳生长和进一步的陆壳分异(翟明国和彭澎，2007)，于1.85Ga最终形成统一稳定的基底(翟明国, 2010, 2011; Zhai and Santosh, 2011; Zhai, 2014)。显然，无论是早期微陆块的形成与生长，还是新太古代末的微陆块拼合，乃至古元古代末东、西两大陆块最终碰撞拼合，均以华北克拉通西部为一古老太古代陆块为前提条件。然而，华北克拉通基底微陆块的划分的证据主要来自中东部地区出露的各类基底岩石的综合研究，现今大同-离石断裂以西的西部陆块，除北部阴山地块和孔兹岩带出露的基底结晶岩有较多研究和证据外，南部占华北克拉通面积近1/5的鄂尔多斯地块基底由于被巨厚的中元古代以来盖层覆盖，其基底岩石的岩石学和同位素年代学研究一直是一个薄弱环节，缺乏直接的地质证据。尽管近年来在鄂尔多斯盆地部分地区少数钻孔岩芯基底片麻岩中进行了一些年代学和变质作用研究，但其成果和认识还不足以全面反映和代表该地块基底整体特征，因而也难以有效约束整个西部陆块基底性质及其形成演化。本文在前人已有研究资料和成果基础上，通过鄂尔多斯地块基底副片麻岩、花岗质片麻岩以及覆盖于其上的长城系碎屑锆石U-Pb年代学和Hf同位素示踪研究，并结合北部阴山及孔兹岩带研究成果，厘定西部陆块基底岩系的主要地质事件，讨论和约束该陆块基底的形成时代以及经历的重要地质事件及其性质。
1 地质概况Zhao et al.(2001, 2005)、Zhao and Zhai (2013)综合华北克拉通基底构造、岩石组合、岩浆及变质作用和同位素年代学研究成果，识别出一条纵贯该克拉通南北的古元古代末期形成的中部碰撞构造带，并以此将华北克拉通基底划分为东、西两大陆块(图 1)。其中，西部陆块位于中部带西缘大同-离石断裂以西，由北部阴山和南部鄂尔多斯两个地块构成，二者于~1.95Ga沿近东西向延伸的孔兹岩带碰撞拼合形成统一西部陆块。北部的阴山地块由太古代基底和中元古代盖层构成(赵国春，2009)，在固阳-武川、四子王旗和白云鄂博几个隆起区出露，主要由新太古代花岗-绿岩地体和高级变质杂岩地体组成(陈亮，2007；马旭东等，2013)。绿岩地体包括了玄武质枕状熔岩、超基性岩、燧石岩、条带状铁石英岩以及少量碎屑沉积岩，普遍经历了绿片岩相-低角闪岩相变质作用(陈亮，2007)。高级变质杂岩由TTG质片麻岩、闪长质片麻岩以及麻粒岩-紫苏花岗岩、二长花岗岩和角闪花岗岩等构成(简平等，2005；Jian et al., 2012；Chen et al., 2017a)，同时还发育与赞岐岩类似的高MgO、Cr和Ni的闪长岩-石英闪长岩类(简平等, 2005；Ma et al., 2014b)。这些不同成分的正片麻岩原岩时代在2.60~2.55Ga之间，它们经历了高角闪岩相麻粒岩相变质与变形改造，峰期变质为2.50~2.45Ga，主要显示逆时针P-T演化轨迹(金巍等，1991；金巍和李树勋，1996；Zhao et al., 1999)。阴山地块以南为一由孔兹岩系岩石构成的近东西展布的线性构造带，沿集宁-大青山-乌拉山-千里山-贺兰山一线长达近千千米(图 1)(Zhao et al., 2005; Guo et al., 2012; Zhao and Zhai, 2013)，其东部集宁地区出露集宁杂岩，中部乌拉山-大青山地区为乌拉山杂岩，西部的贺兰山和千里山为贺兰杂岩，主要由石墨石榴夕线钾长片麻岩、长英质副片麻岩、石榴石英岩及大理岩和少量斜长角闪岩组成(沈其韩等, 1992; 卢良兆等, 1996)。此外，该带还发育了TTG片麻岩、基性麻粒岩及紫苏花岗岩和晚期侵入的S型花岗岩(赵国春等，2002；Yin et al., 2009, 2011; 翟明国，2009；Peng et al., 2010, 2012; Guo et al., 2012; Wan et al., 2013b; 刘平华等，2013；Liu et al., 2014)，这些岩石普遍经历了1.96~1.85Ga麻粒岩相变质作用(Wan et al., 2006; Santosh et al., 2007a, 2009a, 2013; Yin et al., 2009, 2011; Zhao et al., 2010; Dan et al., 2012; Dong et al., 2013; Jiao et al., 2013a)，形成大量中压泥质麻粒岩，同时还存在高压和超高温麻粒岩(翟明国, 2009; Zhao and Zhai, 2013; Cai et al., 2014；Yin et al., 2014)。高压麻粒岩发现于西部贺兰山-千里山以及东部集宁地区(翟明国, 2009；Yin et al., 2011, 2014; Wu et al., 2016)，超高温麻粒岩多见于中东部大青山及集宁地区(翟明国, 2009；Santosh et al., 2009a, b; Guo et al., 2012; Jiao et al., 2015)，同时存在与变质作用基本同期的S型花岗岩(Peng et al., 2012; Jiao et al., 2013b; Yin et al., 2009, 2011; Wang et al., 2017)。孔兹岩带副变质岩碎屑锆石U-Pb年龄和Hf-O同位素研究，将这套岩石的沉积时代限定在2.0Ga之后，并认为是活动大陆边缘或弧后盆地沉积环境的产物(Wan et al., 2009; Dan et al., 2012)，于1.96~1.83Ga经历麻粒岩相变质作用改造(Wan et al., 2006; Santosh et al., 2007a, 2009a, 2013; Yin et al., 2009, 2011, 2014; Zhao et al., 2010; Dong et al., 2013; Jiao et al., 2013a)。
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图 1 华北克拉通基底构造单元划分图(据Zhao et al., 2012修改) Fig. 1 Tectonic subdivision for the basement in North China Craton (modified after Zhao et al., 2012) |
孔兹岩带以南为鄂尔多斯地块，其东为大同-离石断裂、西为贺兰-六盘山断裂带，南由秦岭造山带所围限(图 1)，内部被巨厚的中新元古代碎屑沉积岩、早古生代浅海碎屑岩和碳酸盐沉积以及晚古生代-新生代陆相碎屑岩覆盖，厚度达6000m。重、磁研究揭示，该地块北部为东西向正磁异常区，指示了强磁性麻粒岩相变质岩分布区，可与北部孔兹岩以及集宁和乌拉山杂岩麻粒岩对比；中南部为北东向正、负相间的磁异常区，正磁异带对应于古老基底变质岩展布带，可与其东部出露的吕梁、五台基底变质岩区相连；负磁异常带向东延伸可与吕梁地区出露的界河口群、野鸡山群、岚河群及黑茶山群以及五台地区的滹沱群等表壳岩分布区相对应(贾进斗等，1997；王涛等，2007；李明等，2012；Gao et al., 2015)。盆内不多的钻遇基底岩芯研究揭示，地块北部基底主要为古元古代晚期麻粒岩相变质的泥质变质岩，与北部孔兹岩带泥质麻粒岩相变质作用基本一致(Wang et al., 2014；Gou et al., 2016)，并存在一些新太古代末-古元古代初和古元古代中晚期花岗片麻岩(Zhang et al., 2015)，东部和中南部基底多为副片麻岩和一些片麻状花岗岩类，锆石同位素年代主要记录了古元古代构造热事件(Hu et al., 2013; Wan et al., 2013a; Wang et al., 2014)，并存在少量新太古代末期岩浆活动的记录(Wan et al., 2013a; Zhang et al., 2015)。
2 西部地块早前寒武纪主要地质事件 2.1 阴山地块地质事件阴山地块不同地区不同程度出露太古宙基底岩石，尤以固阳、武川等地区出露最为完整和具代表性，主要出露了新太古代花岗-绿岩带以及TTG质高级片麻岩和麻粒岩-紫苏花岗岩类，并发育了具特殊构造意义的科马提质玄武岩、高镁安山岩、富Nb火山岩和高镁闪长岩/或赞岐岩(简平等，2005；陈亮，2007；Jian et al., 2012；Ma et al., 2013b, 2014)，它们经历了绿片岩相到麻粒岩相不同变质作用的改造。武川西乌兰不浪地区出露高角闪岩相-麻粒岩变质的超镁铁质岩(角闪石岩)、变质基性火山岩(斜长角闪岩)和变质英安岩(中酸性片麻岩)以及蓝晶石榴二长片麻岩和石榴石英岩及大理岩等(马铭株等，2013；Wang et al., 2015a)。对这些地区的岩石成因、变质作用以及同位素年代学大量研究揭示，在武川西乌兰不浪地区存在阴山地块2.7Ga的最古老花岗质片麻岩，并经历了~2.5Ga构造-热事件的改造(董晓杰等，2012；马铭株等，2013)。该区片麻状花岗岩和蓝晶石榴二长片麻岩获得2.58Ga的原岩结晶年龄，蓝晶石榴二长片麻岩和角闪岩的变质年龄为2.50~2.48Ga；一些2.71~2.58Ga碎屑岩浆锆石也经历了~2.5Ga的变质改造(Wang et al., 2015a)，也指示形成于2.7~2.58Ga的岩体多已经历了~2.5Ga变质作用改造。此外，在武川东北部小南沟-明星沟地区和固阳地区发育2.58~2.54Ga的TTG(张永清等，2006)，固阳地区存在2.53~2.51Ga的高镁安山岩和安山岩、2.52Ga的玄武岩-英安岩和2.52Ga的花岗岩及2.52~2.47Ga的高镁闪长岩等岩浆活动(Jian et al., 2012)。该区基性麻粒岩、石榴片麻岩、紫苏花岗岩及角闪片麻岩、角闪岩以及变质辉长岩的原岩年龄变化于2.54~2.51Ga之间(Ma et al., 2013a, 2014a; Zhang et al., 2014)，表明2.54~2.51Ga期间出现了多种类型的岩浆活动。另外，在一些花岗岩中发现2.6Ga的残余陆壳及2.6~3.9Ga的锆石捕掳晶(Ma et al., 2013b)，高镁闪长岩中也发现2.6Ga的继承锆石(Jian et al., 2012)，反映存在更为古老的陆壳物质。此外，基性麻粒岩、石榴片麻岩和角闪岩获得了2.52~2.45Ga的变质年龄(简平等，2005；Jian et al., 2012; Ma et al., 2013a, 2014a)，说明岩体形成之后很快发生了变质作用的改造。综合固阳-武川地区各类岩石年代学研究，阴山地块太古宙基底最早的岩浆活动(TTG)在~2.7Ga已出现，无论是绿岩带，花岗岩类侵入体，还是高级别变质杂岩的原岩形成年龄均集中在新太古代末的2.56~2.51Ga期间，岩浆活动包括辉长岩、TTG、闪长岩、赞岐岩和钾长花岗岩等岩浆侵入以及玄武岩、安山岩和高镁安山岩等火山喷发。对目前已获得的岩浆及变质年龄统计可以看出，该区各类岩浆活动主要发生在2.7~2.45Ga之间，在2.54Ga和~2.45Ga期间又经历了变质作用的改造，大致表现了2.53~2.51Ga和2.50~2.47Ga两个阶段(图 2)。马旭东等(2013)总结了该区变质作用，认为早期(~2.5Ga)的变质作用具逆时针的P-T演化轨迹，与大洋中脊俯冲消减有关；晚期(2.48Ga)变质作用呈现了顺时针P-T演化轨迹，反映了碰撞造山演化过程。最近，在内蒙四子王旗地区发现的2.52~2.49Ga的TTG与大洋俯冲岛弧环境相关，晚期2.47~2.44Ga钾长花岗岩为与碰撞后伸展环境的产物(Chen et al., 2017a, b)，也揭示阴山地块在~2.5Ga发生大洋俯冲碰撞造山，之后发生碰撞造山并于2.47~2.44Ga转为伸展构造环境。
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图 2 阴山地块岩浆及变质事件年龄直方图 数据陶继雄和胡凤翔, 2002; 张玉清和刘俊杰, 2004; 简平等, 2005; 张永清等, 2006; 陈亮, 2007; 董晓杰, 2009; 任云伟, 2010; 徐仲元等, 2011; Dong et al., 2012; Jian et al., 2012; 董晓杰等，2012; 刘利等, 2012；Ma et al., 2013a, b, 2016;马铭株等, 2013；马旭东等, 2013；Zhang et al., 2014; 王丹等, 2014; Wang et al., 2015a; Chen et al., 2017a Fig. 2 U-Pb age histogram of the magmatic and metamorphic zircons from the Yinsh Block |
孔兹岩带岩石以副变质中压泥质麻粒岩为主(翟明国, 2009; Zhao and Zhai, 2013; Cai et al., 2014)，同时还发育高压与超高温变质麻粒岩(Santosh et al., 2007b; 翟明国, 2009; Liu et al., 2012a; Guo et al., 2012; Jiao et al., 2013a, b, 2015; Gou et al., 2014; Yin et al., 2014)。由副变质岩类获得的碎屑锆石U-Pb年龄主要集中于2.2~2.0Ga之间，还有一些2.5~2.25Ga的锆石以及少量新太古代(2.9~2.5Ga)年龄的锆石(图 3a)，同时存在~1.95Ga和~1.86Ga两变质峰期年龄(Zhao et al., 2005; Wan et al., 2006, 2009; Yin et al., 2011; Dan et al., 2012；蔡佳等，2015)，限定它们的沉积时代为2.0~1.95Ga。1.95~1.85Ga的变质事件在孔兹岩带泥质和基性变质岩中均有很好记录，东部集宁、怀安地区的中、高压泥质变质岩获得1.95~1.92Ga和1.90~1.84Ga的变质年龄(Wan et al., 2006; Zhao et al., 2010; Jiao et al., 2013a)，变质辉长苏长岩和变质辉长岩也获得1.91Ga (Peng et al., 2014)和1.86Ga (Peng et al., 2010)的变质年龄，紫苏花岗岩存在~1.96Ga和1.86~1.81Ga的变质年龄(Santosh et al., 2013)，集宁土贵乌拉超高温泥质麻粒岩的变质年龄为1.93~1.91Ga (Santosh et al., 2007a, 2009a, 2013)。中部大青山地区的古元古代表壳岩中也记录了~1.96Ga和1.88~1.83Ga变质事件(Dong et al., 2013)。伴随这两期变质事件，在东部集宁地区出现1.95Ga淡色花岗岩(Wang et al., 2017)和1.92~1.89Ga的S型花岗岩浆侵入(Jiao et al., 2013b)；在中部大青山地区也存在1.95Ga的正长花岗岩和紫苏闪长岩的岩浆活动(Ma et al., 2012)。与中东部地区相同，西部的贺兰山和千里山地区的泥质麻粒岩中也存在1.96~1.92和1.87Ga两组变质和1.90Ga和1.88~1.86Ga的S型花岗岩侵入事件(Yin et al., 2009, 2011；Zhang et al., 2017)。此外，在大青山地区一些古元古代(下乌拉山群和桑干群等)花岗质片麻岩及基性麻粒岩包体中发现了2.5~2.45Ga的花岗岩和2.46~2.44Ga辉长岩及1.97~1.92Ga闪长岩浆活动，它们均经历了2.5Ga、2.45Ga和1.95~1.90Ga及1.85Ga多期变质作用的改造(图 3b)(Wan et al., 2009, 2013b; 刘平华等，2013; Liu et al., 2014, 2017)。因此，孔兹岩带各类岩石的锆石U-Pb年代学研究证明，该带的孔兹岩系岩石是2.0Ga后沉积的产物，之后经历了1.95~1.92Ga和1.89~1.85Ga麻粒岩相改造，同时伴随有1.95~1.85Ga的S型花岗岩浆活动(Yin et al., 2009, 2011; Peng et al., 2012; Jiao et al., 2013b; Wang et al., 2017)。此外，该带还存在记录有2.5~2.4Ga岩浆活动的古元古代早期片麻岩，它们又被1.97~1.92Ga岩浆侵入，并经历了~2.5Ga、2.45Ga以及1.97~1.94Ga和1.87~1.82Ga多期变质作用的改造(图 3)，指示孔兹岩带很可能是一个卷入了不同岩块、并经历了多期构造-岩浆事件改造的复杂构造带。
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图 3 孔兹岩带碎屑(a)及岩浆和变质锆石(b)年龄直方图 数据引自Wan et al., 2006, 2009, 2013b, 2016；Xia et al., 2006a, b；Dong et al., 2007, 2013, 2014；Santosh et al., 2009a, 2013；Yin et al., 2009, 2011；周喜文和耿元生，2009；Peng et al., 2010, 2014；Zhao et al., 2010；Dan et al., 2012；Ma et al., 2012；Jiao et al., 2013b；Liu et al., 2013, 2014, 2017；Gong et al., 2014；钟长汀等，2014；Yang et al., 2015；蔡佳等，2015；徐仲元等，2015；Huang et al., 2016；Wang et al., 2017；Zhang et al., 2017 Fig. 3 U-Pb age histogram of the detrital zircons (a) and magmatic, metamorphic zircons (b) from the Khondalite Belt |
孔兹岩带以南的鄂尔多斯盆地被巨厚的中、新元古代及古生代-中新生代沉积盖层覆盖，盆内无任何基底岩石出露，航磁异常以强宽缓磁异常明显不同于周缘弱磁异常区(Gao et al., 2015)，显示了整体刚性块体特征，被认为是一个具统一基底的太古代稳定陆块(张抗，1989；贾进斗等，1997；邓军等，2005)，并与华北其它地区几个小地块共同构成了华北克拉通七个太古宙小陆块(Zhai and Santosh, 2011; 翟明国, 2012, 2011; Zhai, 2014)，也成为西部陆块重要组成部分(Zhao and Zhai, 2013及其引用文献)。新的航磁异常研究揭示，鄂尔多斯地块并非一具有完整古老基底的地块，可能存在北部伊盟和中部延安-佳县-临县两个古陆核(Wang et al., 2015b)。尽管如此，由于该地块长期缺乏来自基底岩石的直接地质研究，其基底组成、结构和形成时代以及是否具有完整的基底一直缺乏确凿的地质证据予以证明。近年来，在该盆地中不多的钻孔中获得了一些基底岩芯，初步揭示其基底主要由富铝副片麻岩、变粒岩、片岩和大理岩及花岗片麻岩等组成(Hu et al., 2013; Wan et al., 2013; Zhang et al., 2015)，经历了角闪岩到麻粒岩相变质作用(Wang et al., 2014; Gou et al., 2016; He et al., 2016)。其中，地块西北部基底变质岩主要为含堇青石石榴夕线黑云二长片麻岩、石榴夕线堇青石黑云二长片麻岩(Wang et al., 2014; Gou et al., 2016)，东北部以发育黑云钾长片麻岩、条带状二云母钾长花岗岩和混合片麻岩及片麻状花岗岩为主(Hu et al., 2013; Wan et al., 2013; Zhang et al., 2015)，中东部主要由夕线斜长片麻岩、含石墨二云母二长片麻岩、二云母斜长片麻岩以及片麻状黑云母花岗岩构成(Hu et al., 2013; Wan et al., 2013a；Zhang et al., 2015；吴素娟等，2015)，中部地区则主要出现云母石英长石片麻岩和花岗片麻岩类(Wan et al., 2013a; Zhang et al., 2015)。显然，目前的研究表明，这些基底岩芯主要以副片麻岩类为主，Wan et al.(2013a)和Hu et al.(2013)由这些副片麻岩获得古元古代早期2.5~2.2Ga和古元古代晚期2.1~1.85Ga两组锆石U-Pb年龄和少量新太古代岩浆锆石年龄，一些核边结构的锆石具有2.08Ga的核和~1.9Ga变质增生边。此外，不多的片麻状花岗岩获得2.04Ga的形成年龄，在夕线石榴片麻岩中也发现了2.03Ga的岩浆锆石年龄，并存在1.85~1.63Ga变质年龄的锆石增生边(Hu et al., 2013)。Zhang et al.(2015)在北部、中东部和中部几口井的基底岩芯中也发现了2.2~2.0Ga的岩浆活动，并记录了1.85Ga的变质改造年龄，同时还识别出~2.5Ga的岩浆活动。吴素娟等(2015)将中东部龙探1井(图 1)二云母斜长片麻岩碎屑锆石以及前人在棋探1井中得到的碎屑锆石统计后，获得2.05~1.90Ga的继承岩浆锆石年龄以及1.83Ga和1.78Ga两组变质年龄。我们对棋探1井基底岩芯夕线石榴黑云片麻岩的碎屑锆石U-Pb定年分析，同样获得2.17 ~1.90Ga(峰值为~2.0Ga)岩浆锆石年龄，少量Th/U＜0.1的锆石出现＜1.90Ga的变质年龄，是后期变质作用改造的结果。由于变质锆石一般具有低的Th和U含量以及很低的Th/U比值(＜0.1)(Wu and Zheng, 2004)，基于此将钻孔基底岩芯已获得所有副片麻岩锆石中那些低Th和U含量和Th/U＜0.1的锆石剔除，供获得339个继承岩浆锆石，得到的年龄频率直方图同样显示了2.2~2.0Ga的主要年龄组(峰期为2.03Ga)，并存在~2.5Ga的锆石年龄(图 4a)，揭示了鄂尔多斯盆地块基底曾在新太古代末的~2.5Ga和古元古代晚期~2.1Ga发生了两期重要的构造-岩浆活动。此外，对盆地中北部和南部上覆于基底之上的首套盖层长城系3件砂岩碎屑锆石U-Pb定年分析，同样存在~2.5Ga和2.2Ga两个主峰年龄和1.96Ga和1.85Ga的峰期年龄(图 4b)，类似的峰值在中生代盖层砂岩和现代河流沙碎屑锆石U-Pb年龄中也十分明显(图 4c, d)。此外，这些盖层沉积碎屑岩中还有新元古代2.9~2.6Ga(峰值2.7Ga)的锆石以及少量中太古代的锆石，揭示该地块基底存在新太古代岩浆事件。因此，它们与基底各类变质岩获得的年龄结果一致，充分证明鄂尔多斯地块基底在~2.7Ga曾发生了一次构造-岩浆活动，此后分别于~2.5Ga和2.2~2.0Ga又发生了的两期重要的构造-岩浆活动。那些~1.9Ga和~1.85Ga峰期的锆石均显示了低的Th/U比值和变质锆石的结构特征，代表了经历古元古代晚期变质作用改造的结果。一些钻井岩芯的泥质变质岩变质作用研究表明，这些基底副片麻岩均经历了中压麻粒岩相变质作用(Wang et al., 2014; Gou et al., 2016; He et al., 2016)，在泥质麻粒岩中很多锆石出现了变质年龄为1.96Ga左右的增生边(Wan et al., 2013a; Wang et al., 2014)，在该泥质麻粒岩中独居石也获得1.94~1.93Ga的变质年龄(He et al., 2016)，并在独居石的核部和边部分别获得1.96~1.94Ga和1.90~1.88Ga两期变质年龄(Gou et al., 2016)，揭示了两期变质作用改造的结果。综合鄂尔多斯地块基底及盖层和现代河流沙碎屑锆石年龄统计结果，呈现了与西部陆块十分一致的年龄谱(Wan et al., 2011a)，明显出现~2.5Ga及~1.85Ga两个峰值和2.2~2.0Ga的次级峰值，同时出现少量太古代锆石年龄(图 4)，暗示它们很可能来自于西部陆块基底岩石或临近的相关地块。结合该地块基底片麻岩以及花岗质片麻岩存在~2.5Ga和2.2~2.0Ga的岩浆活动，它们的锆石Hf同位素陆壳模式年龄出现~2.7Ga的峰值，且εHf(2.7Ga)均为正值(Zhang et al., 2015)，还出现一些太古代捕获或继承锆石(Wan et al., 2013a; Zhang et al., 2015)。因此推断，该地块很可能在新太古代前已有一定陆壳物质形成，此后在~2.7Ga、~2.5Ga和2.2~2.0Ga出现了三期构造-岩浆活动，并在古元古代末期经历了~1.95Ga和~1.85Ga两期变质作用的改造(图 4)。
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图 4 鄂尔多斯地块基底、盖层及现代河流沙碎屑锆石年龄直方图 数据引自Diwu et al., 2012；Hu et al., 2013；Wan et al., 2013a；Xie and Heller, 2013；Bao et al., 2014；吴素娟等，2015；作者未刊资料 Fig. 4 Age histogram of the detrital zircons from the basement, cover sandstons and moden river sands in the Ordos Block |
综合阴山和鄂尔多斯地块及其二者之间的孔兹岩带早前寒武纪各类岩石中获得的岩浆和变质年龄分析，不难看出，它们共同揭示西部陆块经历了新太古代-古元古代早期和古元古代中晚期岩浆以及变质事件(图 5)。其中，北部阴山地块的岩浆活动明显早于南部的孔兹岩带和鄂尔多斯地块，该地块自~2.7Ga就已有岩浆活动的发生，并在2.58~2.53Ga出现大量各类岩浆活动，且一直持续到2.45Ga，在2.5~2.45Ga期间还受到变质作用的改造。然而，该地块与南部孔兹岩带和鄂尔多斯地块基底明显不同的是缺失古元古代晚期岩浆和变质作用活动的记录(图 5a)。与北部阴山地块不同，其南部的孔兹岩带存在古元古代初期以及古元古代晚期岩浆活动的记录，同时与两期岩浆活动相伴还有基本同期变质作用的出现(图 5b)。但明显不同的是，南部鄂尔多斯地块基底目前虽已确定存在少量~2.5Ga的岩浆活动，至今还未发现同期变质作用，但该地块中2.2~2.0Ga的岩浆活动十分强烈(图 5c)，而北部阴山地块和孔兹岩带均缺失该期岩浆活动(图 5a, b)。然而，古元古代晚期1.95~1.85Ga的变质作用在孔兹岩带和鄂尔多斯地块基底北部及东部均有记录(图 5b，c)。总体上，作为华北克拉通西部陆块三个重要组成部分，它们一同揭示西部陆块曾在新元古代中期(~2.7Ga)、新太古代末-早古元古代早期(2.58~2.45Ga)以及古元古代中晚期(~2.04Ga)和末期(1.95~1.85Ga)发生了多期岩浆活动，同时于新太古代末-古元古代初期(2.6~2.45Ga)以及古元古代晚期~1.95Ga和~1.85Ga发生多期变质作用。另一方面，无论是阴山地块还是鄂尔多斯地块基底岩石、甚至是鄂尔多斯地块盖层及河流沙，它们的锆石εHf(2.7Ga)均为正值，锆石Hf陆壳模式年龄(tDMC)主要介于2.9~2.6Ga(峰期~2.75Ga)(图 6a, b, e-h)，表明在~2.75Ga发生了一次重要的陆壳生长。由此推断，构成西部陆块的北部阴山和南部鄂尔多斯地块可能至少在~2.7Ga的新太古代已有部分陆壳形成，并在~2.75Ga出现一次重要的陆壳生长，此后分别于2.6~2.45Ga和~2.2Ga发生了重要的构造岩浆活动，并在古元古代晚期经历了~1.95Ga和~1.85Ga两期变质作用的改造和伴有同期花岗岩浆的侵入。
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图 5 阴山、鄂尔多斯地块及孔兹岩带岩浆及变质锆石年龄对比直方图 数据陶继雄和胡凤翔，2002；张玉清和刘俊杰，2004；简平等，2005；Wan et al., 2006, 2009, 2013a, b; 吴昌华等，2006；张永清等，2006；Dong et al., 2007, 2013, 2014；陈亮，2007；Santosh et al., 2007a, 2009a, 2013；Yin et al., 2009, 2011；Zhou and Geng, 2009；董晓杰，2009; Peng et al., 2010, 2014；Zhao et al., 2010；任云伟，2010；Xu et al., 2011；Dan et al., 2012；Ma et al., 2012, 2013a, 2014b, 2016；Jian et al., 2012；Jiao et al., 2013a；董晓杰等，2012；刘利等，2012；Dong et al., 2013；Hu et al., 2013；胡建民等，2013；刘建华等，2013；马旭东等，2013；马铭株等，2013；Gong et al., 2014；Liu et al., 2014, 2017；Wang et al., 2014, 2015a, 2017；Zhang et al., 2014, 2015, 2017；王丹等，2014；钟长汀等，2014; Yang et al., 2015; 蔡佳等，2015；吴素娟等，2015；徐仲元等，2015；Gou et al., 2016；He et al., 2016；Huang et al., 2016；Chen et al., 2017a Fig. 5 Comparison age histograms of the magmatic and metamorphic zircons from the Yinsh Block, Ordos Block and Khondalite Belt |
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图 6 阴山、鄂尔多斯地块和孔兹岩带及鄂尔多斯地块盖层和现代河流沙岩浆锆石Hf同位素组成 数据引自Xia et al., 2006a, b, 2008; Yin et al., 2011; Dan et al., 2012; Diwu et al., 2012; Wan et al., 2013a; 马铭株等，2013; Bao et al., 2014; Zhang et al., 2014 2015, 2017; Yang et al., 2015; Chen et al., 2017a; He et al., 2017; Liu et al., 2017作者未刊数据 Fig. 6 Hf isotopic composition of the magmatic zircon from the Yinsh Block, Khondalite Belt and the basement, cover sandstones and modern river sands in the Ordos Block |
华北克拉通西部陆块中目前发现的最古老岩石为阴山地块武川西乌兰不浪地区2.7Ga奥长花岗岩(董晓杰等，2012；马铭株等，2013)，该岩体的锆石εHf(t)=1.52~6.59，tDM=2.43~2.77Ga，tDMC=2.50~2.93Ga，指示该区新太古代2.7Ga一次新生地壳生长。此外，在阴山地块一些花岗岩及高镁闪长岩中还发现2.6~3.9Ga的锆石捕掳晶(Jian et al., 2012; Ma et al., 2013b)，暗示这期新生地壳生长可能在相当范围都有发生，这也从阴山地块2.58~2.45Ga的TTG、花岗质片麻岩及变基性火山岩的锆石εHf(t)＞0，模式年龄变化于2.9~2.8Ga(图 6a, b)，指示来自该新生陆壳再造得到证明。与阴山地块相比，尽管南部鄂尔多斯地块基底未发现2.7Ga的岩石，但在钻孔岩芯~2.1Ga花岗岩中发现了2.67Ga的继承岩浆锆石(Zhang et al., 2015)，同时在其基底上覆盖层长城系及中生界砂岩和现代河流砂中也存在2.95~2.6Ga的碎屑岩浆锆石(图 6e-h)，揭示了鄂尔多斯地块基底曾存在~2.7Ga的岩浆事件。特别是，在鄂尔多斯地块南部钻井长城系碎屑岩中还发现了3.7~3.3Ga的岩浆锆石(图 6c)，其tDM=3.98Ga，tDMC=4.01Ga，与地块南缘古生代火山岩中4.1Ga的捕获锆石年龄基本一致(王洪亮等，2007；第五春荣等，2010)，暗示鄂尔多斯地块很可能存在冥古宙陆壳物质，并成为周缘地区冥古代锆石的源区。这些锆石Hf-O同位素特征反映了4.0Ga就已开始了壳幔分异岩浆活动，此后3.7~3.8Ga的岩浆锆石则是陆壳再造的记录，进一步证明始太古代陆壳物质存在的可能(Diwu et al., 2013)。事实上，华北克拉通3.8Ga的岩石在东部鞍山地区保留的十分有限，此后在新太古代之前也仅有少量新生陆壳生长，大量的新生陆壳生长主要发生在2.9~2.65Ga期间(峰期~2.7Ga)(Wan et al., 2015)，在山东的东、西部(Jahn et al., 1988, 2008；Wan et al., 2011b)，在河南鲁山(Kröner et al., 1988; Sun et al., 1994; Liu et al., 2008；Zhou et al., 2014)以及中部阜平、恒山、中条和赞皇以及陕西华阴等广大地区都存在2.9~2.7Ga的TTG和花岗质片麻岩(Guan et al., 2002；Kröner et al., 2005a, b；Huang et al., 2010；Yang et al., 2013；Zhu et al., 2013；路增龙等，2014；Jia et al., 2016)，代表了华北克拉通一期重要的新生陆壳生长。与东部陆块相比，尽管西部陆块目前仅在阴山地块确定存在2.7Ga的岩石，但在鄂尔多斯地块基底花岗岩类和盖层沉积岩及现代河流砂碎屑锆石中不但存在新太古代、甚至中太古代古老岩浆锆石，同时它们的锆石εHf(t)为正值，Hf陆壳模式年龄(tDMC)集中于2.9~2.65Ga之间(峰值~2.75Ga)(图 6e-h)。此外，阴山地块、孔兹岩带以及鄂尔多斯地块中基底~2.5Ga的各类岩石的锆石εHf(t)＞0，tDMC=2.9~2.7Ga(峰期为~2.7Ga)(图 6a-d)，均证明在2.9~2.7Ga期间可能在更大范围发生有幔源岩浆活动引起的新生地壳形成，同时还包含少量古老地壳物质再造。西部陆块2.8~2.7Ga岩石分布面积较少很可能是由于后期2.5Ga的强烈构造-热事件改造和破坏的结果，当然也不能排除因工作程度不够，在钻遇基底的有限岩芯样品中未能获得这些古老岩石的可能。
3.2 新太古代末-古元古代初(2.58~2.45Ga)地质事件相比于2.7 Ga的岩浆活动，西部陆块在新太古代末-古元古代初期的2.58~2.45Ga期间发生了更为广泛而强烈的岩浆活动，并在北部阴山地块、南部鄂尔多斯地块及二者之间的孔兹岩带古元古代基底各类正片麻岩中均有记录(图 5)。北部阴山地块在2.56~2.45Ga期间出现了多种岩浆活动，其中TTG片麻岩形成于2.53~2.50Ga，这些岩石的锆石εHf(t)=+0.3~+5.5，tDMC=3.18~2.75Ga，少量锆石的εHf(t)=-7.8~-2.1，tDMC=3.89~3.40Ga，表明主要源自新太古代新生陆壳物质和少量古老陆壳物质的源区，它们为陆缘消减板块回撤引起新生陆壳熔融(Chen et al., 2017a, b)或地幔减压熔融岩浆与新生下地壳熔体混合的产物(Jian et al., 2012; 马旭东等，2013)。与此同时，在2.56~2.51Ga期间出现大量与大洋俯冲消减环境有关的玄武岩、安山岩、高镁安山岩及英安岩类(陈亮，2007; Jian et al., 2012; 刘利等，2012；马旭东等，2013)，同期的橄榄石-斜方辉石角闪石岩、斜长角闪岩及基性麻粒岩的钕同位素模式年龄tDM=2.88~2.61Ga，锆石εHf(t)=+1.8~+3.0，tDM1=2.81~2.68Ga，形成于~2.58Ga的变辉长岩、角闪石岩亏损Nb、Zr和Ti，辉长岩εNd(t)=+1.77~+2.23，角闪石岩εNd(t)=+1.48~+3.53，锆石εHf(t)=+7.3，均指示与大洋消减俯冲带岩浆活动密切相关(Ma et al., 2014a, 2016; Wang et al., 2015a)。此外，还出现与大洋俯冲消减板块熔体与上覆地幔楔相互作用形成的赞岐岩(Jian et al., 2012)，它们的εNd(t)和εHf(t)均为正值，全岩钕模式年龄tDM=2.65~2.48，锆石Hf模式年龄tDM=2.8~2.6Ga(峰期为~2.7Ga)，指示是新生陆壳熔体与地幔相互作用的产物(Ma et al., 2013a)，这类岩石大多是汇聚板缘消减大洋板片及沉积物部分熔融的熔体与地幔橄榄岩混合作用的结果(Shimoda et al., 1998; Kamei et al., 2004)。此外，在2.54~2.52Ga期间还有紫苏花岗岩形成，并经历近同期(2.52~2.50Ga)变质作用改造，它们以准铝-过铝质，高MgO、Ni、Cr和Mg#，高Sr和Ba、低K2O/Na2O为特征，也指示是地幔镁铁质岩浆与下地壳部分熔融长英质岩浆混合的结果，近同时麻粒岩相变质与大洋中脊俯冲消减岩浆活动密切相关(Ma et al., 2013b)。因此，阴山地块新太古代晚期2.56~2.50Ga期间发生的各类岩浆作用(Jian et al., 2012)，包括2.53~2.50Ga的TTG、2.53~2.51Ga的各类火山岩和赞岐岩以及2.54~2.52Ga期间形成的高级变质杂岩和紫苏花岗岩类，均是汇聚板缘与大洋俯冲消减相关环境的产物。这些岩浆岩的锆石εHf(t)以正值为主，tDMC=2.9~2.6Ga(峰期为~2.75Ga)，部分锆石的εHf(t)接近同期亏损地幔值，证明阴山地块在新太古代末主要发生了与陆缘板块消减有关的陆壳再造，同时还伴有幔源岩浆新生陆壳的形成，少数岩浆锆石的εHf(t)明显偏负，tDMC＞2.9Ga(图 6a)，暗示也有少量古老陆壳物质的参与。~2.5Ga以来阴山地块仍持续有岩浆活动发生，在2.51~2.47Ga发生地壳深熔(张玉清等，2003；董晓杰等，2012)，并在2.47~2.44Ga期间形成了不同于早期岩浆产物的亚碱性-碱性钾长花岗岩类(Chen et al., 2017a)，它们由软流圈地幔上涌导致早期TTG熔融所形成，代表了陆壳伸展，指示~2.4Ga以来构造体制开始由挤压向伸展转换(Chen et al., 2017b)。
与北部阴山地区相比，孔兹岩带中一些古老正片麻岩中记录的岩浆活动主要发生于古元古代早期的2.50~2.37Ga期间(Wan et al., 2009, 2013b; 刘平华等，2013; Liu et al., 2014, 2017)，并在2.50~2.45Ga期间形成大量花岗质片麻岩及紫苏花岗岩(刘建辉等，2013；张琳等，2016；Liu et al., 2017)，它们以准铝质至弱过铝镁质高钾钙-碱性系列，具轻重稀土中到高度分馏、弱或无铕异常的稀土模式，微量元素富集大离子亲石元素，亏损Nb，Ta及Ti等元素为特征，与由大陆地壳物质部分熔融岩浆产物地球化学特征一致。这些岩石的锆石εHf(t)多为正值，对应的二阶段Hf模式年龄介于2.9~2.55Ga之间(峰值为~2.67Ga)(图 6c, d)，其中花岗岩类锆石εHf(t)=-0.7~+9.75(平均+4.81)，tDMC=2.9~2.4Ga(平均2.64Ga)，紫苏花岗岩锆石εHf(t)=-1.27~+6.85(平均+3.83)，tDMC=2.9~2.6Ga(平均2.7Ga)(Liu et al., 2017)；同期的石榴黑云片麻岩的εHf(2.51Ga)=+0.55~+5.83，tDM=2.80~2.60Ga，石榴黑云花岗岩的εHf(2.50Ga)=+0.27~+5.73，tDM=2.83~2.60Ga (Wan et al., 2009)，~2.5Ga变火山岩锆石εHf(t)=+1.2~+7.0，tDMC=2.84~2.56Ga(Ma et al., 2012)，一致证明它们主要为新生陆壳再造的岩浆产物。此外，在2.44~2.42Ga期间形成了埃达克质石英闪长岩、高镁闪长岩(赞岐岩)以及具Closepet花岗岩特征的角闪二长花岗岩，它们高MgO和Cr、Ni(钟长汀等，2014)，与由壳、幔岩浆混合形成的富MgO、高Cr、Ni的花岗岩类类似(Kamei et al., 2004；Shimoda et al., 1998)，代表了新生陆壳的形成(Moyen et al., 2001)。在2.55~2.5Ga和2.45~2.37Ga还伴有基性岩浆活动的发生(Wan et al., 2009)，这不仅证明了新生地壳形成，同时也标志着构造体制转为伸展环境(Wan et al., 2013b)。另一方面，这些岩石还不同程度经历了近同期(2.50~2.45Ga)变质作用的改造(Wan et al., 2009, 2013b; 刘建辉等，2013；Liu et al., 2017)，这种壳幔岩浆活动与麻粒岩相变质同时出现被认为是地幔柱岩浆活动的结果(Jayananda et al., 1995)。因此，孔兹岩带中古老花岗质片麻岩记录的2.5Ga以来发生的各类岩浆活动，代表了~2.5Ga以来，构造体质由汇聚碰撞转为陆壳伸展，同时出现大量陆壳再造和壳幔岩浆混合作用形成的各类岩浆岩类，并伴有同期变质作用的改造，可能与地幔柱相关的岩浆活动密切相关。
与北部阴山地块和孔兹岩带新太古代末和古元古代初出现大量岩浆活动不同，在鄂尔多斯地块基底中，目前仅在有限的钻井岩芯中发现了少量~2.5Ga的花岗质片麻岩(Zhang et al., 2015)，它们高硅(SiO2=69.09%~73.55%)、富钾(K2O/Na2O=2.04~4.56)，A/CNK=1.10~1.18，属过铝质钾玄岩系列，具轻重稀土较强分馏的中等Eu负异常的右倾稀土模式，微量元素富集Rb，Ba，Th，K等大离子亲石元素、亏损Nb，Ta，P及Ti等，与陆壳物质部分熔融形成的花岗岩类地球化学特征十分一致。这些岩石的锆石εHf(t)=-3.32~+5.02，tDMC=3.06~2.79Ga(图 6e，f)，指示岩浆主要源自新太古代的新生陆壳，同时有部分中太古代陆壳物质的参与，与北部阴山地块和孔兹岩带~2.5Ga的花岗岩类一样，证明鄂尔多斯地块在新太古代末~2.5Ga也发生了以新生陆壳再造为主的构造岩浆事件。综合西部阴山陆块、孔兹岩带以及鄂尔多斯地块新太古代末期-古元古代早期的各类岩浆作用，西部陆块在~2.5Ga之前的岩浆作用主要形成与汇聚有关的大洋俯冲消减环境，形成了陆缘弧岩浆活动的TTG、基性及中酸性火山岩和高镁安山岩及赞岐岩类以及其它类型的侵入岩类，它们均经历了2.52~2.50Ga变质作用改造，代表一次区域汇聚拼合过程。此后，于古元古代初2.5~2.37Ga期间出现高钾的钾长花岗岩类和壳幔混合作用形成的高Mg、Cr和Ni花岗岩类以及同期基性岩浆活动和变质作用，指示自2.5Ga以来构造体制开始了由挤压向伸展转化，可能代表了地幔柱岩浆活动的结果。事实上，新太古代末2.55~2.45Ga期间发生在西部陆块的的岩浆活动，在华北克拉通东部的广大地区也广为出现(Zhai, 2010, 2014；耿元生等，2010；翟明国, 2011; Wan et al., 2015)，形成TTG和二长花岗岩、花岗闪长岩及钾长花岗岩等壳源花岗岩类，并表现为2.55~2.53Ga、2.51~2.50Ga和2.50~2.45Ga三个期次(翟明国, 2011; Wan et al., 2012)。这些花岗岩锆石有变化较大的εHf(t)负和正值，锆石的tDMC多高于或近于其形成年龄，为陆壳物质再造岩浆活动的产物(Geng et al., 2012; Wan et al., 2015)。然而，一些TTG片麻岩和闪长岩锆石有高和正的εHf(t)值，Hf模式年龄与岩体形成年龄相近(刘富等，2009；Diwu et al., 2011)，说明还有新生地壳形成，这也得到同期基性岩浆活动的证明(Li et al., 2011; 彭澎，2016)。此外，与2.52~2.50Ga超镁铁质岩墙-碱性正长岩脉侵入活动基本同时(Li et al., 2011)，华北克拉通基底相当范围发生了逆时针P-T演化轨迹的中压麻粒岩相变质作用(耿元生等，2016)，表明该变质作用很可能是来自地幔的基性岩浆底侵于下地壳底部，带来大量的热导致了中、下地壳物质部分熔融形成花岗质岩浆作用的同时，还引起中、下地壳岩石的变质改造，其机制与地幔柱底侵的构造热体制密切相关(耿元生等，2010)。另一方面，超镁铁质-碱性岩脉的出现，指示太古宙末期华北克拉通岩石圈已有较大的厚度和较高的稳定性(翟明国, 2011)，此后出现陆内裂谷火山-沉积盖层(翟明国，2010)，代表华北克拉通克拉通化的第一套盖层沉积，标志着华北首次克拉通化的结束。
3.3 古元古代中晚期(2.2~1.85 Ga)地质事件世界上许多克拉通在2.45~2.2Ga期间约200~250Myr的时间内出现了岩浆活动停顿的静寂期(Condie and Kröner, 2008; Condie et al., 2009)，西部陆块无论是北部阴山地块，还是南部的鄂尔多斯地块抑或是二者间的孔兹岩带自2.45Ga以来也基本无岩浆活动的发生(图 5)，直到~2.35Ga仅在南部的鄂尔多斯地块基底开始有壳源花岗岩浆活动的出现，并集中发生在2.2~2.0Ga期间(峰期~2.03Ga)(图 5c)。这些花岗岩高硅(SiO2=70.51%~78.39%)和钾(K2O/Na2O=0.68~49.80)，贫钙(CaO=0.12%~1.41%)、低铁(FeOT=1.96%~4.86%)和(MgO=0.43%~1.73%)，A/CNK=1.32~2.64，具有轻重稀土强烈分馏，呈现了中等负Eu异常的右倾稀土模式，微量元素富集Rb、Ba、Th和K等大离子亲石元素，贫高场强元素，Pb明显富集、亏损Nb、Ta、P和Ti等元素，呈现了壳源过铝质钾玄系列岛弧区花岗岩类地球化学特征。它们的锆石Hf同位素组成变化大，呈现了明显偏负到正的εHf(t)(-12.2~+5.5)和范围较大的tDMC(3.12~2.25Ga)(图 7a, b)，并可分为εHf(t)=+0.04~+5.50, tDMC=2.25~2.52Ga以及εHf(t)=-12.2~+1.6，tDMC=2.44~3.12Ga两组，表明它们是既有幔源或新生陆壳源区也有太古代古老陆壳物质源区的岩浆产物。这种同时代、同位素组成变化很大、有幔源或新生陆壳及古老陆壳物质源区花岗岩类的同时出现，多为岛弧环境岩浆作用的结果(Kröner et al., 2014)，结合它们具岛弧花岗岩类地球化学特征，这些花岗岩类代表了鄂尔多斯地块古元古代晚期重要的弧岩浆活动。此类Hf同位素变化较大的2.2~2.0Ga弧岩浆锆石，在鄂尔多斯地块西北部基底(棋探1井，图 1)及北部孔兹岩带副变质片麻岩的继承碎屑锆石中都广泛出现(图 7a, b)，揭示它们成为这些副变质岩的主要物源提供者，同时也表明北部孔兹岩带的南界至少可延伸至现今鄂尔多斯盆地北缘的棋探1井一带。由此，根据北部孔兹岩带和阴山地块无该期岩浆活动推断，鄂尔多斯地块北缘的大洋俯冲很可能是由北向南俯冲于其下，其北缘成为活动大陆边缘，并沉积了孔兹岩带碎屑岩类。与其类似的岩浆活动在2.2~2.0Ga期间也广泛出现于华北克拉通中部带，所产生的岩浆锆石同样出现了变化范围很大的εHf(t)和tDMC(Geng et al., 2012; Santosh et al., 2015)(图 7c, d)，它们的岩石组合及地球化学特征也反映形成于活动陆缘岛弧环境(耿元生等，2006；Liu et al., 2012b; 杜利林等，2012; Santosh et al., 2015)，证明在鄂尔多斯地块东缘也存在同期大洋俯冲消减有关的岩浆活动。此外，鄂尔多斯地块基底变质碎屑岩和部分花岗岩类以及孔兹岩带各类变质岩均经历了1.95~1.85Ga的麻粒岩相变质作用改造(Wan et al., 2006, 2013a; Santosh et al., 2007a, b, 2009a, b; Yin et al., 2009, 2011, 2014; Hu et al., 2013; Jiao et al., 2013a, b; Cai et al., 2014; Wang et al., 2014; Zhang et al., 2015; Gou et al., 2016)，并在泥质麻粒岩中清楚的记录了四个变质演化阶段，构成一典型碰撞造山有关的顺时针P-T演化轨迹(Gou et al., 2016)，这种同期和类似的顺时针P-T演化轨迹也发现于中部带泥质麻粒岩中(Qian et al., 2013, 2015; Wei et al., 2014; Qian and Wei, 2016; Zhao et al., 2017)，表明1.95~1.85Ga期间鄂尔多斯地块作为一独立微陆块先后与北部阴山地块及东部陆块碰撞拼合形成华北克拉通统一基底。在碰撞拼合晚期的1.85Ga左右，陆壳抬升、发生减压熔融在孔兹岩带和中部构造带中出现大量S型花岗岩浆侵入(耿元生等, 2000, 2006; Zhao et al., 2008; Yin et al., 2009, 2011, 2014; Peng et al., 2012; Jiao et al., 2013b; Wang et al., 2017; )，指示碰撞造山已接近晚期并向伸展拉张演化阶段转化，此后进一步拉张裂解大范围出现~1.78Ga镁铁质岩墙群侵入(Peng et al., 2006, 2007, 2010; 彭澎，2016)，标志着华北陆块终极克拉通化基本结束，继而进入到克拉通盖层沉积的稳定演化阶段(翟明国，2011)。
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图 7 鄂尔多斯地块基底花岗岩、副片麻岩和孔兹岩带继承碎屑锆石以及华北中部带花岗岩锆石Hf同位素组成 数据引自本研究及赵瑞幅等，2011；Dan et al., 2012; 杜利林等，2012；Santosh et al., 2015; Zhang et al., 2015; 作者未刊数据 Fig. 7 Hf isotopic composition of the magmatic zircon from the granitoids and para-gneisses in the Ordos basement, detrital zircons from Khondalite Belt and magmatic zircons from the granitoids in the Trans-North China Orogen |
(1)华北克拉通西部阴山和鄂尔多斯地块基底正、副片麻岩及其盖层碎屑岩中均出现新太古和中太古代继承岩浆锆石，锆石Hf同位素二阶段模式年龄主要介于2.9~2.6Ga之间(峰值~2.75Ga)，并存在中太古和古太古代锆石Hf模式年龄，与阴山地块确定的2.7Ga岩石一道证明，西部不同地块基底可能于新太古代早期已形成，并在新太古代~2.7Ga发生了一期陆壳快速生长；
(2) 西部陆块在~2.7Ga经历一期陆壳快速生长后，在~2.5Ga又发生强烈的陆壳再造和少量陆壳生长，而后于2.2~2.0Ga期间沿鄂尔多斯地块北缘和东缘发生俯冲增生及1.95~1.85Ga的陆块碰撞拼合与改造。其中，2.55~2.45Ga期间强烈陆壳再造和生长过程，出现大量壳源和幔源岩浆侵入和麻粒岩相变质作用，揭示了由新太古代末的汇聚挤压转为古元古代初期的伸展，这与华北克拉通大范围岩浆变质事件十分类似，代表了华北克拉通首次克拉通化。2.2~2.0Ga期间，沿鄂尔多斯地块北缘和东缘发生大洋俯冲引起的陆缘弧岩浆活动，导致鄂尔多斯地块基底陆壳进一步增生和再造；于1.95~1.85Ga期间鄂尔多斯地块北部的孔兹岩带和东部的中部造山带均发生了具顺时针P-T演化轨迹的变质作用，形成陆-陆碰撞构造带，至~1.85Ga陆壳抬升伸展、导致陆壳物质减压熔融发生强烈混合岩化和壳源S型花岗岩的形成，其后镁铁质岩墙侵入，标志着克拉通化最终完成。
致谢 感谢组稿人万渝生研究员的热情邀稿！耿元生研究员和朱文斌教授两位评审人员的建设性建议，对本文的进一步完善和提高有很大的帮助，在此表示感谢！
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