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古元古代的构造-岩浆-变质及火山-沉积等地质记录表明，华北克拉通存在三条古元古代构造带：东部的胶-辽-吉带、西部的孔兹岩带及中部造山带（图1；Zhao Guochun et al.，2001，2003，2005，2012），或称辽吉（胶辽）造山/活动带、丰镇造山/活动带和晋豫造山/活动带（图2；翟明国等，2007；Zhai Mingguo et al.，2011）。它们的构造属性、构造格架及动力学演化等关键科学问题不仅对正确认识华北克拉通的形成演化、陆块聚-散的动力学过程非常重要，也涉及到重要矿产资源的形成，因而受到了广泛关注。胶-辽-吉古元古代构造带作为华北克拉通最具代表性、最复杂的一条古元古代造山/活动带，它不仅接受了古元古代巨量陆壳物质沉积，并经历了多期岩浆-变质及构造变形事件的改造（Zhao Guochun et al.，2012; 刘福来等，2015；Liu Jianhui et al.，2021；及其参考文献），经历了十分复杂的构造演化过程。关于其构造属性及构造演化长期存在争议，存在陆内裂谷闭合（张秋生等，1988）、弧-陆（白瑾等，1996；Bai Jin et al.，1996）或陆-弧-陆碰撞（贺高品等，1998a，1998b）及大陆裂解形成初始洋盆-俯冲碰撞洋盆闭合（翟明国等，2007）等多种构造演化模式。为了约束胶-辽-吉带的构造属性及演化，针对其古元古代的岩浆作用、构造变形、变质演化及火山-沉积记录开展了大量的地质调查及研究工作，取得了一系列重要进展，包括：① 确定了胶-辽-吉带的空间格架（Zhao Guochun et al.，2012; 刘福来等，2015；Peng Chong et al.，2016，2020; Liu Chaohui et al.，2018）；② 厘定了广泛分布的造山前伸展背景下形成的（2.2~2.1 Ga）条纹、条痕状A型花岗岩和数量有限的I型花岗岩（路孝平等，2004a，2004b，2005；郝德峰等，2004；Li Sanzhong et al.，2007; 杨德彬等，2009；郭素淑等，2009；Liu Jianhui et al.，2014，2021; 杨春明等，2015; Lan Tingguang et al.，2015; 田瑞聪等，2017; Cheng Shaobo et al.，2017; Wang Chengcheng et al.，2017；Wang Xinping et al.，2017，2020a，2020b; Liu Jin et al.，2018，2020，2021; Zhu Kai et al.，2019；杨玉伟等，2020），双峰式火山岩组合（张秋生等，1988；Peng Qiming et al.，1995; Bi Junhui et al.，2018）及同碰撞（路孝平等，2005；杨明春等，2015; Wang Xinping et al.，2017，2020b; Li Jian et al.，2020; Zhao Yan et al.，2021; Liu Jin et al.，2021）、碰撞后或非造山花岗岩（李三忠等，2003; 郝德峰等，2004；路孝平等，2004a，2004b，2005；杨进辉等，2007；Li Sanzhong，2007; Liu Jianhui et al.，2014; 任云伟等，2017；杨红等，2017；Liu Fulai et al.，2017; Zhang Xiaohui et al.，2021; Mu Maosong et al.，2022；及其参考文献）；③ 测定了带内古元古代变质沉积地层碎屑锆石的U-Pb年龄组分及其Hf同位素成分（Luo Yan et al.，2004，2008; Lu Xiaoping et al.，2006; Wan Yusheng et al.，2006; 刘福来等，2015；Wang Fang et al.，2017; Liu Chaohui et al.，2018; Xu Wang et al.，2019; 及其参考文献）；④ 重建了带内古元古代不同变质作用的P-T条件及P-T演化轨迹（Lu Liangzhao et al.，1996; 贺高品等，1998a，1998b; 刘文军等，1998；王舫等，2010；Tam et al.，2012a，2012b，2012c; Liu Pinghua et al.，2013; Cai Jia et al.，2020a，2020b; 及其参考文献）；⑤ 识别出多期古元古代伸展及挤压构造变形（Yang Zhensheng et al.，1988; 杨振升等，1989，1995；Liu Junlai et al.，1997; 刘俊来等，2002a，2002b，2022a; Li Sanzhong et al.，2005，2012; Tian Zhonghua et al.，2017; Zhang Jian et al.，2020）；⑥ 测定了带内古元古代变质铁镁质—超铁镁质岩的形成时代及变质时代（王惠初等，2011；刘平华等，2013; Meng En et al.，2014; Yuan Lingling et al.，2015; Wang Xinping et al.，2016; Xu Wang et al.，2019; Liu Jianhui et al.，2021）。这些研究进展极大地促进了我们对胶-辽-吉带构造演化的理解和认识。
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图1 华北克拉通构造单元划分及古元古代造山/活动带（据Zhao Guochun et al.，2001，2005）
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Fig.1 Tectonic subdivision and Paleoproterozoic orogenic/mobile belts of the North China craton (after Zhao Guochun et al., 2001, 2005)
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目前，就胶-辽-吉古元古代构造带经历了起始的大陆伸展及随后地壳挤压增厚的造山作用已基本达成了共识，但对大陆伸展的动力学机制仍存在大陆内部软流圈（热点）上涌（Liu Jianhui et al.，2021）、大陆下地壳拆沉诱发软流圈物质上涌（Liu Jin et al.，2018，2020）及与板块俯冲后撤有关的弧后拉张（Xu Wang et al.，2019）等不同认识。对古元古代造山作用也存在哥伦比亚超大陆汇聚背景下受重力驱动的自发造山作用（Liu Jianhui et al.，2021）、受板块边界作用远场效应的板内诱发造山作用（Liu Jin et al.，2018，2020）及弧-陆碰撞（Xu Wang et al.，2019）等不同认识。本文通过总结与胶-辽-吉古元古代构造带形成演化有关的岩浆作用、变质沉积-火山岩系和变质作用及演化等方面的研究成果，结合构造变形及地球物理等方面的证据，对胶-辽-吉古元古代构造带的起源及动力学演化开展了综合讨论。
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1 地质背景
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胶-辽-吉古元古代构造带位于华北克拉通东部陆块，从吉南经辽东、胶北到达安徽五河地区呈北东-南西走向展布，延伸达1200 km，将东部陆块分为其北部的龙岗地块和南部的狼林地块（图1、3）。龙岗地块太古宙基底主要由新太古代TTG花岗质岩石组成，并存在少量古太古代—中太古代岩石（万渝生等，2005；Wan Yusheng et al.，2023; 及其参考文献），其中在鞍山—本溪地区保存有最老~3.8 Ga的岩石（Liu Dunyi et al.，1992，2008; Song Biao et al.，1996；万渝生等，1999，2001；Wang Yusheng et al.，2023; 及其参考文献）。狼林地块早前寒武纪变质基底主要由新太古代TTG花岗质岩石及古元古代变质表壳岩和花岗质岩石组成，它们记录了新太古代末~2.5 Ga及古元古代约1.95~1.85 Ga两期变质变形事件（Zhao Guochun et al.，2006; Zhang Xiaohui et al.，2016a，2016b; 赵磊等，2016a，2016b; Zhai Mingguo et al.，2019; Zhao Lei et al.，2020，2024）。传统上，龙岗地块与狼林地块被认为具有统一的太古宙克拉通基底，称为中-朝克拉通（张秋生等，1988；Wu Jiashan et al.，1998）。最近的研究也证实它们具有统一的早前寒武纪变质基底及演化历史（Zhai Mingguo et al.，2019; Zhao Lei et al.，2020，2024）。
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图2 华北克拉通古元古代造山/活动带（据Zhai Mingguo et al.，2011）
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Fig.2 Paleoproterozoic orogenic/mobile belts in the North China craton (modified after Zhai Mingguo et al., 2011)
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胶-辽-吉古元古代构造带主要由大量的古元古代花岗质岩石、变质基性侵入岩墙和绿片岩相至麻粒岩相变质的火山-沉积岩系组成（张秋生等，1988; Liu Jianhui et al.，2021; 及其参考文献）。古元古代花岗质岩石包括造山前伸展背景约2.2~2.0 Ga侵位的条痕状、片麻状A型花岗岩和数量有限的I型花岗岩、同碰撞I型和S型花岗岩（Liu Jianhui et al.，2021; 及其参考文献）及碰撞后未变形的斑状花岗岩和碱性正长岩。变质基性岩包括形成于2.2~2.1 Ga的变质基性岩墙和形成于1.9~1.8 Ga的变质枕状熔岩（王惠初等，2011；Meng En et al.，2014; Yuan Lingling et al.，2015; Wang Xinping et al.，2016），前者部分经历了1.95~1.80 Ga近等温降压顺时针P-T演化的高压-超高温麻粒岩相变质作用（Tam et al.，2012a，2012b; Liu Pinghua et al.，2013，2017；刘平华等，2017; Cai Jia et al.，2020a）。古元古代变质火山-沉积岩系包括中国安徽的五河群、胶北的荆山群和粉子山群、辽东地区的南、北辽河群、吉南地区的吉安群和老岭群及朝鲜北部的摩天岭群。大量碎屑锆石U-Pb年龄数据显示，其物源主要来自两侧的太古宙变质基底和古元古代花岗质岩石，其沉积时代为2.20~1.95 Ga，并且普遍经历了约1.95~1.80 Ga具有顺时针变质P-T演化轨迹的绿片岩相—高压麻粒岩相变质作用（卢良兆等，1996；贺高品等，1998a，1998b; Zhou Xiwen et al.，2004; Tam et al.，2012a，2012b; Zou Yi et al.，2017，2019; Cai Jia et al.，2020b）或逆时针变质P-T演化轨迹的变质作用（卢良兆等，1996；贺高品等，1998a，1998b; Zou Yi et al.，2018）。中生代以来，胶-辽-吉古元古代构造带经历多期花岗质岩浆侵位和构造变形改造（Wu Fuyuan et al.，2005; Liu Junlai et al.，2005，2013，2022b），并卷入了中国东部中生代印支期—燕山期造山作用（Liu Fulai et al.，2014；刘俊来等，2022b；陈慧等，2022；任纪舜等，2024），使得带内不同地层及岩体之间的相互关系，以及该带的主要边界、空间展布、规模及延伸方向存在不同的认识（图2、3；Zhao Guochun et al.，2005，2012; 翟明国等，2007；Zhai Mingguo et al.，2011； 翟明国，2012; 刘福来等，2015；吴福元等，2016）。
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图3 东部陆块胶-辽-吉造山/活动带的地质简图（据Zhao Guochun et al.，2005; 刘福来等2015）
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Fig.3 Simplified geological map of the Paleoproterozoic Jiao-Liao-Ji orogenic/active belt in Eastern block, North China craton (after Zhao Guochun et al., 2005; Liu Fulai et al., 2015)
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2 岩浆作用
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胶-辽-吉古元古代构造带岩浆作用强烈，伴随构造带的整个发展演化过程，包括造山前伸展构造环境的双峰式岩浆作用、同碰撞地壳挤压增厚背景下的岩浆作用及碰撞后造山带垮塌环境的岩浆作用等。这些不同时期不同构造背景下形成的不同性质岩浆作用为胶-辽-吉古元古代构造带的形成、发展及演化提供了重要的约束。
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2.1 造山前（2.2~2.0 Ga）花岗质岩石
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胶-辽-吉古元古代构造带造山前花岗质岩浆作用是构造带内最强烈的岩浆作用，沿整个构造带广泛发育，形成了构造带内最广泛分布的条纹、条痕状花岗质片麻岩，包括（含磁铁矿）黑云角闪二长花岗岩、正长（钾长）花岗岩、正长岩及黑云母花岗岩等（附表1）。这些造山前侵位的变形花岗质岩石一个最典型的特征是发育有由磁铁矿、黑云母及角闪石等暗色矿物组成的暗色条痕或条纹，形成条痕或条纹状构造，统称“条痕状辽吉花岗岩”。锆石U-Pb年代学研究显示，它们主要形成于2.2~2.1 Ga，部分形成于2.1~2.0 Ga，并记录了1.95~1.80 Ga的变质作用（附表1）。这些变形的花岗质岩石具高硅、富铁及全碱（图4a），K2O/Na2O比值大于1，贫钙、镁（低Mg#）、铝及钛，属铁质、碱钙性或钙-碱性系列（图4c、d），它们具有较高的稀土元素总量，轻微的轻重稀土分异，显示了明显的铕负异常（图5a），高的Th、U、Zr、Hf、K、Yb及Y含量，低的Sr、Ti、Cr及Ni含量（图5b），同时它们具有高的Zr+Nb+Ce+Y（图6a、b）及10000Ga/Al值（图6c、d），使其与未分异的M型、I型及S型花岗岩有所区分，在A型花岗岩判别图解上显示为A型花岗岩。此外，它们具有高的岩浆形成温度（Lan Tingguang et al.，2015; Wang Chengcheng et al.，2017; Wang Xinping et al.，2017，2020a; Liu Jin et al.，2021），这些岩石地球化学特征指示它们具有典型A型花岗岩的特征。根据Eby（1992）A型花岗岩的分类，属于A2型花岗岩。全岩Nd及锆石Hf同位素指示它们主要源自TTG岩石的重熔，并有少量源自地幔新生物质的加入（图7a、b; Lan Tingguang et al.，2015; Wang Xinping et al.，2017，2020a，2020b; Zhao Yan et al.，2021; Mu Maosong et al.，2022）。这些具有典型A型花岗岩岩石地球化学成分、造山前形成的变形花岗质岩石形成于高温低压的伸展构造背景下大陆地壳（TTG岩石）的部分熔融。
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此外，除了广泛分布的A型花岗岩外，胶-辽-吉古元古代构造带内也存在造山前形成的具有埃达克质花岗岩地球化学性质的I型花岗岩，它们与A型花岗岩同时形成，但岩体数量及规模有限，目前对于它们的成因存在拆沉地壳、加厚下地壳或俯冲洋壳的部分熔融等多种认识（宋运红等，2016；Li Jian et al.，2020; Liu Jin et al.，2020；Wang Xinping et al.，2020a; 及其参考文献）。根据它们所处的伸展构造背景，基性下地壳的部分熔融是I型花岗岩形成的一种可选模式。
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2.2 造山前（2.2~2.1 Ga）基性岩
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造山前的基性岩浆作用在胶-辽-吉古元古代构造带广泛发生，形成带内广泛分布的变质基性岩墙、岩脉或岩块，以及巨厚的变质基性火山（玄武岩）沉积。锆石U-Pb年代学研究显示，它们主要形成于2.2~2.1 Ga，并普遍记录了1.95~1.80 Ga的变质作用（附表1），这些变质基性侵入岩及变质基性火山岩与同时形成的花岗质岩石及酸性火山岩构成胶-辽-吉古元古代构造带造山前伸展背景下的双峰式岩浆作用。它们具有亚碱性拉斑系列玄武质岩石地球化学属性（图4a、b），显示变化的硅及铝，高的钙、铁，低的镁、全碱、钛及Mg#值，轻稀土（LREE）相对重稀土（HREE）轻微富集，无明显的Eu异常，富集大离子亲石元素（LILEs）Rb、Ba及K，亏损高场强元素（HFSEs）Nb、Ta、Zr、Hf及Ti等，显示出与E-MORB玄武岩类似的稀土及微量元素地球化学特征（图5c、d），正的锆石εHf（t）值（图7c、d）及变化的全岩εNd（t）值。它们的全岩主量及微量元素地球化学变化趋势及锆石Hf及全岩Nd同位素表明它们可能形成于大陆裂谷环境，源自软流圈地幔的部分熔融（Liu Jianhui et al.，2021）。并且它们的原始岩浆在上升过程中经历了大陆岩石圈地幔及大陆地壳的同化混染作用，以及斜长石、橄榄石及单斜辉石的分离结晶及磷灰石和钛-铁氧化物（如钛铁矿、磁铁矿）的堆晶作用。
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图4 胶-辽-吉古元古代构造带造山前A型花岗岩及造山前变质基性岩地球化学分类图
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Fig.4 Geochemical classification of pre-orogenic A-type granitoid and meta-mafic rocks in the Paleoproterozoic Jiao-Liao-Ji tectonic belt
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（a）—TAS（硅-碱）岩石分类图（据Le Bas et al.，1986）；（b）—变质基性岩AFM（（Na2O+K2O）-FeO-MgO）图（据Irvine and Baragar，1971）；（c）—TFeO/（TFeO+MgO）vs. SiO2；（d）—（Na2O+K2O-CaO）vs. SiO2（据Frost et al.，2001）; A型花岗岩数据源自Lan Tingguang et al.，2015; Wang Xinping et al.，2017，2020a; Liu Jin et al.，2018，2020; Liu Jianhui et al.，2021; Zhang Wen et al.，2022；变质基性岩数据源自Meng En et al.，2014; Yuan Lingling et al.，2015; Wang Xinping et al.，2016; Cheng Changquan et al.，2022
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(a) —the TAS classification (after Le Bas et al., 1986) ; (b) —the AFM ( (Na2O+K2O) -FeO-MgO) classification (after Irvine and Baragar, 1971) for the meta-mafic rocks; (c) — TFeO/ (TFeO+MgO) vs.SiO2; (d) — (Na2O+K2O-CaO) vs. SiO2 classifications (after Frost et al., 2001) ; data for A-type granitoid from Lan Tingguang et al., 2015; Wang Xinping et al., 2017, 2020a; Liu Jin et al., 2018, 2020; Liu Jianhui et al., 2021; Zhang Wen et al., 2022; data for meta-mafic rocks from Meng En et al., 2014; Yuan Lingling et al., 2015; Wang Xinping et al., 2016; Cheng Changquan et al., 2022
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2.3 同碰撞及碰撞后花岗质岩石
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同碰撞花岗质岩石包括I型花岗质岩石和S型花岗岩。I型花岗质岩石包括细粒黑云母二长花岗岩、斜长花岗岩、斑状二长花岗岩及石英闪长岩等，这些花岗质岩石通常具有右倾的稀土配分曲线，富集轻稀土，显示轻微的Eu正异常或无异常，高的Sr/Y及LaN/YbN比值，岩石学及地球化学特征显示为弧型或埃达克质的I型花岗质岩石（如青城子花岗岩）、主要形成于同碰撞造山的加厚地壳背景（路孝平等，2005；Wang Xinping et al.，2017，2020b; Li Jian et al.，2020; Zhao Yan et al.，2021; Liu Jin et al.，2021）；S型花岗岩主要为巨斑状—环斑状含石榴子石（矽线石）花岗岩，主要形成于后碰撞造山阶段（路孝平等，2005；杨明春等，2015）。锆石U-Pb年代学数据显示它们主要形成于1.95~1.85 Ga，对应胶-辽-吉古元古代造山变质作用的高压麻粒岩相变质阶段（附表1; Liu Fulai et al.，2017; Liu Jin et al.，2021）。
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图5 造山前A型花岗质岩石及变质基性岩球粒陨石标准化稀土元素配分图（a、c）及原始地幔标准化微量元素蛛网图（b、d）（标准化值据Sun and McDonough，1989）
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Fig.5 Chondrite-normalized REE patterns (a, c) and primitive mantle-normalized trace element spider diagrams (b, d) for pre-orogenic A-type granitoids and meta-mafic rocks (normalization values after Sun and McDonough, 1989)
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数据源自Meng En et al.，2014; Yuan Lingling et al.，2015; Wang Xinping et al.，2016; Cheng Changquan et al.，2022
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Data from Meng En et al., 2014; Yuan Lingling et al., 2015; Wang Xinping et al., 2016; Cheng Changquan et al., 2022
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未变形的巨斑状—环斑状花岗岩（包括含石榴子石巨斑状花岗岩、黑云母巨斑状花岗岩及肉红色巨斑状钾长花岗岩等）、斜长花岗岩、碱性正长岩（包括角闪石正长岩及辉石正长岩）、含电气石伟晶花岗岩及石英闪长岩等，在胶-辽-吉古元古代构造带中主要分布在吉林集安、辽宁宽甸八河川镇—牛毛坞镇和桓仁东下四平西街—芦家堡子一带、辽宁盖州卧龙泉镇—矿洞沟镇一带及胶北地体内，在朝鲜半岛亦有分布（蔡剑辉等，2002；路孝平等，2005；杨进辉等，2007；Liu Jianhui et al.，2014；杨红等，2017；Li Youlian et al.，2017; Liu Fulai et al.，2017; Zhang Xiaohui et al.，2021; Mu Maosong et al.，2022；及其参考文献），侵入古元古代变质火山-沉积岩系，它们通常具有高的重稀土含量，显示了明显的Eu负异常，亏损Sr、Ti及高场强元素Nb、Ta等，并且具有高的岩浆形成温度，显示出A、S或I型花岗岩的岩石及地球化学特征，主要形成于碰撞造山后造山带垮塌或非造山高温低压的伸展构造背景，源自古元古代花岗质岩石、变质火山-沉积岩系、基性岩或地幔的部分熔融。锆石U-Pb年代学研究显示它们主要形成于1.85~1.80 Ga（附表1），对应胶-辽-吉古元古代变质作用的中低压麻粒岩相—角闪岩相阶段（Liu Fulai et al.，2017）。
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3 变质火山-沉积岩系
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胶-辽-吉古元古代构造带内发育有巨厚的变质火山-沉积岩系，包括胶北的粉子山群和荆山群、辽东的北辽河群和南辽河群、吉南的老岭群和集安群、北朝鲜的摩天岭群及西南延伸方向安徽蚌埠一带的五河群（Zhao Guochun et al.，2012）。其原岩为一套玄武岩和英安岩-流纹岩所构成的双峰式火山岩、灰岩、白云岩和陆源碎屑沉积，沉积环境为稳定的被动陆缘（张秋生等，1988），并经历了绿片岩相—麻粒岩相的变质作用（刘福来等，2015）。传统上，胶-辽-吉古元古代构造带被进一步划分为北带和南带，其中胶北的粉子山群、辽东的北辽河群及吉南的老岭群为北带，胶北的荆山群、辽东的南辽河群及吉南的集安群为南带（Zhao Guochun et al.，2005；刘福来等，2015）。近年来，大量的碎屑锆石U-Pb年代学研究显示，北带与南带的地层胶北的粉子山群与荆山群（图8a、b）、辽东南的北辽河群与南辽河群（图8c、d）、吉南的老岭群与集安群（图8e、f），及安徽蚌埠的五河群（图8g）和北朝鲜的摩天岭群（图8h）均具有类似的碎屑锆石U-Pb年龄组分，指示无论北带还是南带均主要源自太古宙大陆基底岩石及古元古代花岗质岩石。根据碎屑锆石U-Pb年代学（图8a~h；Luo Yan et al.，2004，2006; Li Sanzhong et al.，2005; Lu Xiaoping et al.，2006; Wan Yusheng et al.，2006; 刘福来等，2015；王舫等，2017；Wang Fang et al.，2017，2020; Liu Chaohui et al.，2018; Zhang Wen et al.，2018；Ye Lina et al.，2021; 及其参考文献）及地层内英安岩-流纹岩等中酸性火山岩的锆石U-Pb年代学研究结果（附表1），表明这些变质沉积-火山岩系的原岩沉积时限为2.20~1.95 Ga，而变质时代为1.95~1.80 Ga。
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图6 造山前A型花岗岩判别图（据Whalen et al.，1987）
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Fig.6 Discrimination diagrams of A-type granite for Paleoproterozoic pre-orogenic A-type granitoids (after Whalen et al., 1987)
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FG—分异的长英质花岗岩；OTG—未分异的M、I及S型花岗岩；数据源自Lan Tingguang et al.，2015; Wang Xinping et al.，2017，2020a; Liu Jin et al.，2018，2020; Liu Jianhui et al.，2021; Zhang Wen et al.，2022
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FG—fractionated felsic granites; OTG—unfractionated M-, I-, and S-type granites; data from Lan Tingguang et al., 2015; Wang Xinping et al., 2017, 2020a; Liu Jin et al., 2018, 2020; Liu Jianhui et al., 2021; Zhang Wen et al., 2022
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4 变质作用及演化
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有关胶-辽-吉带的变质作用及变质演化，早期（传统）的研究认为，位于该带南部的荆山群、南辽河群及集安群具有逆时针变质P-T演化轨迹，而北部的粉子山群，北辽河群和老岭群则表现为顺时针的变质P-T演化轨迹，并且认为胶北地区的荆山群和粉子山群变质作用较强，可达高角闪岩相到中—低压麻粒岩相，而南、北辽河群，集安群和老岭群变质作用相对较弱，为绿片岩相—低角闪岩相，局部可达高角闪岩相（卢良兆等，1996； 贺高品和叶慧文，1998a，1998b）。近年来，随着胶-辽-吉古元古代构造带变质作用研究的深入，新的研究显示，不仅胶北地区存在具有顺时针变质P-T演化轨迹的中压及高压泥质麻粒岩（图9a; 王舫等，2010；Tam et al.，2012a，2012b; Zou Yi et al.，2017，2019）和高压基性麻粒岩（图9b；刘文军等，1998；王舫等，2010；Tam et al.，2012c; 刘平华等，2013；Liu Pinghua et al.，2017），而且在南辽河群和集安群中也发现了具有顺时针变质P-T演化轨迹的泥质麻粒岩（图9a; Cai Jia et al.，2017，2020b; Liu Pinghua et al.，2019）和基性麻粒岩（图9a；刘福来等，2015），在安徽蚌埠发现了古元古代高压-超高温基性麻粒岩（图9b；Cai Jia et al.，2020b）。并且变质锆石及独居石U-Pb年代学研究显示，从构造带西南延伸的蚌埠地区（图9c）、到胶北地体（图9d）、辽东南地区（图9e）及构造带东北端的吉南（图9f）地区具有统一的1.95~1.80 Ga变质作用时间，其中1.95~1.85 Ga为高压麻粒岩相变质阶段，而1.85~1.80 Ga为中低压麻粒岩相变质阶段。这些最新的变质作用及演化研究进一步确定了胶-辽-吉古元古代构造带经历了古元古代地壳增厚造山到造山带垮塌、地壳减薄的造山作用过程。
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图7 造山前古元古代花岗质岩石及变质基性岩锆石Hf同位素成分
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Fig.7 Comprehensive zircon Hf isotope composition for pre-orogenic granitoids and meta-mafic rocks
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（a、b）—造山前花岗质岩石的锆石 U-Pb年龄-εHf（t）值及两阶段Hf模式年龄（数据来自Liu Jianhui et al.，2014，2021; Lan Tingguang et al.，2015; 宋运红等，2016；陈井胜等，2017；Wang Chengcheng et al.，2017; Wang Xinping et al.，2017; Wang Chaoyang et al.，2018; Bi Junhui et al.，2018; Zhu Kai et al.，2019; Dong Yu et al.，2019; Liu Jin et al.，2020，2021; Zhang Wen et al.，2022）；（c、d）—变质基性岩的锆石 U-Pb年龄-εHf（t）值及单阶段Hf模式年龄（数据源自Meng En et al.，2014; Wang Xinping et al.，2016; Liu Jianhui et al.，2021）；CHUR—球粒陨石均一储库
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(a, b) —U-Pb ages vs. εHf (t) values and two-stage Hf model ages for pre-orogenic granitoids (data from Liu Jianhui et al., 2014, 2021; Lan Tingguang et al., 2015; Song Yunhong et al., 2016; Chen Jingsheng et al., 2017; Wang Chengcheng et al., 2017; Wang Xinping et al., 2017; Wang Chaoyang et al., 2018; Bi Junhui et al., 2018; Zhu Kai et al., 2019; Dong Yu et al., 2019; Liu Jin et al., 2020, 2021; Zhang Wen et al., 2022) ; (c, d) —U-Pb ages vs.εHf (t) values and single-stage Hf model ages for meta-mafic rocks (data from Meng En et al., 2014; Wang Xinping et al., 2016; Liu Jianhui et al., 2021) ; CHUR—chondritic uniform reservoir
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图8 胶-辽-吉古元古代构造带不同变质沉积地层的碎屑锆石U-Pb年龄谱（数据源自刘福来等，2015； Liu Chaohui et al.，2018; Zhang Wen et al.，2018; 及其参考文献）
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Fig.8 Detrital zircon U-Pb age spectra of different metamorphic sedimentary strata in the Paleoproterozoic Jiao-Liao-Ji tectonic belt (data from Liu Fulai et al., 2015; Liu Chaohui et al., 2018; Zhang Wen et al., 2018; and references therein)
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5 讨论与结论
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5.1 2.2~2.0 Ga地幔物质上涌驱动的陆内伸展
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胶-辽-吉古元古代构造带内广泛分布的造山前A型花岗岩、变质基性侵入岩、由大量的变质流纹岩-英安岩及变质玄武岩组成的双峰式火山岩建造、巨厚的变质火山-沉积岩系、构造带两侧龙岗地块与狼林地块统一的早前寒武纪变质基底及演化历史、地球物理及构造分析均指示早期具有拉张性质的构造变形作用等地质地球物理证据，表明胶-辽-吉古元古代构造带在早期经历了大陆的伸展变形作用或裂谷作用。有关大陆伸展变形，包括主动和被动伸展变形作用，存在岩石圈拉伸及/或地幔上涌（如地幔柱或热点；McKenzie，1978; Jarvis et al.，1980; Olsen，1995; Li Zhengxiang et al.，1999; Li Xianhua et al.，2002）、俯冲板片的回卷及俯冲后撤（Schellart，2005; Schellart et al.，2005）、块体的逃逸或走滑断裂作用（Molnar et al.，1975）及下地壳拆沉（Burchfiel et al.，1985; Kay et al.，1993; Rey et al.，2001）等四种流行并被广泛接受的地球动力学模式。一些学者根据具有所谓“弧岩浆”地球化学性质的造山前高钾钙碱性高分异“I型”花岗质岩石、变质基性侵入岩及火山岩，提出俯冲板片的回卷及俯冲后撤驱动的弧后伸展模式（Xu Wang et al.，2019; Hoernle et al.，2020；及其参考文献）。但是，古元古代早期地球是否存在现代型板块构造仍是目前地球科学领域的一大科学挑战，而且当时岩石圈的成分、结构及热状态与现代岩石圈存在明显的差异，进而也会导致当时板块构造作用的不同（翟明国，2012；Zheng Yongfei et al.，2020; Zhai Mingguo et al.，2020）。就华北克拉通而言，现代板块构造可能直到~0.7 Ga才开始启动（Zhai Mingguo et al.，2020）。尤其值得注意的是，整个胶-辽-吉古元古代构造带一直没有发现真正意义上类似于现代板块洋-陆俯冲作用有关的岩石-构造组合（如残留洋壳、俯冲增生杂岩（楔）、双变质带、与板片俯冲前进或后退有关的岩浆作用时空变化、弧背构造及沉积、多期弧后伸展及沉积作用、以及大型走滑断裂等）。“弧岩浆”的地球化学性质可能主要继承了源区太古代TTG岩石或基性岩浆上升过程受大陆岩石圈地幔和地壳的同化混染作用（Liu Jianhui et al.，2021）。此外，带内巨厚的变质火山-沉积岩系具有稳定的被动陆缘沉积环境（张秋生等，1988），“南带”和 “北带”变质沉积地层具有统一的地层层序及类似的物源（如统一的锆石U-Pb成分）（图8），这些都难以用弧后伸展模式解释。另外一些学者则提出岩石圈的拆沉及随后软流圈的上涌可能导致了东部陆块沿胶-辽-吉古元古代构造带陆内伸展（裂谷作用）和造山前A型花岗岩的形成（Liu Jin et al.，2020）。但是，这种模式导致的软流圈上涌有限，很难造成胶-辽-吉古元古代构造带规模的陆内裂谷作用。
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图9 胶-辽-吉古元古代构造带中压—高压泥质麻粒岩（a）及基性麻粒岩（b）的变质P-T演化及不同地区的变质年龄（c~f）（据Cai Jia et al.，2020a，2020b; 及其参考文献）
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Fig.9 Summary of the metamorphic P-T paths for medium pressure (MP) -high pressure (HP) pelitic granulites (a) and mafic granulites (b) , and metamorphic zircon U-Pb ages (c~f) for different regions in the Paleoproterozoic Jiao-Liao-Ji tectonic belt (after Cai Jia et al., 2020a, 2020b; and references therein)
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1—辽宁南辽河石榴角闪岩（Liu Pinghua et al.，2017）；2—辽宁南辽河泥质麻粒岩（Liu Pinghua et al.，2019）；3—胶北高压基性麻粒岩（Liu Pinghua et al.，2013）；4—胶北高压泥质麻粒岩（Zou Yi et al.，2017）；5—胶北高压泥质麻粒岩（Tam et al.，2012a）；6—胶北高压基性麻粒岩（Tam et al.，2012c）；7—胶北高压泥质麻粒岩（王舫等，2010）；8—胶北中压泥质麻粒岩（Tam et al.，2012b）；9—吉南中压Opx-Crd-Grt泥质麻粒岩（Cai Jia et al.，2017）；10—吉南高压Sil-Crd-Grt泥质麻粒岩（Cai Jia et al.，2020a）；11—安徽蚌埠高温—超高温基性麻粒岩（Cai Jia et al.，2020b）；Ky—蓝晶石；And—红柱石；Sil—矽线石；Crd—堇青石；Grt—石榴子石；Qz—石英；Cpx—单斜辉石；Opx—斜方辉石
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1—garnet amphibolite from southern Liaohe, Liaoning (Liu Pinghua et al., 2017) ; 2—pelitic granulite from southern Liaohe, Liaoning (Liu Pinghua et al., 2019) ; 3—HP mafic granulite from Jiaobei terrane (Liu Pinghua et al., 2013) ; 4—HP pelitic granulite from Jiaobei terrane (Zou Yi et al., 2017) ; 5—HP pelitic granulite from Jiaobei terrane (Tam et al., 2012a) ; 6—HP mafic granulite from Jiaobei terrane (Tam et al., 2012c) ; 7—HP pelitic granulite from Jiaobei terrane (Wang Fang et al., 2010) ; 8—MP pelitic granulite from Jiaobei terrane (Tam et al., 2012b) ; 9—MP Opx-Crd-Grt pelitic granulite from southern Jilin (Cai Jia et al., 2017) ; 10—HP Sil-Crd-Grt pelitic granulites from southern Jilin (Cai Jia et al., 2020a) ; 11—high temperature-ultrahigh temperature mafic granulite from Bengbu area, Anhui (Cai Jia et al., 2020b) ; Ky—kyanite; And—andalusite; Sil—sillimanite; Crd—cordierite; Grt—garnet; Qz—quartz; Cpx—clinopyroxene; Opx—orthopyroxene
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考虑到下地壳的加热在降低大陆岩石圈伸展所需的岩石圈强度和厚度方面起着至关重要的作用。而地幔柱（热点）上升或弧后区域含俯冲板片流体岩浆的上涌能够形成异常高温和相对低密度的软流圈上涌地幔，并能提供长期的导热和浮力（Morgan，1971; Loper，1985; Duncan et al.，1991; Olsen，1995）。同时考虑到胶-辽-吉古元古代构造带同时形成的高温A型花岗质岩石和源自地幔的基性岩石以及高温（HT）—超高温（UHT）变质作用所指示的高地温梯度（Zou Yi et al.，2019; Cai Jia et al.，2020b）。我们建议与地幔柱（热点）上升形成的异常高温和相对低密度软流圈上涌是东部陆块沿胶-辽-吉古元古代构造带在约2.2~2.0 Ga发生陆内伸展最可能的动力学机制。
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5.2 重力驱动的板块汇聚造山作用
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胶-辽-吉古元古代构造带具有顺时针变质P-T演化轨迹的中压—高压泥质麻粒岩及高温—超高温基性麻粒岩的厘定（图9a、b），指示胶-辽-吉古元古代构造带经历了与板块汇聚有关的从地壳增厚到地壳减薄的造山作用过程。由于早期板块构造的动力学机制与现代板块构造可能存在显著不同（Zhai Mingguo et al.，2020）。因此，确定胶-辽-吉古元古代构造带板块汇聚、地壳增厚造山的驱动力对于理解早期板块构造的动力学机制具有重要的意义。带内同时出现的高压及高温—超高温麻粒岩不仅暗示地壳的增厚作用，而且也证实带内具有高的地温梯度。东部陆块在太古宙末伴随着大量TTG岩石的形成会形成大量麻粒岩相—榴辉岩相下地壳残留体（图10a），由于华北克拉通东部陆块在新太古宙末形成了稳定的克拉通岩石圈地幔，能够确保其麻粒岩相—榴辉岩相的高密度下地壳能够稳定保留。东部陆块岩石圈受异常高温和相对低密度软流圈上涌所驱动，在2.2~2.0 Ga沿胶-辽-吉古元古代构造带发生伸展，伸展停止后，不仅岩石圈冷却密度增加会发生热沉降，而且保留下来的高密度榴辉岩化下地壳连同岩石圈地幔受重力（负浮力）驱动能够沉入高温和相对低密度的软流圈地幔，并驱动两侧的龙岗地块和狼林地块发生汇聚，导致胶-辽-吉古元古代构造带发生地壳增厚造山作用，带内岩石发生中压—高压及高温—超高温麻粒岩相变质作用。这种受板块自身重力（负浮力）驱动的板块俯冲（下沉）并拖拽板块运动已被地球物理观测、板块运动的力学分析及动力学模拟所证实（Isacks et al.，1968; Anderson et al.，2001; Stern et al.，2007; 陈凌等，2020），并被普遍接受和理解的重要板块构造活动，在板块构造中发挥了重要的作用。加之胶-辽-吉古元古代构造带内并没有洋-陆俯冲作用导致地壳增厚的岩石-构造组合。因此，我们提出东部陆块高密度麻粒岩相—榴辉岩相下地壳连同岩石圈地幔，在沿胶-辽-吉带发生伸展变形后，受重力（负浮力）作用，相对热的、低密度的软流圈发生下沉（俯冲）（图10c），并驱动动两侧的龙岗地块和狼林地块发生汇聚造山作用。之后，随着造山带根部的移除，软流圈上涌，造山带发生垮塌和造山后伸展（图10d）。
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5.3 动力学演化
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综合胶-辽-吉古元古代构造带的构造-岩浆-变质及变质火山-沉积序列已有研究，建立了胶-辽-吉古元古代构造带的起源及动力学演化模式：① 华北克拉通东部陆块新太古代末巨量TTG岩石形成的同时，在下地壳形成巨量高密度的麻粒岩相—榴辉岩相残留物质，新太古代末已形成的稳定克拉通岩石圈地幔使这些高密度的麻粒岩相—榴辉岩相残留物质能够稳定保留（图10a）。② 在2.2~2.0 Ga期间，受地幔柱（热点）驱动，热的相对低密度的软流圈上涌，东部陆块沿胶-辽-吉构造带发生陆内伸展变形（陆内裂谷作用），破裂形成北部的龙岗地块和南部的狼林地块，并导致TTG岩石、基性下地壳及同位素亏损的软流圈地幔发生部分熔融，形成造山前A型花岗质岩石、I型花岗质岩石、基性及超基性侵入岩和双峰式火山岩系（图10b）。③ 在1.95~1.85 Ga，高密度的麻粒岩相—榴辉岩相下地壳连同岩石圈地幔，受重力作用（负浮力）驱动，发生俯冲（下沉）进入热的、低密度的软流圈地幔，带动龙岗地块和狼林地块沿胶-辽-吉带发生汇聚造山作用，导致地壳增厚和同碰撞S型花岗岩、埃达克质I型花岗岩、中压—高压及高温—超高温麻粒岩的形成（图10c）。④ 在1.85~1.80 Ga，造山带发生去根作用，软流圈上涌，导致造山带的垮塌、快速剥露和造山后伸展，广泛的造山后岩浆作用和具有逆时针变质 P-T演化的变质作用（Zou Yi et al.，2018；图10d）。
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图10 胶-辽-吉古元古代构造带构造及动力演化图
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Fig.10 Schematic tectonic and geodynamic evolution of the Paleoproterozoic Jiao-Liao-Ji belt
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（a）—巨量的高密度麻粒岩相—榴辉岩相下地壳残留随着太古宙末巨量TTG岩石的形成而产生；（b）—在2.2~2.0 Ga，热的、相对低密度的软流圈地幔（热点）上涌驱动动东部陆块沿胶-辽-吉带发生陆内伸展，分裂成北部的龙岗地块与南部的狼林地块；（c）—在1.95~1.85 Ga，高密度下地壳连同岩石圈地幔受重力（负浮力）驱动俯冲（下沉）进入热而低密度的软流圈，带动两侧的龙岗地块与狼林地块汇聚挤压造山，造成地壳加厚及顺时针变质P-T演化轨迹的中压—高压麻粒岩相和高温—超高温麻粒岩相的变质作用；（d）—在＜1.8 Ga（1.85~1.80 Ga），造山带去根，软流圈上涌，造山带垮塌及造山后伸展
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(a) —voluminous high-density granulite-eclogite facies residual was generated in the lower crust along with formation of voluminous Archean TTGs in the Eastern block, and was preserved by the stable craton lithospheric mantle formed at the end of Archean; (b) —at ca.2.2~2.0 Ga, intracontinental extension driven by upwelling of hot and relatively low-density asthenospheric mantle (hotspot) along the Jiao-Liao-Ji belt took place, resulting in the Eastern block was broken into the northern Longgang block and southern Nangrim block; (c) —at ca.1.95~1.85 Ga, plate-convergent compressed orogenic processes led by gravity (negative buoyancy) -driven sinking (subduction) of highdensity lower crust (lithosphere) , which causes crustal thickening and formation of medium pressure (MP) -high-pressure (HP) and hightemperature (HT) ultrahightemperature (UHT) granulites with clockwise pressure-temperature-time (P-T-t) paths; (d) —at ＜1.8 Ga (1.85~1.80 Ga) , the orogenic belt collapse caused by the delamination of the orogenic root, and subsequent hot asthenospheric upwelling resulted in rapid exhumation and postorogenic extension of the orogenic belt
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致谢：感谢任纪舜院士对本人开展太平洋构造域1∶500万大地构造图编制及大地构造研究所给予的支持、帮助、鼓励和指导！并向任先生的严谨治学态度和在大地构造领域的卓越贡献致敬！祝任先生福如东海，寿比南山！对两位审稿人给予的修改建议表示衷心的感谢!
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附件：本文附件（附表1）详见http://www.geojournals.cn/dzxb/dzxb/article/abstract/202501090?st=article_issue
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摘要
胶-辽-吉古元古代构造带的构造属性及动力学演化长期存在争议。本文通过总结该带构造-岩浆-变质作用及变质火山-沉积岩系的已有研究成果，发现造山前2.2~2.0 Ga花岗质岩石主要为形成于高温低压伸展构造环境的A型花岗岩，部分为源自下地壳基性岩部分熔融形成的I型花岗岩，它们与变质基性侵入岩及变质流纹岩-英安岩和变质玄武岩构成了造山前大陆伸展背景下的双峰式岩浆作用。它们“弧岩浆”属性的地球化学性质主要继承自源区太古宙TTG岩石或基性岩浆上升过程受大陆岩石圈地幔和地壳的同化混染作用。整个胶-辽-吉古元古代构造带没有发现真正意义上类似于现代板块洋-陆俯冲作用有关的岩石-构造组合(如残留洋壳、俯冲增生杂岩(楔)、弧背构造、大型走滑断裂、双变质带及岩浆作用的时空变化等)。龙岗地块和狼林地块具有统一的太古宙克拉通基底及演化历史。“南带”和“北带”的不同变质沉积地层具有类似的物源，沉积环境为稳定的被动陆缘，沉积时代为2.20~1.95 Ga，并经历了1.95~1.80 Ga顺时针变质P-T演化轨迹的中压—高压麻粒岩相和高温—超高温变质作用。综合已有的地质及地球物理证据，构建了胶-辽-吉古元古代构造带的起源及动力学演化模式：① 华北克拉通东部陆块新太古代末巨量TTG岩石形成的同时，在下地壳形成巨量高密度的麻粒岩相—榴辉岩相残留物质，新太古代末已形成的稳定克拉通岩石圈地幔使这些高密度的麻粒岩相—榴辉岩相残留物质能够稳定保留。② 在2.2~2.0 Ga，热的、相对低密度的软流圈热点上涌，东部陆块沿胶-辽-吉构造带发生陆内伸展变形，破裂形成北部的龙岗地块和南部的狼林地块。③ 在1.95~1.85 Ga, 高密度的榴辉岩化下地壳连同岩石圈地幔，受重力(负浮力)作用驱动，俯冲(下沉)进入热的、低密度的软流圈地幔，带动龙岗地块和狼林地块沿胶-辽-吉带发生汇聚造山作用。④ 在1.85~1.80 Ga，造山带去根，软流圈上涌，造山带垮塌及造山后伸展。
Abstract
The origin and geodynamic evolution of the Jiao-Liao-Ji tectonic belt have long been controversial. This article summarizes comprehensive research results on the tectono-magmatic-metamorphic processes and metasedimentary-volcanic successions in this belt. It is found that the 2.2~2.0 Ga pre-orogenic granitoids are mainly A-type, formed in a high-temperature, low-pressure extensional setting. Some are I-type granitoids derived from partial melting of mafic rocks in the lower crust. These pre-orogenic granitoids, along with metamafic intrusive rocks, metarhyolite-dacite, and metabasalt, constitute a bimodal magmatism in a continental extension setting. Their geochemical “arc magma” affinity is mainly inherited from Archean TTG rocks or attributed to crustal and/or continental lithospheric assimilation-contamination during mafic magma upwelling. Litho-tectonic assemblage (residual oceanic crust, subduction accretionary complexes, retroarc structures, large strike-slip faults, paired metamorphic belts, and spatiotemporal variations in magmatic activity) similar to that produced by modern-plate subduction has not been found in the Paleoproterozoic Jiao-Liao-Ji tectonic belt. The Longgang and Nangrim blocks share a coherent Archean basement and evolutionary history. The different metasedimentary strata in the “southern belt” and “northern belt” were deposited on a stable passive continental margin between 2.20 and 1.95 Ga. These strata share a similar provenance and underwent partial medium-pressure (MP)-high-pressure (HP) and high-temperature (HT)-ultrahigh-temperature (UHT) granulite-facies metamorphism with clockwise P-T paths involving isothermal decompression at ca. 1.95~ 1.80 Ga. Based on comprehensive geological and geophysical evidence, we propose the following tectonic model for the origin and geodynamic evolution of the Paleoproterozoic Jiao-Liao-Ji tectonic belt. ① Voluminous high-density granulite-eclogite facies residuals formed in the lower crust alongside the generation of extensive Archean TTGs in the Eastern block. The stable cratonic lithospheric mantle formed at the end of the Archean allowed these high-density granulite-eclogite facies residuals to be stably preserved in the lithosphere. ② During 2.2~2.0 Ga, intracontinental extension driven by upwelling of an asthenospheric hotspot along the Jiao-Liao-Ji belt fractured the Eastern block into the northern Longgang block and southern Nangrim block. ③ At ca. 1.95~1.85 Ga, the negative buoyancy of the high-density eclogitized lower crust and lithospheric mantle triggered their subduction (sinking), forcing convergent orogeny between the Longgang and Nangrim blocks along the Jiao-Liao-Ji belt. ④ At ca. 1.85~1.80 Ga, orogenic belt collapse caused by delamination of the orogenic root, followed by subsequent hot asthenospheric upwelling, resulted in the rapid exhumation and post-orogenic extension of the orogenic belt.
关键词
华北克拉通 ； 胶-辽-吉古元古代构造带 ； 重力驱动的板块汇聚造山 ； 大陆伸展 ； 胶北地体
