2021, Vol. 37
引用本文
张健, 李怀坤, 田辉, 刘欢, 周红英, 刘文刚. 2021. 华北克拉通燕辽裂谷长城纪碱性岩锆石U-Pb年代厘定和Hf-O同位素特征. 岩石学报, 37(1): 231-252, doi: 10.18654/1000-0569/2021.01.14
Zhang J, Li HK, Tian H, Liu H, Zhou HY and Liu WG. 2021. Zircon U-Pb dating and Hf-O isotope characteristics of Changchengian alkaline rocks from the Yanliao Rift in the North China Craton. Acta Petrologica Sinica, 37(1): 231-252(in Chinese with English abstract)
华北克拉通燕辽裂谷长城纪碱性岩锆石U-Pb年代厘定和Hf-O同位素特征
1. 中国地质调查局天津地质调查中心, 天津 300170;
2. 中国地质调查局前寒武纪地质研究中心, 天津 300170;
3. 中国地质调查局华北科技创新中心, 天津 300170
2. 中国地质调查局前寒武纪地质研究中心, 天津 300170;
3. 中国地质调查局华北科技创新中心, 天津 300170
摘要: 基性的碱性岩通常形成于伸展环境，具有富碱和不相容元素富集等地球化学特征，它们来源于深部富集地幔，是探索地幔交代和深部地球动力学的"岩石探针"。华北克拉通北缘燕辽裂谷内发育团山子组和大红峪组钾质火山岩以及侵入串岭沟组的钠质岩脉，它们共同组成了长城纪碱性岩系列。本文利用SHRIMP锆石U-Pb同位素方法对平谷-蓟县地区钾质火山岩进行年代学测试，获得误差范围内一致的年龄：1613±11Ma、1634±18Ma（团山子组）和1605±19Ma、1630±10Ma（大红峪组），说明钾质火山岩喷发的持续时间短，且与侵入串岭沟组的钠质岩脉同期（~1625Ma）。钾质火山岩和钠质岩脉的锆石Hf-O同位素组成相似：εHf（t）=-2~+4（正态分布峰值+0.6），δ18O=4.5‰~7.7‰明显高于正常地幔锆石的值，钾质火山岩和钠质岩脉的母岩浆源自相同的富集地幔，源区受到高δ18O物质的交代作用而富含钾质矿物，如角闪石或金云母。华北克拉通中-新元古代岩浆事件是伸展环境的产物，其锆石Hf同位素组成在~1.32Ga发生突变，由富集到亏损，暗示岩石圈地幔经历强烈的交代改造作用，可能成为检验地幔柱或者板块深俯冲驱动超大陆裂解机制的窗口。
关键词:
锆石 U-Pb年代学 Hf-O同位素 碱性岩 燕辽裂谷 长城纪
Zircon U-Pb dating and Hf-O isotope characteristics of Changchengian alkaline rocks from the Yanliao Rift in the North China Craton
1. Tianjin Centre, China Geological Survey, Tianjin 300170, China;
2. Precambrain Geological Research Centre, China Geological Survey, Tianjin 300170, China;
3. North China Center for Geoscience Innovation, China Geological Survey, Tianjin 300170, China
2. Precambrain Geological Research Centre, China Geological Survey, Tianjin 300170, China;
3. North China Center for Geoscience Innovation, China Geological Survey, Tianjin 300170, China
Abstract: Mafic alkaline rocks are geochemically enriched in alkali and incompatible elements and genetically related to extensional settings. They are derived from enriched mantle, and thus can decipher the mantle metasomatism and deep geodynamics. The Changchengian alkaline rocks, outcropped in the Yanliao Rift at northern margin of the North China Craton, include the potassium volcanic rocks of the Tuanshanzi and Dahongyu formations along with the sodium dike intruding into the Chuanlinggou Formation. SHRIMP zircon U-Pb isotope chronological dating of the volcanic rocks from Pinggu-Jixian area yield concordant ages of 1613±11Ma, 1634±18Ma (the Tuanshanzi Formation) and 1605±19Ma, 1630±10Ma (the Dahongyu Formation), respectively. All these consistent ages within analytical error indicate the potassic volcanics were short-lived eruption, broadly coeval with the ca. 1625Ma sodic dikes. The potassic volcanic rocks and sodic dikes display similar zircon Hf-O isotope compositions, i.e., εHf(t) ranging from -2 to +4 with a Gaussian distribution pattern peaking at +0.6, while δ18O ranges from 4.5‰ to 7.7‰ mostly higher than normal mantle zircon value. The potassic volcanic rocks and sodic dikes, composed of K-rich minerals such as hornblende or phlogopite, are originated from the common enrichment mantle which was previously metasomatized by elevated δ18O materials. The North China Craton underwent multi-rifting events during the Meso- and Neo-proterozoic, their zircon Hf isotopes abruptly shift from enrichment to depletion at ca. 1.32Ga, suggesting that the lithospheric mantle underwent strong metasomatism. The Mesoproterozoic mafic rocks in North China Craton can play a key role for testing the mechanism of supercontinental breakup driven by mantle plumes or/and deep plate subduction.
Key words:
Zircon U-Pb chronology Hf-O isotope Alkaline rock Yanliao rift Changchengian Period
中-新元古代(1.8~0.75Ga)被称作“地球的中年期(Earth's middle age)”或“无聊的十亿年(boring billion)”(Roberts，2013；Cawood and Hawkesworth, 2014；Zhai et al., 2015)，时间跨越两个超级大陆(Supercontinent)的演化阶段，即哥伦比亚(Columbia/Nuna)超大陆裂解和罗迪尼亚(Rodinia)超大陆聚合，是地质历史上承前启后的特殊时期。从“超大陆旋回”(Nance et al., 1988；Li et al., 2008；Hawkesworth et al., 2017)的角度观察，中-新元古代的全球构造环境相对稳定，并且得到一系列岩浆活动记录(如非造山的斜长岩、A型花岗岩涌现，Ashwal，2010；Condie，2020)和地球化学指标(大气氧浓度，Holland et al., 2006；海水Sr同位素，Shields，2007；碎屑锆石εHf(t)，Belousova et al., 2010)近无异常等的印证。
华北克拉通(North China Craton, NCC)充分参与到Columbia/Nuna超大陆的汇聚和裂解过程中(Condie，2002；Rogers and Santosh, 2002，2003；Wilde et al., 2002；Zhao et al., 2002a, 2004a；Zhai and Liu, 2003；Hou et al., 2008；Ernst et al., 2008；Zhai et al., 2015)，具有基底和盖层组成的典型双层结构。华北克拉通在中-新元古代属于裂谷盆地和沉积盖层的发育阶段，构造环境相对稳定，与“地球中年期”的特点一致。古元古代晚期(~1.85Ga)，经历吕梁运动(中条运动)的变质造山事件，将几个太古宙和古元古代花岗岩-绿岩带及高级区域变质带(2.0~1.85Ga)拼贴形成一个规模较大的基底陆块(图 1a，Zhao et al., 2001, 2005, 2011, 2012；Guo et al., 2002；Lu et al., 2002, 2008；Zhai and Liu, 2003；Kusky and Li, 2003；Kröner et al., 2005；Zhai et al., 2005；Santosh，2010；Zhai and Santosh, 2011；Santosh et al., 2012)。~1.8Ga之后，华北克拉通构造机制由碰撞挤压向拉张伸展转换(Meng et al., 2011)，东北缘的燕辽、西南缘的豫陕和西北缘的渣尔泰-白云鄂博三大裂谷系统逐渐形成。裂谷内部的盖层沉积厚度巨大、出露广泛，未经历明显的变质作用。
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图 1 华北克拉通前寒武纪构造简图(a，据Zhao et al., 2005；Santosh，2010)、华北克拉通北缘燕辽裂谷中-新元古界分布略图(b，据黄学光等，2000①)和平谷-蓟县地区长城系火山岩分布图(c) Fig. 1 Precambrian tectonic sketch map of the North China Craton (a, after Zhao et al., 2005; Santosh, 2010), sketch map showing the distribution of the Meso-Neoproterozoic strata in the Yanliao Rift, northern North China Craton (b) and Changchengian volcanic rock distribution in Pinggu-Jixian area (c) |
截止目前，围绕燕辽裂谷(图 1b，蓟县剖面)的研究工作最为深入，主要体现在早期生命起源和演化(Zhu and Chen, 1995；Xiao et al., 1997；Peng et al., 2009；Zhu et al., 2016；Ma et al., 2017；Shi et al., 2017a, b；Yang et al., 2017；Qu et al., 2018；Miao et al., 2019)、古沉积环境(Li et al., 2003；Chu et al., 2007；Luo et al., 2014；Guo et al., 2015；Zhang et al., 2015, 2018a；Ding et al., 2017；Tang et al., 2017; Canfield et al., 2018；Shang et al., 2019)、古地磁与古大陆恢复重建(Pei et al., 2006；Zhang et al., 2006, 2012a, 2018b；Chen et al., 2013a；Xu et al., 2014；Cai et al., 2020；Zhao et al., 2020)等方面。上述令人瞩目的进展得益于地层格架的搭建和时间序列的精确厘定。
大红峪组和团山子组的碱性火山岩位于燕辽裂谷长城系地层上部，可能是裂谷系统内唯一的火山熔岩单元，也是最早实现锆石U-Pb定年对地层时代精确约束的测年对象，获得TIMS单颗粒锆石U-Pb年龄1625.3±6.2Ma(蓟县大红峪组，陆松年和李惠民，1991)和1683±67Ma(平谷团山子组，李怀坤等，1995)，由此奠定地层对比的基础。更为关键的是，侵入串岭沟组基性岩脉与火山岩同时期(张健等，2015)，虽然二者均以碱性OIB为主要的地球化学特征，但是K2O和Na2O组成存在明显区别。基性岩脉为钠质，而火山岩高钾低钠，K2O的富集程度高达~15%(K2O/Na2O≈1400，Wang et al., 2015a)，因此，钾质和钠质岩石成因的对比研究需要更细致的工作。
随着测试技术的进步和研究区域的扩大，火山岩和岩脉的锆石原位U-Pb定年结果被纷纷报道(Lu et al., 2008；高林志等，2008；张拴宏等，2013；Wang et al., 2015a；张健等，2015)。虽然年龄结果多集中在1.62~1.63Ga范围(详细内容见讨论部分)，但是Wang et al.(2015a)测得团山子组粗面玄武岩和大红峪组粗面安山岩分别为1671±5Ma和1664±6Ma，大部分>1.65Ga的测年结果明显偏老，并与下覆地层串岭沟组凝灰岩年龄1621±6.9Ma和1634.8±6.9Ma(孙会一等，2013；刘典波等，2019)以及依据综合资料推测的长城系底界年龄~1650Ma(李怀坤等，2011；Li et al., 2013；王泽九等，2014；周红英等，2020)相矛盾。火山岩年龄不仅对地层锚点的标定至关重要，而且深刻影响着岩浆过程以及时空演化规律的解释。
基性的碱性岩通常形成于伸展环境，具有富碱和富不相容元素等地球化学特征，来源于深部富集地幔，是探索地幔交代和深部地球动力学的“岩石探针”。本文首先系统采集平谷-蓟县地区长城系团山子组和大红峪组火山熔岩样品，使其达到空间范围的全面覆盖；然后利用SHRIMP锆石U-Pb同位素方法进行系统年代学再研究，进一步廓清燕辽裂谷长城纪碱性岩的形成时代；再通过锆石Hf-O同位素特征，示踪火山岩和基性岩脉的岩石成因和源区类型；最后结合华北克拉通在中-新元古代岩浆事件Hf同位素的成果资料，探讨Columbia/Nuna超大陆裂解过程中岩石圈演化形式。
① 黄学光、朱士兴、贺玉贞等.2000.承德地区中、上元古界层序地层学研究(科研报告，未出版)
1 区域地质背景研究区位于华北克拉通东北缘燕辽裂谷内平谷-蓟县一带(图 1c)，盖层沉积不整合覆盖于新太古代迁西群(密云群)混合岩化的片麻岩、角闪岩、麻粒岩等高级变质杂岩之上。裂谷系统里的“蓟县中-上元古界剖面”驰名中外，厚度近万米，包括长城系、蓟县系和青白口系(自下而上，下同)。长城系由碎屑岩、泥质岩和碳酸盐岩构成完整的海侵沉积旋回，包括常州沟组、串岭沟组、团山子组和大红峪组。早期的地层划分方案将高于庄组划归长城系，李怀坤等(2010)和田辉等(2015)在不同地区获得高于庄组中-上部凝灰岩夹层的锆石U-Pb年龄均显示其应归属于蓟县系，本文采用近年来被普遍接受的地层划分观点(全国地层委员会，2002；李怀坤等, 2009, 2010, 2011, 2014；Su et al., 2010；王泽九等，2014；田辉等，2015)，将长城系和蓟县系的分界置于大红峪组和高于庄组之间。需要明确的是，国内外学者在中元古代起始的时间上存在1.8Ga和1.6Ga的分歧，本文沿用国内地质同行普遍认可的1.8Ga作为界限。
常州沟组 为一套以砂岩为主的碎屑岩组合。下部为砾岩、含砾粗砂岩、长石石英砂岩和石英砂岩；上部石英砂岩和砂质页岩。地层由下至上，粒度由粗变细，属于正向沉积旋回。常州沟组地层角度不整合覆盖于新太古代各类片麻岩和麻粒岩之上。
串岭沟组 为一套以粉砂质伊利石页岩为主，夹少量砂岩和碳酸盐岩的岩石组合。下部为滨海潮间带灰色粉砂岩和粉砂质页岩，含砂岩透镜体和条带；中部为潮下低能带灰绿色页岩，常含有碳质碎片和星散状黄铁矿；上部以潮间带黑色粉砂质页岩和粉砂岩为主，并夹砂岩凸镜体和条带。上下两部分受砂岩夹层影响，层理多呈波状起伏，中部层理平直，砂岩透镜体中有直线形斜层理，波痕和干裂等构造。串岭沟组与下伏常州沟组整合接触。
团山子组 以铁白云岩为主，夹少量泥质白云岩和含粉砂质白云岩。下部以泻湖相灰黑色含铁白云岩为主，夹板状泥岩和泥质白云岩，白云岩中常见星散状或结核状黄铁矿，风化面呈褐红色；上部以含硅质层黑色含铁白云岩为主，并夹薄厚不等的白云质砂岩，常见岩盐假晶、干裂和浅水波痕，为盐度较高的潮间-潮上带沉积。团山子组与下伏的串岭沟组为整合过渡关系。火山岩夹层位于团山子组上部，主要为富钾粗面安山岩，发育气孔构造和绳状构造，锆石U-Pb年龄为1637±15Ma(张拴宏等, 2013, 图 1c)。
大红峪组 根据岩石组合分为3段。下部以碎屑岩为主，厚层乳白色石英岩状砂岩夹紫红色粉砂岩、含浅绿色硅质条带的含砂白云岩或白云质石英砂岩以及翠绿色富钾页岩，具有韵律式沉积特征；中部以大量火山岩的出现为标志，包括富钾基性火山熔岩、火山角砾岩(集块岩)，夹少量石英砂岩和凝灰岩；上部主要为碳酸盐岩层，发育叠层石和大的礁状体。在砂岩中常见波痕、交错层理和干裂等沉积构造。与下伏的团山子地层为整合接触关系。
大红峪组火山岩是一套超钾质，富铝、贫硅的粗面岩-碱玄岩-响岩组合。空间上东西向延伸，主要分布于北京平谷、天津蓟县、冀东遵化和滦县等地(图 1c)，出露面积为600km2，在平谷和蓟县最大厚度分别为718m和490m(胡俊良等，2007)。岩石喷发类型复杂多样，既有强烈爆发产出的火山角砾岩(集块岩)，也有熔岩和凝灰岩。西部(平谷地区大华山和熊儿寨)火山活动较为强烈，熔岩比例大，厚度近500m；东部(蓟县地区下营附近)以火山角砾岩为主；中部多为火山碎屑岩。根据大红峪组火山产物及其间赋存的石英砂岩划分出4期喷发旋回，分别被3层石英砂岩隔开：其中第4期熔岩最为发育，遍布全区。其它3期火山活动较弱，熔岩层较薄，并依次变厚，火山角砾岩、火山碎屑岩和凝灰岩等较发育，且不同地区厚度各异，显示大红峪期火山活动由弱变强伴有多次喷发间隙的特点。此外，以脉状穿插侵入的辉绿岩、煌斑岩和正长斑岩等在大红峪组和下伏地层发育。
2 样品采集和分析方法 2.1 样品采集本次研究采集火山岩样品共7件(15ZJ01~15ZJ07)，其中4件样品分选出锆石(15ZJ02大红峪组粗面玄武岩；15ZJ04团山子组粗面岩；15ZJ05大红峪组粗面安山岩；和15ZJ06团山子组粗面玄武岩)。
15ZJ02采自平谷大华山镇苏子峪东南(40°13′34.70″N、117°5′41.50″E)，位于大红峪组火山岩的下部，发育气孔杏仁构造，呈褐红色，粗面玄武岩具有斑状结构，块状构造，主要由斜长石(~70%)、普通辉石(~15%)和少量的角闪石、黑云母及磁铁矿组成。斑晶为基性斜长石和辉石，斜长石半自形板状，粒径0.34~1.8mm，发育聚片双晶及卡钠复合双晶。岩石整体发生强烈碳酸盐化、粘土化。15ZJ04(40°14′44.30″N、117°7′10.90″E)和15ZJ06(40°14′52.85″N、117°26′56.70″E)分别采自平谷熊耳寨乡和蓟县黄崖关村附近，属于团山子组上部的火山岩夹层，为一套富钾粗面玄武岩、火山角砾岩及凝灰质砂岩等。火山岩露头表面呈褐黄色，新鲜面灰白色，气孔发育被白云石充填而形成杏仁状构造，未遭受明显的变质。岩浆水平流动导致岩层上部气孔明显被拉长，扁平面与上覆白云岩产状相一致。火山岩组成矿物主要由碱性长石、斜长石、辉石(部分绿泥石化)、角闪石、黑云母及磁铁矿组成。15ZJ05采自平谷黄松峪附近(40°12′28.27″N、117°13′59.99″E)，为大红峪组粗面安山岩，新鲜面呈灰白色，风化后呈褐黄色、褐红色，气孔杏仁构造发育。板状结构，斑晶主要为钾长石和少量的斜长石，钾长石呈自形-半自形，长径1~3mm。基质由钾长石、斜长石和基性矿物及磁铁矿组成，基性矿物强烈的绿泥石化、黑云母化。
2.2 锆石U-Pb年代和Hf-O同位素样品经破碎和淘洗, 在双目镜下挑出锆石，锆石分选工作由河北省区域地质矿产调查研究所实验室完成。将待测锆石样品颗粒和锆石标样浇铸在环氧树脂靶上，待环氧树脂固化以后将样品靶打磨、抛光至锆石的核部。通过透、反射光显微照相和阴极发光图像分析，对锆石内部结构进行研究。锆石U-Th-Pb和O同位素测定在北京离子探针中心的SHRIMP Ⅱ二次离子探针质谱仪上完成，U-Th-Pb测试原理和方法见Compston et al.(1984, 1992)和Williams(1998)。一次离子流(O2-)强度为2.0~2.5nA，束斑直径为25~30μm。标准样品和待测样品分析比例为1/4。采用标准锆石TEMORA(参考年龄为417Ma；Black et al., 2004)进行同位素分馏校正，M257(参考年龄561Ma；U含量840×10-6；Nasdala et al., 2008)标定待测锆石的U含量，利用实测的204Pb进行普通铅校正。数据处理采用SQUID和Isoplot程序(Ludwig，2003)。单个数据的误差为1σ，加权平均年龄误差为95%置信度。O同位素测试原理和流程见文献Ickert et al.(2008)和Wan et al.(2013)。将做过SHRIMP锆石U-Pb定年的样品靶再次进行抛光处理，以消除前期O2-源对锆石表面的污染。一次离子流(133Cs+)强度为15nA，加速电压为10kV。δ18O的计算方法即样品与维也纳标准海水18O/16O(V-SMOW)的千分差。仪器质量分馏(IMF)校正采用标准锆石TEMORA(δ18O=8.20‰；Black et al., 2004)。
锆石Lu-Hf同位素分析在中国地质调查局天津地质调查中心同位素实验室的193nm准分子激光剥蚀系统(New Wave)和多接收器电感耦合等离子体质谱仪(Thermo Fisher Neptune；MC-ICP-MS)完成。仪器运行条件、Lu-Hf同位素分析方法见吴福元等(2007)和耿建珍等(2011)。静态信号采集模式，激光剥蚀时间30s，积分时间0.131s。激光束斑直径50μm，能量密度10~11J/cm2，频率为8Hz。采用GJ-1和Plesövice作为外标。176Lu衰变常数为λ=1.865×10-11/y(Scherer et al., 2001)，球粒陨石的(176Hf/177Hf)CHUR和(176Lu/177Hf)CHUR比值分别为0.0332和0.282772(Blichert-Toft et al., 1997)，现今亏损地幔的(176Hf/177Hf)DM和(176Lu/177Hf)DM比值分别0.28325和0.0384(Nowell et al., 1998)，用于计算地壳模式年龄(tDM2)的大陆地壳平均值为0.015(176Lu/177Hfcc；Griffin et al., 2000)。
3 分析结果 3.1 锆石U-Pb年代学锆石颗粒大部分为无色或淡黄色透明-半透明晶体，多呈长柱状，自形-半自形，粒径50~150μm，长宽比2: 1~3: 1 (图 2a-d)。阴极发光图像(CL image)显示带状或者不规则分区，具有基性岩浆成因的特征。4个样品进行锆石U-Pb年代学测试结果见表 1。由于样品年龄>1.0Ga，锆石颗粒可能受到不同程度Pb丢失的影响，理论上锆石207Pb/206Pb表面年龄更接近其实际的结晶年龄(Gehrels，2014)，因此本文全部用207Pb/206Pb加权平均年龄进行讨论。
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图 2 北京平谷大华山-天津蓟县黄崖关地区长城纪碱性火山岩(团山子组15ZJ04和15ZJ06；大红峪组15ZJ02和15ZJ05)锆石SHRIMP U-Pb谐和图(a-d)、207Pb/206Pb年龄加权平均值(e-h)和锆石CL图像 Fig. 2 SHRIMP zircon U-Pb concordia diagrams (a-d), 207Pb/206Pb age weighted mean plots (e-h) and typical zircon CL images of the Changchengian alkaline volcanic rocks (the Tuanshanzi Formation, samples 15ZJ04 and 15ZJ06; the Dahongyu Formation, samples 15ZJ02 and 15ZJ05) from areas of Dahuashan of the Pinggu, Beijing to Huangyaguan of Jixian, Tianjin |
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表 1 北京平谷大华山-天津蓟县黄崖关地区长城纪碱性火山岩锆石SHRIMP U-Th-Pb同位素测试结果 Table 1 SHRIMP zircon U-Th-Pb isotope of the Changchengian alkaline volcanic rocks from areas of Dahuashan of Pinggu, Beijing to Huangyaguan of Jixian, Tianjin |
样品15ZJ02分析7颗锆石，U和Th含量分别为49×10-6~391×10-6和28×10-6~404×10-6，Th/U比值0.5~1.0。其中点1.1谐和度低 < 80%，具有明显的Pb丢失现象(图 2a)，晶格可能受到辐射损伤的影响(7颗锆石中U和Th含量最高)，年龄统计时予以剔除；其余颗粒谐和度均>95%，207Pb/206Pb表面年龄变化范围1569~1620Ma，加权平均值为1605±19Ma(图 2e；MSWD=0.81；N=6)。样品15ZJ04分析20颗锆石，U和Th含量分别为31×10-6~159×10-6和11×10-6~136×10-6，Th/U比值0.4 ~ 0.9。绝大多数颗粒谐和度> 95%(点10.1除外，谐和度92%)，207Pb/206Pb表面年龄变化范围1562~1641Ma(图 2b)，加权平均值为1613±11Ma(图 2f；MSWD=0.93；N=19)。样品15ZJ05分析13颗锆石，U和Th含量分别为21×10-6~ 417×10-6和11×10-6~136×10-6，Th/U比值0.3~1.0。获得两组年龄数据：6颗锆石(点1.1、2.1、8.1、10.1、12.1和13.1)CL振荡生长环带代表中酸性岩浆来源，207Pb/206Pb表面年龄变化范围2477~2540Ma，加权平均值为2519±21Ma(图 2c；MSWD=4.0；N=6)，与华北克拉通主要的基底岩系年龄一致，与常州组和串岭沟组碎屑锆石U-Pb年龄谱中新太古代晚期的峰值相对应(Wan et al., 2003)，推测其为岩浆上升过程从围岩捕获的锆石；其余7颗锆石207Pb/206Pb表面年龄变化范围1544~1656Ma，剔除谐和程度低的点9.1(谐和度76%)，加权平均值为1634±18Ma(图 2g；MSWD=1.18；N=6)。样品15ZJ06分析12颗锆石，U和Th含量分别为134×10-6~265×10-6和67×10-6~178×10-6，Th/U比值0.5~0.8，全部颗粒位于谐和线附近(图 2d)，207Pb/206Pb表面年龄变化范围1602~1673Ma，加权平均值为1630±10Ma(图 2h；MSWD=1.02；N=12)。
3.2 锆石Hf-O同位素组成特征对团山子组和大红峪组4件钾质火山岩锆石样品进行Hf-O同位素分析。与上述钾质火山岩形成对比，选取侵入串岭沟黑色页岩的钠质基性岩脉锆石(样品06JX01-1，U-Pb年龄和Lu-Hf同位素见张健等，2015)进行O同位素测试。
对碱性火山岩的41个锆石颗粒进行原位Lu-Hf同位素测定(表 2、图 3)，分析结果表明团山子组和大红峪组钾质火山岩的锆石有非常均匀且一致的Hf同位素组成：团山子组锆石(15ZJ04和15ZJ06)176Hf/177Hf初始值为0.281691~0.281840, 对应的εHf(t)=-2.0~3.3；大红峪组锆石(15ZJ02和15ZJ05)176Hf/177Hf初始值为0.281700~0.281849, 对应的εHf(t)=-2.2~3.7。绝大多数锆石样品176Lu/177Hf比值小于0.002，176Lu原位衰变造成的176Hf/177Hf比值随时间累积的变化非常小。因此，其结晶的锆石基本可以有效保留该岩浆的初始176Hf/177Hf比值(Patchett et al., 1982；吴福元等，2007)。综合本文和前人资料(Wang et al., 2015a；张健等，2015)，团山子组和大红峪组钾质火山岩以及基性岩脉Lu-Hf同位素组成变化范围一致(图 3a)，εHf(t)符合正态分布规律，峰值为+0.62(N=157，图 3b)。与同时期的亏损地幔值(~+10)比较，长城系碱性火山岩和岩脉显示偏富集特征。
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表 2 北京平谷大华山-天津蓟县黄崖关地区长城纪碱性火山岩(团山子组15ZJ04和15ZJ06；大红峪组15ZJ02和15ZJ05)锆石Lu-Hf同位素 Table 2 Zircon Lu-Hf isotope of the Changchengian alkaline volcanic rocks (the Tuanshanzi Formation, samples 15ZJ04 and 15ZJ06; the Dahongyu Formation, samples 15ZJ02 and 15ZJ05) from areas of Dahuashan of Pinggu, Beijing to Huangyaguan of Jixian, Tianjin |
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图 3 北京平谷-天津蓟县长城纪碱性火山岩(06JX05-1B、15ZJ02、15ZJ04、15ZJ05和15ZJ06)和岩脉(06JX01-1)锆石Lu-Hf同位素特征 Fig. 3 Zircon Lu-Hf isotope characteristics of the Changchengian alkaline volcanic rocks (Sample 06JX05-1B, 15ZJ02, 15ZJ04, 15ZJ05 and 15ZJ06) and dike (Sample 06JX01-1) from areas of Pinggu of Beijing to Jixian of Tianjin |
钠质基性岩脉和钾质火山岩的O同位素测试结果见表 3和图 4。基性岩脉δ18O=4.6‰~ 7.7‰(N=22)，概率统计的峰值为5.9‰和7.4‰；钾质火山岩δ18O=4.5‰~7.0‰(N=30)，峰值为5.7‰和6.2‰。钾质火山岩和钠质基性岩脉的O同位素变化范围较大，多数测试点明显高于地幔锆石值(5.3±0.3‰，Valley et al., 1994)和洋岛拉斑玄武岩的平均值(5.4‰)，总体位于大陆地区镁铁质熔岩δ18O的变化范围(4.9‰~8.0‰，郑永飞，1999)。
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表 3 北京平谷-天津蓟县长城纪碱性火山岩(15ZJ02、15ZJ04、15ZJ05和15ZJ06)和岩脉(06JX01-1)锆石O同位素 Table 3 Zircon O isotope of the Changchengian alkaline volcanic rocks (samples 15ZJ02, 15ZJ04, 15ZJ05 and 15ZJ06) and dike (Sample 06JX01-1) from areas of Pinggu of Beijing to Jixian of Tianjin |
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图 4 北京平谷-天津蓟县长城纪碱性火山岩(15ZJ02、15ZJ04、15ZJ05和15ZJ06)和岩脉(06JX01-1)锆石氧同位素特征 Fig. 4 Zircon oxygen isotope characteristics of the Changchengian alkaline volcanic rocks (samples 15ZJ02, 15ZJ04, 15ZJ05 and 15ZJ06) and dike (Sample 06JX01-1) from areas of Pinggu of Beijing to Jixian of Tianjin |
华北克拉通北缘燕辽裂谷长城系碱性岩浆岩主要有两种类型：分别是以团山子组和大红峪组为代表的钾质火山岩和以侵入串岭沟组为代表的钠质岩脉。通过不同测试方法已经积累大量的年龄数据。其中，侵入串岭沟的钠质岩脉的出露规模比较小，年龄结果比较一致，为1634±9Ma(LA-ICP-MS，张拴宏等，2013)和1620±9Ma(SHRIMP，张健等，2015)。但是钾质火山岩的形成时代还未形成统一的认识，包括TIMS：1625.3±6.2Ma(大红峪组，陆松年和李惠民，1991)和1683±67Ma(团山子组，李怀坤等，1995)；LA-ICP-MS：1637±15Ma(团山子组，张拴宏等，2013)、1671±15Ma(Wang et al., 2015a)和1664~1645Ma(大红峪组，Wang et al., 2015a)；SHRIMP：1622±32Ma和1624±9Ma(大红峪组，Lu et al., 2008；张健等，2015)。综合上述资料，钾质火山岩的年龄范围较大1.68~1.62Ga，陆松年和李惠民(1991)、张拴宏等(2013)、Lu et al.(2008)和张健等(2015)利用不同测年方法获得的年龄结果一致~1625Ma，而Wang et al.(2015a)的年龄普遍较大，最早起始时间为1671±15Ma。如果按照上述结果计算，喷发活动持续周期长达~50Myr理应形成巨厚的火山岩层。但是，从沉积响应的角度考虑，大红峪组火山岩的下部具有波痕、干裂等沉积构造的碎屑物质，上部被含叠层石的碳酸盐岩覆盖，火山活动发育于坳陷盆地的沉降阶段，基本排除因正地形遭受隆升剥蚀的可能性。另外，砂岩碎屑与火山物质的沉积速率相当可观，这显然与野外实际观察到有限的岩浆规模及地层厚度(~500m)不相符。更关键的是，串岭沟组凝灰岩年龄1621±6.9Ma和1634.8±6.9Ma(孙会一等，2013；刘典波等，2019)，其上覆的团山子组和大红峪组火山岩的年龄应更年轻。本文系统分析出露于平谷-蓟县地区钾质火山岩的形成时代，力求空间尺度和地层序列的全面覆盖，获得SHRIMP锆石U-Pb年龄1613±11Ma、1634±18Ma(团山子组)和1605±19Ma、1630±10Ma(大红峪组)，且在误差范围内基本一致。锆石自形程度低、CL带状分区以及高Th/U比值表明其为高温基性岩浆结晶过程的产物。因此，锆石结晶年龄~1625Ma能够代表岩石的形成时代，整个长城系碱性火山岩是在较短的时限内以火山角砾岩(集块岩)、熔岩和凝灰岩等形式集中喷发。这一认识得到大红峪组上、下地层串岭沟组和高于庄组凝灰岩夹层年龄的支持(李怀坤等，2010；孙会一等，2013；田辉等，2015；刘典波等，2019)。此外，侵入串岭沟组的钠质岩脉与火山岩同期发育。
4.2 长城系碱性岩的成因侵入串岭沟的钠质岩脉和多数团山组和大红峪组的钾质火山岩为玄武质成分，普遍具有低SiO2(< 53%)、高碱含量(Na2O+K2O=5%~13%)，少量为过碱性的碱玄质或响岩质火山岩(胡俊良等，2007；Wang et al., 2105a；张健等，2015)，共同组成长城系碱性岩系列。钾质火山岩和钠质岩脉的主量元素除K2O和Na2O在各自端元富集外(K2O/Na2O变化范围0.1~130，个别样品高达~1400)，前者的全碱和SiO2含量较高，而后者的MgO、CaO、FeOT和TiO2含量较高，Al2O3含量没有明显的区别。FeOT和TiO2含量与铁钛氧化物在岩浆结晶过程中氧逸度控制的饱和程度或重力分异有关。Hacker图解上，样品SiO2连续变化且与其它主量元素具有良好的线性关系，长城系碱性岩来自相同的母岩浆，可能经历分离结晶作用。同样，钾质火山岩和钠质岩脉微量元素组成与洋岛玄武岩OIB特征类似，富集大离子亲石元素(LILE，Rb、Ba和Th等)、高场强元素Nb-Ta显示弱的正异常。相容元素Cr、Co和Ni的含量偏低，岩浆经历橄榄石和(或)辉石的分离结晶。钾质火山岩的稀土元素总量(∑REE)比钠质岩脉高，结合其高SiO2和低MgO的特征，代表分离结晶的结果。轻稀土元素(LREE)富集，轻、重稀土分馏大说明岩浆的熔融程度低以及源区可能存在高压相石榴石的残留。Eu异常特征和斜长石的分离结晶不明显。
长城系碱性岩分布于华北克拉通燕辽裂谷的内部，其主体为碱性OIB型玄武岩，属于大陆裂解的产物。目前，对于板内碱性玄武岩成因的争议主要围绕：(1)来源于软流圈地幔还是岩石圈地幔(Pilet et al., 2004)或者是软流圈地幔-岩石圈地幔的相互作用(Tang et al., 2006)；(2)源岩是地幔橄榄岩还是非地幔橄榄岩，比如角闪岩、辉石岩或榴辉岩(Hirschmann et al., 2003；Niu，2008；Yang et al., 2019a)以及橄榄岩与非橄榄岩的机械混合(Liu et al., 2008)；(3)岩浆是单一来源的还是不同来源的岩浆混合(Niu，2008)。钾质火山岩和钠质岩脉的锆石Hf同位素变化范围一致(εHf(t)=-2~+4)，暗示相同的地幔源区，εHf(t)峰值为+0.62明显比同期的亏损地幔(~+10)富集，属于软流圈地幔-岩石圈地幔相互作用的结果。识别其富集组分是源区的岩石圈物质添加还是岩浆上升过程的地壳混染尤为重要。以下事实可以排除地壳混染的可能性：(1)长城系碱性岩为OIB型，微量元素Nb-Ta富集，明显不同于壳源岩浆Nb-Ta亏损；(2)碱性岩主要是喷发形式，在地壳居留时间较短，二者相互作用的几率小；(3)Nb/La(>1)和Zr/Nb比值以及Nd-Hf同位素的变化范围不大。因此，岩浆的同位素富集继承源区本身的属性，华北长城系碱性岩源区受到岩石圈物质的交代作用。
锆石抗改造能力强，可以有效保存岩浆初始的成分信息并且避免后期围岩的干扰。幔源岩浆结晶出来的锆石有非常一致的δ18O值5.3‰±0.3‰，而且该比值受岩浆分异的影响很小, 由岩浆分异造成的全岩δ18O值增高会被锆石/熔体之间的δ18O分馏增加所补偿。因此, 锆石O同位素用来鉴别碱性岩源区中岩石圈物质(Zhu et al., 2017)。与裂谷环境低δ18O不同(Wang et al., 2011a；Watts et al., 2011)，长城系碱性岩比正常地幔值5.3‰±0.3‰明显偏大，岩浆锆石的高δ18O特征通常认为源区有沉积物质的加入。考虑到碱性火山岩富钾特点，其地幔源区可能受到高δ18O沉积岩的交代作用，经过深俯冲作用被带入地幔的沉积物质尤其是泥质岩石在不同深度的熔融，会释放出大量富K或者Na的熔/流体交代地幔橄榄岩。交代过程富K或者Na的熔/流体不断消耗源区的橄榄石，从而增加地幔橄榄岩中辉石的比例，其中一部分含角闪石或者金云母等钾质矿物。而且，这些矿物本身富含挥发份，显著降低地幔强度以及固相线的温度，促进减压或者升温条件下部分熔融形成原始岩浆。
4.3 华北克拉通中新元古代岩浆特点和动力学机制自~1.8Ga，华北克拉通内部识别出熊耳、燕辽和渣尔泰-白云鄂博三个裂谷带(裂谷盆地)，其中熊耳裂谷(1.8~1.75Ga)底部发育河湖相砂岩-泥岩沉积(大古石组，1.8~1.78Ga)，是华北克拉通结晶基底形成后最早的盖层沉积，而燕辽裂谷的起始时间稍晚，最新的研究成果将其盆地发育的起始时间限定在~1.65Ga以后。华北克拉通内保存着大量岩浆事件的记录(相振群，2014；翟明国等，2014；耿元生等，2020)并与裂谷带(裂谷盆地)耦合发育，呈幕式演化特征，说明“无聊的十亿年”并不无聊：1)1.83~1.75Ga华北南缘熊耳火山岩群和碱性岩带以及太行山地区的基性岩墙群(Zhao et al., 2002b, 2004b, 2009a, 2018；Wang et al., 2004, 2008, 2010, 2014a, 2016a, b，2019；耿元生等，2004；陈斌等，2006；Peng et al., 2007, 2008, 2015；韩宝福等，2007；徐勇航等，2007；He et al., 2008, 2009, 2010；Zhao and Zhou, 2009；胡国辉等，2010；崔敏利等，2010; Cui et al., 2011, 2013；柳晓艳，2011；Xia et al., 2013；Zhang et al., 2013；Yang et al., 2014a, 2019b, c；Deng et al., 2016a；Li et al., 2016, 2020；师江朋等，2017；Xue et al., 2018；邓小芹等，2019；Jia et al., 2020；Xu et al., 2020)；2)1.75~1.67Ga华北克拉通北缘燕辽裂谷带内非造山侵入的斜长岩(anorthosite)、纹长二长岩(mangerite)、紫苏花岗岩(charnockite)、花岗岩(granite)等(AMCG组合)(Rämö et al., 1995；赵太平等，2004；杨进辉等，2005；Zhang et al., 2007；高维等，2008；Zhao et al., 2009b；Jiang et al., 2011；Liu et al., 2011, 2016；Peng et al., 2012；王惠初等，2012；Chen et al., 2013b, 2019；Wang et al., 2013a, 2018；Yang et al., 2014b；相振群，2014；Teng and Santosh, 2015；Li et al., 2019；康健丽等，2020)，同期莱芜地区亦有基性岩的报道(Li et al., 2015)；3)1.63~1.62Ga燕辽裂谷富钾碱性岩、华北南缘龙王幢碱性花岗岩和鲁西泰山基性岩墙(陆松年等，2003；胡俊良等，2007；包志伟等，2009；相振群等，2012；Wang et al., 2013b, 2015a, 2020a；相振群，2014；邓小芹等，2015；张健等，2015；Deng et al., 2020)；4)1.33~1.30Ga以侵入到下马岭组与雾迷山组的基性岩墙(床)(Zhang et al., 2009, 2012b, 2017a；李怀坤等，2009；Wang et al., 2014b；Zhu et al., 2020a)以及白云鄂博碳酸岩和冀北地区酸性岩体(Yang et al., 2011；Shi et al., 2012；相振群，2014；Zhang et al., 2017b)；5)~1.23Ga华北克拉通东缘的通化辉绿岩墙、建平-青龙基性岩墙(裴福萍等，2013；Wang et al., 2015b, 2016c, 2020b)、滦南第四系覆盖的隐伏基性岩体以及沂水地区的辉长岩(Peng et al., 2013；相振群，2014)；6)0.9~0.75Ga胶辽-徐淮、冀东以及朝鲜等地的基性岩墙以及0.85~0.82Ga大红口组和渣尔泰群的岩浆活动(Liu et al., 2006；彭润民等，2010；阎国翰等，2010；Peng et al., 2011；Wang et al., 2011b, 2012；Hu et al., 2014；Ling et al., 2015；Zhang et al., 2016；Su et al., 2018；彭澎等，2018；Zhu et al., 2019；胡国辉等，2019)。除大规模岩浆事件群之外，盆地内出现多期以凝灰岩和斑脱岩为特征的火山活动：1.64~1.56Ga串岭沟组、洛峪口组、龙家园组和高于庄组(李怀坤等，2010；苏文博等，2012；孙会一等，2013；田辉等，2015；李承东等，2017；刘典波等，2019；张恒等，2019)，1.48~1.44Ga雾迷山组和铁岭组(Su et al., 2010；李怀坤等，2014)以及1.39~1.32Ga下马岭组和白术沟组(Gao et al., 2008；Su et al., 2008；Zhu et al., 2020b)。
华北克拉通1.8~0.75Ga岩浆事件群主要是基性岩墙、A型花岗岩以及少量的碳酸岩脉，具有双峰式的岩浆特点。酸性端元绝大多数为A型花岗岩形成于高温低压条件下，是伸展环境的标志，时间集中分布于1.84~1.50Ga(曾令君等，2013；Deng et al., 2016b)，空间局限在裂谷盆地发育的范围。绝大多数的锆石Hf同位素富集，位于2.5Ga的地壳演化线附近(tDMC≈2.5Ga，图 5)，岩浆主要来自克拉通基底陆壳岩石的部分熔融。基性端元以碱性-亚碱性拉斑质的镁铁质岩墙或岩席为主，是幔源岩浆活动的产物，大规模岩墙群或岩席群的出现与陆内裂谷或者超大陆裂解有关，暗示强烈的深部地球动力学过程。岛弧型钙碱性岩石仅出现在熊耳期(Wang et al., 2004, 2008；He et al., 2008, 2009, 2010；Zhao et al., 2009a)，赵太平等(2007)将其地球化学特征解释为继承于受俯冲组分改造的陆下岩石圈富集地幔源区，但仍属于裂谷构造背景，并得到沉积学的支持。
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图 5 华北克拉通中-新元古代岩浆事件锆石/斜锆石Hf同位素特征 黑色点和彩色点分别代表酸性和基性-中性岩石.基性-中性岩石锆石/斜锆石Hf同位素数据来自：韩宝福等，2007；Zhao et al., 2009b；Wang et al., 2011b, 2012, 2013a, 2014a, 2015a, b，2016a，b；Zhang et al., 2012b；相振群，2014；Yang et al., 2014a, b，2019c；张健等，2015；Teng and Santosh, 2015；Liu et al., 2016；Chen et al., 2019；Li et al., 2019, 2020；Zhu et al., 2019, 2020a；本文.酸性岩石锆石Hf同位素数据来自：杨进辉等，2005；陈斌等，2006；Zhang et al., 2007, 2012b；包志伟等，2009；Zhao and Zhou, 2009；Wang et al., 2010, 2013b, 2018, 2019；Jiang et al., 2011；Shi et al., 2012；Cui et al., 2013；曾令君等，2013；相振群，2014；Yang et al., 2014b, 2019c；邓小芹等, 2015, 2019；Deng et al., 2016a, b；师江朋等，2017；Xue et al., 2018；Zhao et al., 2018；Jia et al., 2020；Li et al., 2020；康健丽等，2020；Xu et al., 2020 Fig. 5 Zircon/baddeleyite Hf isotope characteristics of magma events during Meso-Neoproterozoic from the North China Craton |
中-新元古代华北克拉通处于持续裂解阶段，翟明国等(2014)形象地称其为“一拉到底的构造环境”，不同期次的基性岩浆活动被习惯性解释为地幔柱驱动。但是，这种成因上的联系是通过推测而建立，并无真正意义上的因果关系。实际上，华北克拉通中-新元古代的基性镁铁质岩石Mg#普遍偏低，Si饱和，矿物组成多以单斜辉石和斜长石为主，说明岩浆经历不同程度的分离结晶过程，并不能代表地幔部分熔融所产生的原始岩浆。而且，橄榄石以斑晶形式零星的出现，高镁苦橄岩存在的可能性不大，但它却是约束地幔柱的有效手段。所以，地幔柱模型是否是形成基性岩浆的必要条件或者地幔柱在超大陆裂解过程中所起的作用是亟需回答的问题。目前，地球科学领域关于大陆裂解的动力学机制的争论愈发激烈，代表的观点有：(1)核幔边界或者软流圈地幔起源的地幔柱(自下而上bottom-up，Anderson，1994；Li and Zhong, 2009)；(2)大洋板块深俯冲驱动的板块构造(自上而下top-down，Niu，2020)；以及(3)地幔柱和深俯冲二者兼而有之(Zhang et al., 2019；Chen et al., 2020；李献华，2021)。公认的现代板块构造以及冷俯冲作用起始于新元古代(~0.8Ga，Stern，2005)，但是，根据华北克拉通中部带高压变质(Zhao et al., 2002a)、深源包裹体(Xu et al., 2018)以及地球物理探测(Wan et al., 2020)可以明确：华北克拉通在古元古代晚期已经存在板块的持续深俯冲范式，并得到地球化学数据的支持(Liu et al., 2019)。因此，在解释华北克拉通中-新元古代“一拉到底”的驱动力时，除了考虑地幔柱模型，板块构造模型也不能排除。根据目前现有的资料，尚不能给出明确的选择。但是，综合华北克拉通基性岩锆石Hf同位素发现在~1.32Ga发生突变(图 5)：早期的多数岩浆Hf同位素富集(εHf(t) < 0)，晚期岩浆亏损(εHf(t)>0)，暗示该时期出现岩浆源区和构造体制的重大转折。同样，熊耳、燕辽和渣尔泰-白云鄂博三大裂谷盆地的沉积作用在~1.32Ga骤然停止，直至~1.0Ga又重新启动(Liu et al., 2020；Zhu et al., 2020b；李怀坤等，2020)，普遍存在下马岭组-长龙山组(燕辽裂谷)和白术沟组-三川组之间(熊耳裂谷)长达~300Myr的沉积间断，说明整个华北克拉通在~1.32Ga发生整体的抬升。因此，~1.32Ga岩浆很有可能成为检验大陆裂解驱动模型的窗口。华北克拉通在未经中生代岩石圈减薄和破坏之前，显生宙的地幔包体Lu-Hf和Re-Os模式年龄集中指向~1.3Ga(Li et al., 2011；Zheng et al., 2014)，说明中元古代的岩石圈受到强烈的交代改造，从而降低克拉通的稳定性。如果从行星地球的尺度观察，~1.3Ga地球内部液态铁冷却导致的内核生长引起古地磁场强度的显著增加(Biggin et al., 2015)，Condie(2020)推测地核降温受到俯冲板块到达核幔边界并聚集的影响。地球内部物理(化学？)条件的改变势必引起表层地壳的耦合响应，能否形成超大陆裂解需要更深入的工作。
5 结论本文分析长城纪碱性岩锆石U-Pb年代学和Hf-O同位素并总结华北克拉通中-新元古代岩浆事件锆石Hf同位素，获得以下三点认识：
(1) 出露于平谷-蓟县地区钾质火山岩的形成年龄分别为1613±11Ma、1634±18Ma(团山子组)和1605±19Ma、1630±10Ma(大红峪组)，说明它们在~1625Ma集中喷发，持续时间较短，与侵入串岭沟组的钠质岩脉同期。
(2) 钾质火山岩和钠质岩脉的锆石Hf-O同位素相似：碱性岩源自富集地幔(εHf(t) =-2~+4，正态分布峰值+0.6)，源区受到高δ18O沉积物质的交代(δ18O=4.5‰~7.7‰，多数高于地幔锆石值)而富含钾质矿物，如角闪石或金云母。
(3) 华北克拉通中-新元古代发育多期与裂解作用有关的岩浆事件，在~1.32Ga发生锆石Hf同位素突变，由富集转向亏损的特征，暗示强烈的交代作用，可能是检验地幔柱或者板块俯冲驱动超大陆裂解机制的窗口。
致谢 感谢任纪舜院士、陆松年研究员和刘敦一研究员对我们研究工作的长期支持。
谨以此文祝贺沈其韩院士百岁华诞，向沈先生始终如一的严谨治学态度以及在前寒武纪地质和变质地质学领域所取得的卓越贡献致敬！
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