2017, Vol. 33
2. 合肥工业大学资源与环境工程学院, 合肥 230009
2. School of Resources and Environmental Engineering, Hefei University of Technology, Hefei 230009, China
华北克拉通位于北部的中亚造山带和南部的秦岭-苏鲁-大别造山带之间，是我国最大和最古老的克拉通。华北克拉通形成于太古宙-古元古代，并在显生宙白垩纪时期经历了强烈破坏，其地质演化一直是国内外地质学界的研究热点 (Zhao et al., 2001; Zhai et al., 2002; Kusky et al., 2007a, b; Kusky, 2011; Zhai and Santosh, 2011; Zhao and Cawood, 2012; Zhao and Guo, 2012; Zheng et al., 2013)。虽然有学者认为华北不同陆块之间的拼贴在太古宙即已完成 (Kusky et al., 2001; Kusky and Li, 2003)，但不断积累的大量高精度年代学数据表明，华北克拉通形成过程中的地体拼贴主要发生于古元古代 (Zhao et al., 2012)。
近十年来，有关华北克拉通最重要的研究成果就是在其中识别出三条古元古代造山带 (图 1a)：中部造山带将华北克拉通分为东部陆块和西部陆块，胶辽吉带将东部陆块进一步划分为龙岗陆块和狼林陆块，孔兹岩带将西部陆块进一步分为阴山陆块和鄂尔多斯陆块 (Zhao et al., 2005; Zhao and Zhai, 2013)。国内外学者已对中部造山带和孔兹岩带进行了大量研究 (Kröner et al., 2005; Faure et al., 2007; Wang, 2009; Li et al., 2010; Santosh, 2010; Santosh et al., 2012; Trap et al., 2012; Zhang et al., 2012)。而相比之下，作为我国古元古代岩石出露较为完整的胶辽吉带则研究相对滞后，对于其中产出的具有条带状、片麻状特征的被称为条痕状花岗岩 (辽吉花岗岩) 的古元古代二长花岗片麻岩 (张秋生, 1988)，学术界对其来源、成因、类型及构造环境等一直争论不休。关于条痕状花岗岩的来源及类型，刘光启 (1989)将该花岗岩识别为层状混合岩，认为其不是岩浆型的，而是重熔岩浆型的，原岩是沉积变质岩，赵凤顺和胡平 (1989)以及曲洪祥等 (2000)认为该花岗岩以火山-沉积岩重熔型的S型花岗岩为主。路孝平等 (2004b)以及郝德峰等 (2004)认为该花岗岩为A型花岗岩，杨明春等 (2015a)则认为该花岗岩属于I型花岗岩。在成因和构造环境方面，条痕状花岗岩最初被认为形成于元古宙早期的一种特殊的优地槽-坳拉槽环境中 (张秋生和李守义, 1985; Sun et al., 1993)。刘永江和李三忠 (1996)、陈树良等 (2000)以及郝德峰等 (2004)认为该花岗岩形成于裂谷环境中；刘俊来等 (2002)认为其形成于褶皱带早期阶段演化的伸展作用过程中；路孝平等 (2004b)认为条痕状花岗岩是辽吉地区古元古代地层沉积的基底岩石, 是地层沉积之前地壳拉张作用的结果, 属于一种非造山型花岗岩；杨明春等 (2015a)认为该花岗岩形成于下地壳来源的酸性岩浆和富集地幔来源的基性岩浆的混合，属于钙碱性弧岩浆。
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图 1 华北克拉通构造划分图 (a, 据Zhao et al., 2005) 和辽吉地区地质简图 (b, 据辽宁省地质矿产局, 1989; Wu et al., 2005修改) Fig. 1 Tectonic subdivision of the North China Craton (a, modified after Zhao et al., 2005) and geological sketch map of the Liaoji Belt (b, modified after BGMRL, 1989; Wu et al., 2005) |
花岗质岩石是早期地壳演化的重要记录者，花岗岩中蕴含着有关大陆形成与演化的丰富信息，上述有关条痕状花岗岩 (二长花岗片麻岩) 的争议严重制约了对区域构造演化的深入认识。作为辽吉带内的主要组成岩石之一，古元古代条痕状花岗岩经历了辽吉带形成与演化的整个过程，并在持续的地质演化过程中经历了强烈变形而形成明显的片麻状构造。因此，对该花岗岩进行岩石学、地球化学和成因学研究，可以解决上述争议，还原辽吉地区古元古代地质演化的整个过程，并进一步深入探讨华北克拉通早前寒武纪构造样式。鉴于此，本文选择胶辽吉带主要地质要素之一的条痕状花岗岩，对其进行详细的岩石学、地球化学和成因学研究，以期进一步深入探讨胶辽吉带北部辽吉地区的早前寒武纪地质演化。
2 地质背景和样品胶辽吉带呈北东-南西向展布于华北克拉通东部，介于龙岗陆块和狼林陆块之间，其展布范围包括北部的辽吉地区 (辽吉带) 和南部的胶北地区 (胶北地体)，辽东在古元古代地质构造划分上即属于辽吉地区。辽吉地区古元古代岩石组合主要包括变质火山-沉积岩、花岗岩和镁铁质侵入体 (图 1b)，其中变质火山-沉积岩被划分为北侧的老岭群和北辽河群以及南侧的集安群和南辽河群 (贺高品和叶慧文, 1998)。老岭群和北辽河群由透闪变粒岩、钠长浅粒岩、变质石英砂岩、硅质条带大理岩、白云石大理岩、十字石榴二云片岩和千枚岩等组成，原岩为陆源碎屑岩-碳酸盐岩建造 (路孝平等, 2005)。集安群和南辽河群由透辉变粒岩、蛇纹石化大理岩、斜长角闪岩、石墨大理岩、细粒黑云片麻岩、石榴夕线片麻岩等组成，原岩为火山岩-陆源碎屑岩-碳酸盐岩建造，以含有较多的变质火山岩区别于老岭群和北辽河群。近年来，随着分析测试技术的不断提高，不同学者获得了许多辽吉地区不同种类岩石的高精度U-Pb年代学资料。研究表明，上述辽吉带内火山-沉积岩形成于2.1~2.0Ga，并于1.9~1.88Ga发生变质作用 (Luo et al., 2004, 2008; Lu et al., 2006; Wan et al., 2006; 于介江等, 2007; 王惠初等, 2011; Xie et al., 2011; Meng et al., 2013a, 2014; 孟恩等, 2013; Li and Chen, 2014; 秦亚等, 2014; Hu et al., 2015; 李壮等, 2015; Li et al., 2015; 王惠初等, 2015)。
辽吉带内古元古代花岗质岩浆作用分为两期：条痕状花岗岩形成于2.2~2.1Ga (路孝平等, 2004b; Li and Zhao, 2007; 胡古月等, 2014; 杨明春等, 2015a)，斑状花岗岩和碱性正长岩侵位于1.88~1.85Ga (蔡剑辉等, 2002; 路孝平等, 2004a, 2005; 杨进辉等, 2007; 杨明春等, 2015b)。条痕状花岗岩总是出现在辽河群或集安群的底部或是大型褶皱的核部 (路孝平等, 2004b)，与周围古元古代火山-沉积岩呈构造接触 (图 2a)，均经历了强烈的变形作用 (图 2b)。辽吉地区古元古代镁铁质侵入体亦分为2.1Ga和1.8Ga两期，但与火山-沉积岩和花岗岩相比出露较少，且多以岩墙岩脉形式产出 (Yuan et al., 2015)。
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图 2 条痕状花岗岩野外照片与显微照片 Qtz-石英；Pl-斜长石；Kfs-钾长石；Pth-条纹长石；Mc-微斜长石 Fig. 2 Field photographs and photomicrographs of the monzogranitic gneisses Qtz-quartz; Pl-plagioclase; Kfs-potassium feldspar; Pth-perthite; Mc-microcline |
本文所研究的鸡冠山岩体和老黑山岩体均为胶辽吉带辽吉地区古元古代条痕状花岗岩，前人通过SHRIMP U-Pb锆石年代学研究获得两岩体年龄分别为2175±13Ma和2166±14Ma (Li and Zhao, 2007)。鸡冠山岩体呈浅肉红色，细粒花岗变晶结构，片麻状构造。主要矿物组成为石英 (35%)+斜长石 (15%~20%)+条纹长石 (15%~20%)+钾长石 (10%~15%)+磁铁矿 (3%)+角闪石 (1%~3%)，副矿物主要有榍石和锆石。石英他形粒状，大都呈集合体排布，具有拉长和波状消光现象。斜长石呈短柱状，发育聚片双晶，有些已发生明显的弯曲变形 (图 2c)，部分绢云母化黝帘石化。由于后期变形强烈，大部分矿物均有破碎。老黑山岩体呈粉灰色，中粗粒花岗变晶结构，片麻状构造。主要矿物组成为石英 (25%~30%)+条纹长石 (25%~30%)+斜长石 (10%~15%)+微斜长石 (5%~10%)+钾长石 (5%)+磁铁矿 (5%)+角闪石 (3%~5%)，副矿物有锆石、榍石、独居石、褐帘石等。石英他形粒状，溶蚀长石形成港湾，有的被拉长形成断续的条带。斜长石具有明显的聚片双晶，微斜长石发育格子双晶 (图 2d)。角闪石呈黄绿色，不规则柱粒状，有的蚀变为黑云母和绿泥石。
3 分析方法全岩主量和微量元素分析在中国地质科学院国家地质实验测试中心完成。主量元素分析在3080E型荧光光谱仪 (XRF) 上进行，分析精度优于5%。微量元素在等离子质谱仪 (ICP-MS) 上测定，含量大于10×10-6的元素，分析误差为5%；含量小于10×10-6的元素，分析误差为10%。全岩Sm-Nd同位素的化学分离在北京大学造山带与地壳演化教育部重点实验室同位素分离超净实验室内完成，通过阳离子交换柱法分离和纯化。同位素测试在中国地质调查局天津地质调查中心同位素实验室利用Triton热电离质谱仪 (TIMS) 完成，Nd含量由同位素稀释法获得，分析误差小于0.5%。
4 分析结果样品的主量和微量元素分析结果见表 1。结果显示，辽吉地区鸡冠山岩体和老黑山岩体成分均匀，具有一致的地球化学特征。岩体主要成分包括SiO2(72.15%~74.52%)、Al2O3(12.26%~12.97%)、K2O (4.02%~5.75%)、Na2O (3.22%~4.03%)、Fe2O3(1.48%~2.04%)、FeO (1.06%~2.07%)、CaO (0.71%~1.99%)、TiO2(0.25%~0.33%)、MgO (0.12%~0.28%)、MnO (0.03%~0.06%) 和P2O5(0.02%~0.06%)。样品K2O/Na2O比值大于1(1.00%~1.73%)，属于富钾质岩石，样品全碱 (K2O+Na2O) 含量变化于7.97%~9.08%。在SiO2-Na2O+K2O图中，辽吉条痕状花岗岩位于钙碱性花岗岩区域内 (图 3a)，在SiO2-K2O图中，条痕状花岗岩主要位于高钾钙碱系列区域 (图 3b)。样品具有高的FeOT/(FeOT+MgO) 比值，绝大多数为含铁量较高的铁质花岗岩 (图 3c)。样品铝指数ASI (A/CNK=分子数Al2O3/(CaO+Na2O+K2O)) 介于0.84~1.03之间，A/NK值为1.11~1.17，在A/CNK-A/NK图解中落入准铝质和过铝质区域 (图 3d)。
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表 1 条痕状花岗岩的主量元素 (wt%) 和微量元素 (×10-6) 分析结果 Table 1 Major (wt%) and trace (×10-6) element data for the monzogranitic gneisses |
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图 3 条痕状花岗岩的SiO2-Na2O+K2O (a, 据Middlemost, 1994)、K2O-SiO2(b, 据Peccerillo and Taylor, 1976)、SiO2-FeOT/(FeOT+MgO)(c, 据Frost et al., 2001) 和A/CNK-A/NK (d, 据Maniar and Piccoli, 1989) 图解 Fig. 3 SiO2 vs. Na2O+K2O (a, after Middlemost, 1994), K2O vs. SiO2 (b, after Peccerillo and Taylor, 1976), SiO2 vs. FeOT/(FeOT+MgO) (c, after Frost et al., 2001) and A/CNK vs. A/NK (d, after Maniar and Piccoli, 1989) diagrams for the monzogranitic gneisses |
样品稀土元素含量较高 (∑REE=202.7×10-6~668.9×10-6)，轻重稀土分馏较为明显，其 (La/Sm)N=1.94~5.73，(La/Yb)N=4.80~20.6，具有弱的铕负异常。样品稀土配分曲线中，轻稀土元素富集，呈右倾模式，重稀土元素呈平坦分布模式 (图 4a)。微量元素特征显示样品具有高的Zr (256×10-6~384×10-6)、Th (5.94×10-6~42.40×10-6)、La (31.2×10-6~158.0×10-6)、Ce (72.8×10-6~297.0×10-6)、Y (43.2×10-6~54.8×10-6) 含量，非常低的Nb (14.0×10-6~22.2×10-6)、Ta (1.15×10-6~1.56×10-6)、Sr (71.8×10-6~104×10-6)、Sc (3.81×10-6~7.46×10-6)、Cr (0.89×10-6~2.21×10-6)、Co (0.66×10-6~1.54×10-6)、Ni (0.35×10-6~1.13×10-6) 含量。
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图 4 条痕状花岗岩的球粒陨石标准化稀土元素配分图解 (a) 和原始地幔标准化微量元素蛛网图 (b)(标准化值据Sun and McDonough, 1989) Fig. 4 Chondrite-normalized REE patterns (a) and primitive mantle-normalized trace elements patterns (b) for the monzogranitic gneisses (normalizing values after Sun and McDonough, 1989) |
样品的Sm-Nd同位素分析结果见表 2。样品Sm含量为8.62×10-6~13.20×10-6，Nd含量为37.6×10-6~72.9×10-6，初始143Nd/144Nd变化于0.511226~0.511657之间，fSm/Nd变化于-0.44~-0.30之间。全岩Nd模式年龄根据DePaolo (1981)的计算方法计算获得，结果显示样品的εNd(t) 值为-3.3~-0.9，两阶段模式年龄tDM2=2860~2669Ma (岩体U-Pb年龄根据Li and Zhao, 2007)。
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表 2 条痕状花岗岩的Nd同位素组成及计算参数 Table 2 Whole rock Nd isotopic composition and calculation parameters of the monzogranitic gneisses |
长期以来，许多关于辽吉地区地质演化的争论都来源于对花岗岩和周围火山-沉积岩之间关系的不同理解。以往的地质观察表明，条痕状花岗岩总是出现在辽河群或集安群等火山-沉积岩的底部或大型褶皱构造的核部，但局部又可见其见其侵入于上述火山-沉积岩之中，从而有花岗岩在元古宙“重就位”之说 (张秋生, 1988)。在野外，条痕状花岗岩同周围的火山-沉积岩呈明显的构造接触关系 (图 2a)，表明两者是通过后来的构造作用混合拼贴在一起的，仅仅依据野外产状很难判断两者形成的先后顺序。所以，进一步明确花岗岩和火山-沉积岩的关系需要借助于两者的年代学研究。
虽然早期曾有学者认为火山-沉积岩的形成早于花岗岩侵位时间 (张秋生, 1988)，但近年来高精度的SHRIMP和LA-ICP-MS锆石U-Pb年代学分析表明，这一结论是不成立的 (Luo et al., 2004; Li and Zhao, 2007; Li and Chen, 2014)。通过仔细观察可以发现，南、北辽河群、集安群和老岭群等火山-沉积岩可以进一步划分为火山岩组分和沉积岩组分，两者在成因来源方面明显不同。虽然沉积岩的沉积时限被限定在2.1~1.9Ga，但其中碎屑锆石年龄从晚太古代变化至古元古代，并具有~2.1Ga和~2.5Ga两个峰值 (Luo et al., 2008)。相比之下，火山岩组分的形成时代为2.2~2.1Ga，只有极少量的~2.5Ga的继承锆石年龄 (Lu et al., 2006; Li and Chen, 2014; Meng et al., 2014)。因此，2.2~2.1Ga侵位的条痕状花岗岩与火山-沉积岩中的火山岩组分是同时代的，但老于火山-沉积岩中沉积岩组分的沉积时限。换言之，花岗岩和上述火山岩组分代表古元古代岩浆活动，而火山-沉积岩中的沉积岩组分，一部分来源于古元古代岩浆岩的风化剥蚀，另一部分则来源于太古宙基底。
在讨论花岗岩与火山-沉积岩关系时必须要提及的是，南、北辽河群、集安群和老岭群等古元古代地层命名的客观性与真实性仍需要进一步探讨。长期以来，上述辽吉地区古元古代火山-沉积岩被当做地层来命名和处理，但近年来大量的年代学研究对上述地层的存在与命名提出了质疑。例如，就沉积时限而言，辽河群最底部的浪子山组比覆盖在其上的包括盖县组在内的辽河群其它地层均要年轻，并且群内各组一级地层的定年结果表现为全然无序，与原有自下而上各组地层时代逐渐变年轻的命名顺序完全无法对应并互为矛盾 (Luo et al., 2004; Wan et al., 2006)。因此，辽河群的原有沉积序列已被后期构造运动所强烈改造。
5.2 条痕状花岗岩成因类型及源区性质条痕状花岗岩具有低的CaO、MgO、Sc、Cr、Co、Ni、Sr、Eu含量，高的K2O/Na2O、FeOT/MgO、Ga/Al比值和Ga、Zr、Y含量等与A型花岗岩相一致的地球化学特征。条痕状花岗岩10000Ga/Al比值大于2.6，在Whalen et al. (1987)提出的判别图解中，绝大多数条痕状花岗岩都投影在A型花岗岩区域 (图 5)。Frost et al. (2001)进一步明确了铁含量在判别A型花岗岩中的作用，即在SiO2-FeOT/(FeOT+MgO) 图解中，位于铁质/镁质分界线之上及附近的花岗岩属于A型花岗岩。如图 3c所示，在SiO2-FeOT/(FeOT+MgO) 图中，除少数投影点分布在铁质/镁质分界线之下以外，绝大多数条痕状花岗岩均位于铁质/镁质分界线之上，即为A型花岗岩。本文样品以较高的Na2O (3.22%~4.03%) 和较低的P2O5含量 (0.02%~0.06%) 区别于高分异的S型花岗岩 (Na2O均值2.81%，P2O5均值0.02%)，以高的形成温度 (813~867℃)、FeOT含量 (2.52%~3.55%) 和低的Rb含量 (106×10-6~171×10-6) 区别于高分异的I型花岗岩 (温度均值764℃，FeOT含量一般小于1.00%，Rb含量大于270×10-6)(King et al., 1997; 贾小辉等, 2009)。样品较高的Zr丰度 (256×10-6~384×10-6) 也是其区别于I型花岗岩的重要特征。
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图 5 条痕状花岗岩成因类型判别 (据Whalen et al., 1987) Fig. 5 Genetic type discrimination of the monzogranitic gneisses (after Whalen et al., 1987) |
关于A型花岗岩的来源，一般认为其可以由地壳物质部分熔融形成，也可以是幔源碱性玄武质岩浆分离结晶作用的产物 (Loiselle and Wones, 1979; Eby, 1990; Frost et al., 2007; Dall’Agnol et al., 2012)。本文样品具有较高的SiO2(72.15%~74.52%) 和K2O (4.02%~5.75%)，MgO (0.12%~0.28%)、Cr (0.89×10-6~2.21×10-6)、Ni (0.35×10-6~1.13×10-6) 含量极低，表明其为壳源岩浆。Collins et al. (1982)曾提出过熔融出花岗岩之后的残余长英质麻粒岩相下地壳作为A型花岗岩的源区，但这一模式被后来的岩石学实验所推翻：A型花岗岩最有可能源自英云闪长质-花岗闪长质地壳岩石15%~40%程度的部分熔融 (Creaser et al., 1991)。进一步的实验岩石学研究表明，铝质A型花岗岩形成于钙碱性花岗质岩石在低压 ( < 4kbar) 条件下的脱水部分熔融 (Patiño Douce, 1997)。辽吉条痕状花岗岩属于亚碱性花岗岩 (图 3a)，在A/CNK-A/NK图解中落入准铝质和过铝质区域 (图 3d)，是典型的铝质A型花岗岩，而不是碱性花岗岩。King et al. (1997)指出，铝质A型花岗岩和碱性A型花岗岩具有不同的地球化学特征及成因，碱性A型花岗岩是幔源碱性镁铁质岩浆分离结晶作用的产物，而铝质A型花岗岩则源于具有正常水含量的长英质地壳的部分熔融。澳大利亚拉克兰造山带内的铝质A型花岗岩即为长英质地壳在高温条件下部分熔融的产物 (King et al., 1997)。本文样品具有高的Yb (4.21×10-6~5.56×10-6)、Y (43.2×10-6~54.8×10-6) 含量，低的 (La/Yb)N和相对平坦的重稀土分布模式 (图 4a)，反映其源自无石榴石残留相的熔融源区。Eu负异常和强烈亏损的Sr元素 (图 4b) 暗示条痕状花岗岩源区较浅 ( < 30km)，处于斜长石稳定域内。辽吉条痕状花岗岩εNd(t) 值介于-8.63~+2.32(本文数据; 郝德峰等, 2004; 杨明春等, 2015a)，tDM为2860~2669Ma (杨明春等, 2015a)，大于岩石形成年龄，暗示条痕状花岗岩源区主要为太古宙基底，混有少量古元古代新生地壳 (图 6)。因此，条痕状花岗岩形成于低压条件下长英质太古宙地壳的脱水部分熔融。
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图 6 条痕状花岗岩的εNd-t图解 Fig. 6 Diagram of εNd vs. t for the monzogranitic gneisses |
King et al. (1997)在研究澳大利亚拉克兰造山带时明确指出，A型花岗岩可以形成于威尔逊旋回的各个阶段。在总结前人大量工作的基础上，Bonin(2007) 同样认为，A型花岗岩可以产于包括活动陆缘、被动陆缘、克拉通、裂谷等在内的各种构造环境中。本文样品富集Rb、U、K等大离子亲石元素和轻稀土元素，亏损Nb、Ta、Ti等高场强元素，具有明显的俯冲带岩浆特征 (Floyd and Winchester, 1975; Pearce, 1982; Briqueu et al., 1984)。条痕状花岗岩在Rb/30-Hf-Ta×3图中落入火山弧区域 (图 7a)，在Y+Nb-Rb图解中落入火山弧花岗岩以及火山弧花岗岩和板内花岗岩之间的过渡区域 (图 7b)。Eby (1992)将A型花岗岩分为A1型和A2型两个亚类，A1型花岗岩具有与洋岛玄武岩相类似的地球化学特征，A2型花岗岩则具有明显的岛弧岩浆特征。在Y/Nb-Rb/Nb和Nb-Y-Ce图解中 (图 7c, d)，辽吉条痕状花岗岩均落入A2型花岗岩区域，其Y相对于Nb更富集，具有与岛弧玄武岩相似的Y/Nb等元素比值，与辽吉带内同期变质基性岩一样，均显示俯冲成因 (王惠初等, 2011; Li and Chen, 2014; Meng et al., 2014; Yuan et al., 2015)。本文样品的Nb/Ta (11.34~14.88) 比值介于地壳Nb/Ta (11~12) 和地幔Nb/Ta (≈17.5) 之间，反映其源区受到了来自俯冲带交代地幔的流体的影响 (Green, 1995)。
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图 7 条痕状花岗岩的Rb-Hf-Ta (a, 据Harris et al., 1986)、Y+Nb-Rb (b, 据Pearce et al., 1984)、Y/Nb-Rb/Nb (c, 据Eby, 1992) 和Nb-Y-Ce (d, 据Eby, 1992) 判别图 VAG-火山弧花岗岩；syn-COLG-同碰撞花岗岩；WPG-板内花岗岩；ORG-洋中脊花岗岩 Fig. 7 Discriminations of Rb-Hf-Ta (a, after Harris et al., 1986), Y+Nb vs. Rb (b, after Pearce et al., 1984), Y/Nb vs. Rb/Nb (c, after Eby, 1992) and Nb-Y-Ce (d, after Eby, 1992) for the monzogranitic gneisses VAG-volcanic arc granitoids; syn-COLG-syn-collisional granitoids; WPG-within plate granitoids; ORG-ocean ridge granitoids |
关于辽吉地区古元古代构造演化的学术观点大致可以分为裂谷和岛弧两种。裂谷观点认为华北克拉通东部陆块在太古宙时为一整体，在古元古代早期经历了裂谷作用而形成洋盆，将东部陆块分裂为北部的龙岗陆块和南部的狼林陆块，其后伴随着洋盆的消减闭合，最终裂谷消失，龙岗陆块和狼林陆块又重新拼合 (陈荣度, 1984; 张秋生, 1984; 刘永江和李三忠, 1996; Luo et al., 2004; Li et al., 2005; Lan et al., 2015; Peng et al., 2016)。这一裂谷张开并闭合观点着重阐述的是，龙岗陆块和狼林陆块在太古宙时本来是一整体，正是由于古元古代的裂谷作用才产生了辽吉活动带，辽吉带的演化经历了一个从大陆拉张形成洋盆到大洋俯冲消减陆块重新拼合的完整的威尔逊旋回，裂谷作用是这一观点所强调的核心内容。而与裂谷张开并闭合观点相悖的是，另一些学者则认为龙岗陆块和狼林陆块之前并不在一起，两陆块无亲缘关系，只是由于大洋的消失才使得两陆块最终拼合在一起 (刘永达等, 1989; 白瑾等, 1993; Faure et al., 2004; Lu et al., 2006; Li and Chen, 2014; Meng et al., 2014)。这一观点强调俯冲作用在辽吉带形成过程中的重要作用及意义，并且龙岗陆块和狼林陆块在古元古代之前没有亲源性。
研究胶辽吉带古元古代构造演化时，首先必须要明确古元古代岩石的分布范围。长期以来，胶辽吉带以外的两侧区域分别被称为龙岗陆块和狼林陆块 (Zhao et al., 2005)。太古宙龙岗陆块早已被吉南和辽北地区出露的具有太古宙年龄的TTG片麻岩所确定 (Liu et al., 1992; Song et al., 1996; Wan et al., 2005, 2012; Wu et al., 2008, 2016; Grant et al., 2009; Guo et al., 2015; Zhu et al., 2015)，但狼林陆块的命名及分布范围却值得怀疑 (图 1a)。狼林陆块的命名是依据出露于朝鲜的狼林群，但迄今为止，在狼林群中仍未发现具有确定太古宙年龄的TTG片麻岩，而且在狼林群中所获得的最老的年龄也只有1.9Ga，那些在野外看似TTG片麻岩的岩石实际上形成于古元古代晚期而并非太古宙 (Zhao et al., 2006)。换言之，临津江带以北的所谓的太古宙狼林群实际上是形成于古元古代晚期的岩石地层单位，胶辽吉带的真实展布范围比现在所认为的要大，狼林群很有可能也是胶辽吉带的一部分。事实上，在胶辽吉带以外的东南侧的辽东半岛地区，太古宙基底仅仅局限于最东南端的金州-庄河一带 (路孝平等, 2004a; Wu et al., 2005; Meng et al., 2013b)。但是在以往的研究中，由于缺乏高精度年代学的限定，太古宙基底的分布范围经常被过于夸大，而这一问题在地质学研究中是非常普遍的：许多岩石在野外看上去像是TTG片麻岩，但年代学研究表明它们形成于元古宙甚至显生宙。
胶辽吉带从朝鲜经中国东北延伸至山东半岛，在中国境内包括了北部的辽吉地区 (辽吉带) 和南部的胶北地区 (胶北地体)。然而，虽然胶北地区和辽吉地区同属胶辽吉带，但两地区的岩石构造组成却明显不同：胶北地体出露有大量的太古宙TTG片麻岩和夹杂于其中的新太古代-古元古代高压麻粒岩 (Zhou et al., 2004, 2008a, b; Tang et al., 2007; Tam et al., 2011, 2012a, b, c; Liu et al., 2012, 2013a, b, 2015; Wan et al., 2014; Wang et al., 2014; Wu et al., 2014a, b; Xie et al., 2014; Shan et al., 2015a, b; Zhao et al., 2015)，并在此过程中发生了强烈的混合岩化作用 (Liu et al., 2014)；而辽吉带则主要由古元古代火山-沉积岩和其中的侵入岩组成 (Luo et al., 2004, 2008; Lu et al., 2006; Wan et al., 2006; Li and Zhao, 2007; Li and Chen, 2014; Meng et al., 2014; Li et al., 2015; Yuan et al., 2015)，很少有太古宙灰色片麻岩出露，并且直到最近才发现有少量高压麻粒岩 (刘福来等, 2015)。因此，辽吉带和胶北地体古元古代期间的构造演化必然存在差异。
在研究辽吉带构造演化时必须要指出并强调的是，仅仅依据南辽河群和北辽河群是否具有相似的年龄和同位素特征，并不能判断南、北辽河群是形成于裂谷环境还是岛弧环境。在辽吉带，辽宁省内的南辽河群和北辽河群的主要差异即在于，南辽河群主要由火山碎屑岩构成，具有逆时针的变质P-T轨迹，而北辽河群则主要是陆源碎屑岩，具有顺时针的P-T轨迹，并且在吉林省，南部集安群与北部老岭群的差别也同样如此 (贺高品和叶慧文, 1998; Wan et al., 2006)。此外，东南部集安群和南辽河群内卷入的古元古代侵入岩也明显多于西北部的老岭群和北辽河群。上述岩石构造组合的空间分布最符合板块构造体制下的大陆弧后盆地环境 (Şengör, 1990; Condie, 1997)：东南部的集安群和南辽河群靠近俯冲带海沟一侧，西北部的老岭群和北辽河群靠近内陆一侧，来自火山弧一侧的火山碎屑岩、侵入岩和来自内陆一侧的陆源碎屑岩共同充填了辽吉带这一古元古代弧后盆地。辽吉带的弧后盆地属性也得到了前人对区域内同期变质基性岩 (包括基性火山岩和侵入岩) 的相关研究的支持 (王惠初等, 2011; Meng et al., 2014)。然而，之前关于裂谷和岛弧的争论却往往是在讨论辽吉带本身是否标志着消失了的大洋 (缝合带)(Faure et al., 2004; Luo et al., 2004, 2008; Li et al., 2005, 2006, 2011; Lu et al., 2006; Li and Zhao, 2007; Li and Chen, 2014; Yuan et al., 2015)。而实际上发生俯冲的洋壳远在东部陆块以东南 (朝鲜半岛以东南，根据现今相对位置)，并不位于辽吉带：古元古代时期东部陆块东侧的岩浆弧大致位于朝鲜半岛，即朝鲜岛弧，辽吉带处于朝鲜岛弧 (大陆边缘弧) 的弧后区域 (Peng et al., 2014)。由于集安群、老岭群、南辽河群和北辽河群均为海相沉积 (张秋生, 1988)，所以，辽吉弧后盆地在古元古代时位于海平面以下，但大陆弧后辽吉地区的伸展作用是否足够强大以致拉张出弧后洋壳，仍需进一步深入研究。
如图 8所示，古元古代早期 (2.22.1Ga)，东部陆块以东的大洋岩石圈板块向西北方向俯冲于东部陆块之下 (Peng et al., 2014)，洋壳的持续俯冲与后撤导致弧后不断伸展，进而在大陆岛弧后侧产生2.2~2.1Ga期间的辽吉弧后盆地，弧后伸展作用促发了由条痕状花岗岩和变质基性岩构成的双峰式岩浆活动，大陆边缘弧 (朝鲜弧) 一侧的火山碎屑岩和内陆一侧的陆源碎屑岩分别从两侧经搬运沉积在辽吉弧后盆地中，最终形成了以火山碎屑岩为主的南辽河-集安群和以陆源碎屑岩为主的北辽河-老岭群。俯冲作用导致洋壳及其上覆沉积物脱水，产生的流体向上运移并交代地幔楔，使地幔楔发生部分熔融，幔源岩浆随后上升并加热地壳，使太古宙-古元古代长英质地壳在高温低压低氧逸度条件下发生脱水部分熔融，产生了辽吉地区古元古代条痕状花岗岩。在后期的地体拼贴过程中，条痕状花岗岩与周围岩石共同变形并最终构造挤压在一起。
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图 8 古元古代早期 (2.2~2.1Ga) 辽吉地区构造环境示意图 Fig. 8 Schematic illustration showing tectonic environment of the Liaoji region during Early Paleoproterozoic (2.2~2.1Ga) |
(1) 辽东古元古代条痕状花岗岩为高钾钙碱性铝质A型花岗岩，具有高的K2O/Na2O、FeOT/MgO、Ga/Al比值和Ga、Zr、Y含量以及低的CaO、MgO、Sr、Cr、Co、Ni含量，形成于低压条件下长英质地壳的部分熔融。
(2) 条痕状花岗岩富集Rb、U、K等大离子亲石元素和轻稀土元素，亏损Nb、Ta、Ti等高场强元素，具有明显的俯冲带岩浆特征。
(3) 古元古代早期 (2.2~2.1Ga) 辽吉地区处于大陆弧后盆地构造环境，强烈的弧后伸展作用产生了A2型条痕状花岗岩。在后期的地体拼贴过程中，条痕状花岗岩与周围岩石共同变形并最终构造挤压在一起。
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