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胶东地区的北苏鲁超高压变质带广泛发育新元古代花岗片麻岩,记录了780~700Ma的成岩年龄和240~220Ma的变质年龄,这些新元古代花岗片麻岩通常被认为与扬子克拉通有亲缘性,是扬子克拉通北缘大陆裂解的产物(Yin An et al., 1993; Li et al., 1994; 陆松年, 1998; 李永刚等, 1999; 郑永飞等, 2003)。有关北苏鲁超高压变质带与华北克拉通胶北地块之间构造边界的认识长期存在分歧,前人观点达十余种之多(曹国权等, 1990; 林钧堂, 1993; 张希道和王来明, 1996;Ishizaka et al., 1996;Wallis et al., 1999; 翟明国等, 2000;宋明春等, 2000;Hao Tianyao et al., 2002; 徐扬等, 2015)。近年来,随着基础地质调查、同位素年代学和地球化学研究等数据的积累,分歧逐渐减小,目前已趋于两种主要观点:① 基于地球物理的研究推断五莲-青岛-荣成断裂是华北克拉通与苏鲁造山带的边界构造带(曹国权等, 1990;Hao Tianyao et al., 2002; 郝天珧等, 2004);② 基于岩石学、地球化学的研究主张五莲-即墨-牟平断裂是两者的界线(薛怀民等, 2006; Tang Jun et al., 2008a; Zhang Shaobing et al., 2014)。由于碰撞造山带深俯冲—折返构造的复杂性以及侏罗纪以来构造-岩浆作用的叠加改造,使确定华北克拉通东南缘与苏鲁超高压变质带之间构造边界的性质和准确位置较为困难。
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前人针对华北板块和扬子板块的碰撞过程做了大量的研究工作,提出了多种碰撞造山模型(Okay et al., 1992; Yin An et al., 1993;Li, 1994; Lin and Li, 1995; 翟明国等, 2000; Yuan et al., 2003; Xu Zhiqin et al, 2006; 许志琴等, 2007; Li Sanzhong et al., 2017),针对华北-扬子板块的俯冲极性和方式、高压/超高压岩石变质作用和折返过程等关键问题提出多种观点。为解释北苏鲁超高压变质带航磁异常与地表地质不一致的现象以及深部地壳结构的差异,Li(1994)曾提出一个地壳拆离模式,推测扬子陆块的上地壳从下地块拆离并在碰撞期间在华北陆块之上推覆了400余千米,而扬子岩石圈的下部则沿着缝合带俯冲到华北陆块之下。翟明国等(2000)认为北苏鲁造山带与华北克拉通的分界线不是一条断层,高压—超高压板片折返过程中可能发生了与薄皮构造机制类似的结构过程。Xu Peifen et al.(2002)认为地震层析成像揭示了苏鲁造山带之下的“鳄鱼状”地壳速度结构。许志琴等(2006)为解释北苏鲁超高压变质带中存在的华北克拉通基底物质提出了一个陆—陆碰撞的俯冲剥露模式,认为是扬子板块深俯冲过程中,拽动相邻的华北克拉通胶北地块的部分物质向下俯冲。但是,华北克拉通变质基底物质大量出现在北苏鲁超高压变质带的新元古代花岗片麻岩中,以物质成分限定的五莲-即墨-牟平构造边界与地球物理异常不一致等现象依然令人困惑。在总结前人研究的基础上,笔者对胶东地区相关地质问题进行了反思,对胶南地区新元古代花岗岩的产出背景有所质疑,认为新元古代花岗岩归属扬子陆块可能制约了苏鲁造山带研究的思路。
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1 新元古代花岗岩与华北克拉通接触边界性质
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主流观点认为五莲-即墨-牟平断裂带构成了苏鲁造山带的北界,西北侧是华北克拉通的重要组成部分胶北地块,东南侧以出露苏鲁造山带的新元古代花岗片麻岩为特征(图1)。五莲-即墨-牟平断裂带由多条NNE向、呈雁列展布的断裂组成,延伸长约200km, 宽20~40km, 斜切胶东半岛(图2)。张岳桥等(2007)认为五莲-即墨-牟平断裂带至少有6条主要断裂,区域地质调查工作中多强调其中的桃村、郭城、朱吴(崖子)、海阳(育黎)等4条主干断裂,其中的桃村断裂将早白垩世牙山岩体和院格庄岩体左行错断了约30km(图1)。在桃村断裂与海阳断裂之间近30km的范围内,野外露头上难以见到明显的构造混杂现象。
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图1 胶东地区地质图
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Fig.1 Geological map of Jiaodong area
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1 —新生界;2—中生界;3—新元古代蓬莱群;4—中元古代芝罘群;5—古元古代粉子山群;6—古元古代荆山岩群;7—太古宙地质体;8—晚中生代花岗岩类;9—晚三叠世花岗岩;10—新元古代花岗片麻岩岩;11—古元古代花岗岩;12—镁铁质—超镁铁质岩;13—榴辉岩透镜体;14—断层及推测断层;15—韧性剪切构造带; ①—桃村断裂;②—郭城断裂;③—朱吴断裂;④—海阳断裂;⑤—米山断裂
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1 —Cenozoic; 2—Mesozoic; 3—Neoproteroczoic Penglai Group; 4—Mesoproterozoic Zhifu Group; 5—Paleoproterozoic Fenzishan Group; 6—Paleoproterozoic Jingshan Group Complex; 7—Archean geological bodies; 8—Late Mesozoic granitoids; 9—Late Triassic granite; 10—Neoproteroczoic granitic gneisses; 11—Paleoproterozoic granite; 12—mafic-ultromafic rock; 13—eclogite; 14—faults and inferred faults; 15—ductile shear zone; ①—Taocun fault; ②—Guocheng fault; ③—Zhuwu fault; ④—Haiyang fault; ⑤—Mishan fault
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图2 胶东乳山-牟平地区地质简图
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Fig.2 Geological map of Rushan-Muping area in Jiaodong Peninsula
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1 —新生界;2—中生界;3—新元古代蓬莱群;4—古元古代粉子山群;5—古元古代荆山岩群;6—太古宙地质体;7—白垩纪花岗岩;8—晚侏罗世花岗岩;9—新元古代花岗片麻岩;10—榴辉岩;11—断层及推测断层;12—样品位置及编号;13—新元古代花岗岩北界大致走向;①—桃村断裂;②—郭城断裂;③—朱吴断裂;④—海阳断裂;⑤—米山断裂
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1 —Cenozoic; 2—Mesozoic; 3—Neoproterozoic Penglai Group; 4—Paleoproterozoic Fenzishan Group; 5—Paleoproterozoic Jingshan Group Complex; 6—Archean geological bodies; 7—Cretaceous granite; 8—Late Jurassic granite; 9—Neoproteroczoic granitic gneisses; 10—eclogite; 11—faults and inferred faults; 12—sample location and number; 13—general trend of the northern boundary of the Neoproterozoic granitoids; ①—Taocun fault; ②—Guocheng fault; ③—Zhuwu fault; ④—Haiyang fault; ⑤—Mishan fault
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因侏罗纪—白垩纪花岗岩侵位和断裂活动以及白垩纪火山-沉积盆地覆盖,胶北地块变质基底与新元古代花岗片麻岩之间的接触边界一直没有明确的界线。在1∶25万烟台市幅区调工作中(山东省地质调查院,2003❶),受当时锆石测年技术的制约,桃村断裂以西的部分晚侏罗世花岗岩(玲珑花岗岩),因其具有片麻理构造且有许多新元古代锆石年龄信息,被划归震旦纪花岗岩。而古元古代荆山岩群野头岩组(祥山岩段)的建组剖面就位于桃村断裂东南侧的祥山一带,并有古元古代“祥山式”岩浆熔离型铁矿产出(王惠初等, 2021)。近几年,随着大量高精度测年数据的积累,在新一代山东地质志编制过程中,新元古代花岗片麻岩被限定到朱吴-崖子断裂以东(图2)。沿海阳断裂的育黎—午极—玉林店一带构造变形较强烈,断裂东侧新元古代花岗片麻岩中存在较多大理岩、云母片岩、石英岩、石榴斜长角闪岩等表壳岩包体,片麻理总体走向北东,向东南倾斜50°~70°;但断裂带西侧依然有较多新元古代花岗片麻岩出露。由此可见,西侧的桃村断裂和东侧的海阳断裂均非胶北地块变质基底与北苏鲁新元古代花岗片麻岩的岩性分界线,一系列的断层左行错动使初始的岩性分界线难窥全貌。因此以晚中生代的断裂带来限定中晚三叠世的构造边界并不妥当。
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在牟平南侧可以观察到新元古代花岗片麻岩中有云母片岩呈夹层状产出,两者产状一致。花岗片麻岩中褶皱构造发育,片麻理产状总体向北东中等角度倾斜。牟平南侧荆山岩群与花岗片麻岩之间无明显构造界线,但为区分两个构造单元,花岗片麻岩中的云母片岩、大理岩等岩石残块划归苏鲁造山带变质表壳岩组合,而将北侧牟平—养马岛一带的变质表壳岩划归古元古代荆山岩群,两者之间人为地以断层隔开(图2)。故而,胶北地块与苏鲁造山带的界线由朱吴(崖子)断裂在牟平南侧转至海阳断裂。笔者在牟平南侧花岗片麻岩中(样品位置:121°36.39′E,37°20.92′N)获得的岩浆结晶锆石U-Pb年龄为745±8Ma,变质边年龄为247±1.6Ma(图3)。
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在五莲地区苏鲁造山带北缘与胶莱盆地的结合部位,断续分布着以五莲杂岩为代表的未遭受超高压变质的岩石残片(图4),被认为是扬子板块北缘的新元古代岩石,在扬子板块俯冲过程中被刮削下来构造叠置于俯冲带附近的增生杂岩之上(Zheng Yongfei et al., 2005; Zhou Jianbo et al., 2008a, 2008b)。五莲杂岩分布于从家屯、胡家和海眼口等地,它们以石门-薛家庄韧性剪切带与超高压变质带分界。宋明春等(2020)对胡家和丛家屯岩片的斜长角闪岩研究表明,胡家斜长角闪岩时代为古元古代末期(1790±27Ma、1853±15Ma),而从家屯斜长角闪岩时代为新元古代(797±11Ma、782±16Ma),且具有E-MORB地球化学特征,指示张裂的构造背景;认为从家屯和胡家斜长角闪岩分别与扬子板块和华北板块具有构造亲缘性。Zhou Jianbo et al.(2008a)对海眼口一带的五莲群研究显示,变质基性火山岩的SHRIMP U-Pb锆石年龄为761±8Ma(是否可代表火山岩的结晶年龄存疑);变质沉积岩中碎屑锆石年龄范围为3478~625Ma,大致可以分为四组:＞3000Ma(最古老的年龄为3339Ma)、2.7~2.4Ga(峰值为2.44Ga)、2.2~1.8Ga(峰值为2.16Ga)以及~770Ma(两个数据)。并用最年轻的碎屑锆石来限定五莲群的沉积时代,认为五莲群的沉积时代晚于770Ma。从侵入五莲群的弱片麻状黑云二长花岗岩中获得了747±14Ma的单颗粒锆石U-Pb年龄(Zhou Jianbo et al., 2003)。
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笔者在五莲海眼口一带的五莲群中采集了三个年龄样品,分别为石英岩(10SD02)、黑云变粒岩(10SD03-1)和侵入黑云变粒岩中的花岗岩脉(10SD03-2)。在石英岩和黑云母变粒岩中获得的碎屑锆石年龄信息与Zhou Jianbo et al.(2008a)的结果类似。黑云变粒岩中锆石铅丢失较严重,最大年龄~3.2Ga,最小年龄为~1.3Ga,＜1.8Ga的年龄数据极少;在U-Pb年龄谐和图上可构成两条不一致线,上交点年龄分别为2164±80Ma和2498±36Ma(图4d),~2.15Ga是胶北地块上胶-辽-吉带特有的岩浆活动,碎屑锆石年龄谱特点指示其来源于华北克拉通。侵入黑云变粒岩中的花岗岩脉中获得了777.5±2.4Ma的岩浆结晶年龄(图4e)。五莲群碎屑锆石年龄谱明显区别于苏北海州群以新元古代早中期锆石为主的碎屑锆石年龄谱(Zhou Jianbo et al., 2012),结合Zhou Jianbo et al.(2008a)和宋明春等(2020)的基性火山岩测年数据,我们更倾向于认为五莲群是沉积在华北克拉通东南部的火山-沉积建造,~780Ma的双峰式岩浆岩组合是华北克拉通东南部大陆裂解的岩浆响应。
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图3 牟平南山新元古代花岗片麻岩的锆石U-Pb年龄
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Fig.3 Zircon U-Pb age of the Neoproterozoic granitic gneiss in southern Muping
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图4 五莲地区地质简图(a、b)和五莲群黑云变粒岩及侵入其中的花岗岩脉(c)的锆石U-Pb年龄(d、e)
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Fig.4 Geological sketch maps of Wulian area (a, b) and zircon U-Pb ages (d, e) of fine-grained biotite felsic gneiss of Wulian Group and granite veins (c)
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1 —第四系;2—五莲群坤山组;3—五莲群海眼口组;4—白垩纪火山-沉积岩;5—白垩纪花岗岩;6—新元古代花岗岩;7—新元古代闪长岩; 8—断层及推测断层;9—采样位置
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1 —Quaternary; 2—Kunshan Formation, Wulian Group; 3—Haiyankou Formation, Wulian Group; 4—Cretaceous volcanic-sedimentary rocks; 5—Cretaceous granite; 6—Neoproterozoic granite; 7—Neoproterozoic diorite; 8—faults and inferred faults; 9—sampling location
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因此,有理由相信胶东地区新元古代花岗片麻岩与华北克拉通胶北地体之间主要为侵入接触关系,是后来的构造变形使两者之间多呈构造接触。
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2 胶南新元古代花岗岩中太古宙—古元古代岩石残片的构造属性
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苏鲁造山带新元古代花岗片麻岩中除存在一些榴辉岩透镜体外,还存在许多变质表壳岩、TTG片麻岩和超镁铁质岩块,主要分布于午极、海阳所、泽库、臧格庄、港西、威海西北和西南等地。变质表壳岩主要包括变粒岩、大理岩、黑云片岩、石英岩等岩石类型,有少量富铝片岩、石墨透辉变粒岩、斜长角闪岩和麻粒岩。这些变质表壳岩零星出露, 层序不完整且变质变形强烈,规模小的几米至十几米,大的有数平方千米,多以包体或残片的形式赋存于花岗片麻岩中。20世纪末,区域地质调查根据岩石组合特征通常将这些变质表壳岩与胶东岩群和荆山岩群对比,含变质基性火山岩的组合划归新太古代胶东岩群,具孔兹岩系特点的岩石组合划归古元古代荆山岩群(曹国权等, 1990;张希道和王来明, 1996;张增奇和刘明渭, 1996; 宋明春等, 2000; 王来明等, 2002)。后因新元古代花岗岩普遍被认为是识别扬子陆块属性的标志,将苏鲁造山带划归扬子陆块北缘的观点逐渐占据上风(Li et al., 1994, 2003; Wallis et al., 1999;Zheng Yongfei et al., 2004;唐俊等, 2004a; Tang Jun et al., 2008a; Zhou Jianbo et al., 2008a),其中的变质表壳岩通常不再与胶东岩群和荆山岩群对比。近几年,随着研究工作的深入,在苏鲁造山带中识别出越来越多的新太古代—古元古代的岩石(陆松年, 1998;Liou et al., 2006; 许志琴等, 2006; Zhang et al., 2006; Tang Jun et al., 2008a; Zhou Jianbo et al., 2008b; 孔庆波, 2009;Zhang Shaobing et al., 2014; Xiang Hua et al, 2014; Liu Fulai et al., 2017; 刘利双等, 2017; 徐扬等, 2017; Liu Lishuang et al., 2018a),有些记录了古元古代晚期(1.9~1.8Ga)的变质事件,包括高温—超高温麻粒岩相变质作用和中-高压麻粒岩相变质作用(翟明国等, 2000;Liou et al., 2006; Zhang et al., 2006; Xiang Hua et al., 2014; Liu Fulai et al., 2017; Xu Haijin et al., 2019; Feng Peng et al., 2020; 熊志武等, 2021)。但对于这些新太古代—古元古代岩石的原岩性质和构造属性,依然存在较大争议,部分研究者认为它们是来自扬子板块的陆壳物质(Tang Jun et al, 2008a; Xiang Hua et al, 2014);更多的学者则认为它们与华北板块具有亲缘性(翟明国等, 2000; Liou et al., 2006; Liu Fulai et al., 2017; 刘利双等, 2017; Liu Lishuang et al., 2018a; Xu Haijin et al., 2019;Feng Peng et al., 2020;熊志武等, 2021)。
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许志琴等(2006)基于北苏鲁造山带中~2.4Ga变质基底属于华北克拉通(胶辽朝地块)一部分的认识,提出了苏鲁高压/超高压陆-陆碰撞俯冲剥蚀新模式,即扬子板片在240~220Ma的深俯冲作用下拖拽上部胶辽朝地块的一部分形成了楔形俯冲剥蚀体,之后又快速折返地表。Liou et al.(2006)和Zhang et al.(2006)报道了出露于海阳所地区的古元古代(~1.85Ga)变质的麻粒岩以及~1.8Ga的花岗片麻岩,并认为该杂岩体属于胶-辽-吉地体的一部分。Liu Fulai et al.(2017)和Feng Peng et al.(2020)在海阳所地区识别出丰富的新太古代至古元古代的火成原岩,包括约2.6~2.5Ga变质镁铁质岩和2.85Ga、2.7Ga、2.55~2.5Ga及2.4Ga的TTG片麻岩;而区内变质表壳岩的沉积年龄约为2.1~1.9Ga,显示出与胶北地体的荆山岩群和粉子山群相似的原岩年龄;大量变质锆石U-Pb测年记录了海阳所杂岩遭受的古元古代晚期(约1.87~1.86Ga)和中三叠世(约245~225Ma)变质事件,以及对应的两次稍晚的退变质作用;故而认为海阳所地区的各种变质岩与胶北地体具有岩石组合、岩石学、地质年代学和P-T演化方面的亲缘性,可视为胶北地体不可分割的一部分。Liu Fulai et al.(2017)提出海阳所杂岩与苏鲁超高压变质带并置的演化模式,即在中晚三叠世扬子克拉通的俯冲过程,华北克拉通边缘的地壳物质逆冲推覆至苏鲁地体上并一同进入俯冲隧道,而后折返于地表。
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前人曾对苏鲁造山带中榴辉岩的原岩形成时代进行了诸多研究,大多数集中在800~750Ma之间(Zheng Yongfei et al., 2004, 2006; 刘福来等, 2007, 2009)。刘利双等(2017)对午极和荣成一带变基性岩的研究显示存在多种成因类型,既存在与华北板块古老变质基底相关的变基性岩,也存在与华南板块北缘新元古代裂解相关的超高压榴辉岩(Liu Lishuang et al., 2018a)。Feng Peng et al.(2020)报道有825Ma的基性岩墙侵位在~2.85Ga太古宙花岗片麻岩中,表明新元古代基性岩墙既可侵位于新元古代花岗片麻岩中,也可侵位在与胶北地体有亲缘性的太古宙TTG片麻岩中。
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本次工作,在海阳断裂东侧采集了三件测年样品,分别是海阳所南端的含石榴子石石英岩(S1801,121°38.68′E,36°44.22′N)、诸往镇东南的二长花岗片麻岩(S1819,121°44.62′E,36°53.09′N)和午极南的斜长角闪岩(S1814,121°24.41′E,36°56.60′N)。薄层状的含石榴子石石英岩(S1801)与黑云母片岩等共生,呈强烈褶皱变形的残片产于太古宙TTG片麻岩中,从中分选出的锆石在阴极发光图像上多显示出核边结构,即具岩浆结晶振荡环带的残核和浅色的环带不清晰的变质边,部分颗粒残核已消失。锆石测年数据显示有不同程度的铅丢失,具岩浆结晶振荡环带的锆石残核的测试数据构成的不一致线上交点年龄为2690±18Ma(图5a),变质锆石或锆石变质边除少量古元古代末期变质年龄数据外,主要反映出一组~2.43Ga的上交点年龄,显示可能存在太古宙末期的变质作用,但没有明显的三叠纪变质痕迹。二长花岗片麻岩样品(S1819)中的锆石主要为具振荡环带的岩浆结晶锆石,部分锆石具浅色的不完整的变质边,获得的测年数据显示有少量新太古代捕获锆石,其余测点数据构成一条不一致线,上交点年龄为1847±11Ma,下交点年龄为231±70Ma(图5b),分别代表花岗岩结晶年龄和变质改造时代,说明花岗岩形成于古元古代晚期,在中晚三叠世卷入了苏鲁造山带的碰撞造山过程。岩浆结晶年龄与Zhang Shaobing et al.(2014)采自午极地区的花岗片麻岩类似。午极南的斜长角闪岩与大理岩呈互层状产出(图6a),斜长角闪岩样品(S1814)中的锆石主要为变质成因锆石,阴极发光图像上大多数锆石展现出深色的核部和厚薄不均的浅色变质边,部分深色核部具有变质锆石所特有的冷杉状条纹。测试结果显示岩浆结晶锆石残核保留极少,测试数据可构成一条不一致线,上交点年龄为1843±14Ma(图6b),谐和度较好的8个207Pb/206Pb年龄的加权平均值为1840±16Ma,两者近于一致,代表斜长角闪岩遭受变质的时代。下交点年龄虽然误差较大,但也反映出中生代的叠加改造信息。上述三个样品的碎屑锆石年龄谱和变质年龄均反映出与胶北地块的亲缘性。
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图5 乳山地区含石榴子石石英岩(a)和黑云二长花岗片麻岩(b)的锆石U-Pb年龄
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Fig.5 Zircon U-Pb ages of garnet-bearing quartzite (a) and biotite monzonite granite gneiss (b) in Rushan area
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图6 午极镇南与大理岩共生的斜长角闪岩的锆石U-Pb年龄
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Fig.6 Zircon U-Pb age of amphibolite associated with marble in the south of Wuji
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(a)—野外照片;(b)—锆石U-Pb谐和图
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(a)—Field photograph;(b)—zircon U-Pb concodia
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从威海地区的泥质麻粒岩(Xu Haijin et al., 2019;熊志武等, 2021)到海阳所的泥质片岩(Liu Fulai et al., 2017)和午极地区的基性麻粒岩(刘利双等, 2017; Liu Lishuang et al., 2018a)及本文与大理岩共生的斜长角闪岩都被证明它们是相当于荆山岩群的古元古代地质体,均记录了古元古代末期的变质作用和~230Ma的变质作用改造。
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纵观整个北苏鲁地区,除榴辉岩和超镁铁质岩的原岩多数为新元古代的基性岩外,绝大多数变质表壳岩和TTG片麻岩都是太古宙—古元古代的产物,与胶北地块变质基底具有明显亲缘性。大小各异的、大量太古宙—古元古代的岩石残块“漂浮在新元古代花岗片麻岩的海洋中”,特别是米山断裂以西没有遭受高压—超高变质的地区,很难用构造混杂来解释。因此有理由相信这些新元古代花岗岩是侵入到胶北地块的变质基底中的。
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3 胶北地块新元古代年龄信息
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胶北地块中存在大量的新元古代的年龄信息,唐俊等(2004b)曾报道在胶北莱西市南墅粉子山群橄榄大理岩中测得残留锆石核部岩浆结晶年龄(769±48Ma、786±67Ma)和变质年龄(215±34Ma、240±44Ma),被解释为三叠纪华北-扬子大陆碰撞造山过程中北苏鲁超高压变质带物质逆冲推覆到胶北地块之上 (Tang Jun et al., 2006)。
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胶北地块上招远地区的晚侏罗世玲珑花岗岩,早在20世纪末就有报道晚侏罗世岩浆结晶锆石中存在新元古代的残核(苗来成等, 1998)。随着胶东成为世界瞩目的金矿矿集区,许多学者对胶东的中生代花岗岩开展了大量岩石成因及其与金成矿关系的研究。其中的玲珑花岗岩也引起了岩石与矿床研究者的广泛关注,许多学者从玲珑花岗岩的岩石学、锆石年代学、全岩Sm-Nd、锆石Hf和氧同位素等方面探讨了花岗岩的成因及其构造背景(Zhang Juan et al., 2010; Yang Kuifeng et al., 2012; Jiang Neng et al., 2012; Ma Liang et al.2013; 黄涛等, 2014;Yang Liqiang et al., 2017)。
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笔者也曾在大柳行和桃村一带采样,样品S1714采自大柳行南齐家沟金矿附近(120°59′30″E, 37°33′32″N),S1811采自桃村东曲家村附近(121°14′50″E, 37°9′33″N)。两个样品的锆石U-Pb年龄谱大体相似,分别给出了168±3Ma和164±3Ma的成岩年龄,另有一组分别为704±8Ma和755±13Ma的新元古代的残余锆石年龄,以及少量太古宙—古元古代的继承锆石(图7)。桃村样品中755~210Ma之间的年龄数据没有明确的地质意义,很大程度上是新元古代锆石改造的结果。但两个样品中古老残余锆石有所差别,大柳行南样品主要为太古宙的锆石,而桃村南的样品中主要为古元古代的锆石,指示源区岩石组成有所不同。
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Zhang Juan et al.(2010) 研究认为玲珑花岗岩和昆嵛山花岗岩均来自太古宙—古元古代大陆地壳的部分熔融。岩石具有类似于现代埃达克岩的地球化学特征,较低的MgO、Ni含量和Mg#值,表明其来源于俯冲增厚大陆地壳的部分熔融,而非拆沉的下地壳。玲珑花岗岩和昆嵛山花岗岩中均出现新元古代残余锆石U-Pb年龄,锆石Hf模型年龄指向太古宙—古元古代,认为其来源与华南陆块具有构造亲缘性,也包含有来自华北陆块的古老地壳物质,推测是两个碰撞大陆之间造山根的部分熔融。Yang Kuifeng et al.(2012) 也认为胶北地块西北部晚侏罗世玲珑和栾家河花岗岩为过铝质、LREE富集、HFSE亏损、Sr/Y值较高,εHf(t)值较低,形成于相对高压条件下,可能来自加厚太古宙下地壳的部分熔融。
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Jiang Neng et al.(2012) 对比研究了玲珑花岗岩6个样品的继承锆石年龄的O和Hf同位素组成,两个含有~2.5Ga继承锆石和高δ18O岩浆锆石的样品被解释为主要来自华北克拉通的下地壳;其余四个样品含有丰富的新元古代继承锆石,其δ18O和εHf(t) 类似于苏鲁造山带高压变质岩中的新元古代锆石,因此认为岩浆源区主要来自华南陆块的俯冲大陆地壳。六个样品的岩浆锆石的δ18O和εHf(t) 均表明没有地幔衍生岩浆的贡献,而εHf(t) 和δ18O则反映了源区的不均匀性。
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图7 玲珑花岗岩的锆石U-Pb年龄谐和图
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Fig.7 Zircon U-Pb age concordance of Linglong granite
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(a)—大柳行齐家沟;(b)—桃村东南
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(a)—Qijiagou, Daliuhang; (b)—southeast of Taocun
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Ma Liang et al.(2013)的研究显示玲珑花岗岩中存在四组继承锆石,年龄峰值分别为~208Ma、~750Ma、~1800Ma和~2450Ma。地球化学研究表明玲珑花岗岩与埃达克岩有一定的相似性,具较高的初始87Sr/86Sr比值(0.7097至0.7125),较低的εNd(t) (-20.3~-17.7)和可变锆石εHf(t) (-22.2~-8.7)值,也认为岩浆源于加厚下地壳的部分熔融,没有任何地幔成分的贡献。Yang Liqiang et al., (2017) 根据玲珑花岗岩的高Ba-Sr、全岩εNd(t) (-22.4~-10.9)和εHf(t)值(-39.1~-1.5)变化范围大等特征,认为玲珑花岗岩的岩浆是由胶北地体和苏鲁地体含石榴石、角闪石的和富碱的下地壳部分熔融形成;动力学机制是在古太平洋岩石圈向西俯冲背景下,板块回滚诱发的软流圈上升流引起;岩浆上升过程中与不同的老地壳相互作用导致花岗岩中存在许多太古宙至早中生代的继承锆石。
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以上研究结果几乎均认可玲珑花岗岩在成因上具有华南陆块的印记,是三叠纪华北与华南板块陆-陆碰撞造山带根部下地壳部分熔融的产物。所谓的华南陆块的印记主要是新元古代的岩浆作用以及指向古元古代的锆石Hf模式年龄。
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但存在两个令人困惑的问题,一是玲珑花岗岩作为增厚大陆地壳部分熔融的产物,没有地幔物质的贡献,只能推测是华南陆块(扬子克拉通)的大陆地壳俯冲到华北陆块(华北克拉通)的大陆地壳之下,而没有壳幔相互作用;但超高压变质岩的折返指示大陆地壳曾经俯冲到地幔深部,不可能俯冲到胶北地块的地壳与地幔之间。二是胶北地块上没有发现三叠纪的岛弧岩浆岩,这也被认为是板块陡俯冲的证据;如果华南陆块曾经俯冲到招远一带胶北地块大陆地壳之下,理应存在俯冲板片的脱水熔融,导致弧岩浆作用。
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因此,有理由怀疑胶北地块深部的新元古代岩浆岩地壳并非华南陆块的俯冲大陆板片,很可能是华北克拉通东南部大陆在新元古代伸展裂解时形成的隐伏岩体,岩浆源区主要是古元古代胶-辽-吉造山带的深部地壳物质。
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4 胶北地块大陆边缘三叠纪的俯冲作用
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前人对华北-扬子板块的俯冲极性和方式、高压/超高压岩石变质作用和折返过程等进行了诸多研究,主流观点认为扬子板块俯冲到华北板块之下,后期折返与逆冲使苏鲁超高压变质地体推覆到华北板块之上(Okay et al., 1992; Yin et al., 1993;Li, 1994; Lin and Li 1995;Xu Peifen et al., 2002)。也有学者认为是扬子板块北向俯冲拽动华北板块边缘俯冲(许志琴等, 2006, 2007;Liu Fulai et al., 2017)。但近年来,逐渐有研究者(Li Sanzhong et al., 2017;郭润华等, 2017;李三忠等, 2017;郑洪伟等, 2020)认为华北与扬子板块碰撞的俯冲极性可能相反,不是扬子板块的向北俯冲,而是华北板块向东南俯冲。Li Sanzhong et al.(2017) 基于大陆边缘地层学、弧岩浆作用缺乏、北苏鲁超高压变质地体中存在大量胶北地块基底残片及~1.85Ga的变质作用记录、高压-超高压岩片构造样式等的综合分析,提出了一个华北板块南向俯冲至大华南板块之下形成巨型弯山构造的新模式。如果是华北板块俯冲,就是以新元古代花岗片麻岩为主构成的大陆边缘先行俯冲,随后是胶北地块主体俯冲。
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4.1 胶北地块俯冲的地球物理信息
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前人对胶东及附近区域做过大量地球物理研究工作。Xu Peifen et al.(2002)依据地震层析成像结果解译苏鲁造山带之下P波速度结构具有复杂的“鳄鱼嘴式”形态,扬子板块上、下地壳拆离,华北板块速度异常体楔入其中。横穿诸城凹陷的南北向反射地震剖面揭示(吴冲龙等, 2006),苏鲁造山带北侧边界附近中上地壳中存在着三层结构:上部的胶莱盆地沉积盖层,中部的苏鲁楔状地体和下部代表华北板块的胶北地块基底。苏鲁楔状地体中发育一组向北仰起的叠瓦状逆冲断层,而胶北地块显示出向南俯冲的态势,提出可能存在着华北板块与扬子板块相向俯冲于苏鲁地体之下的陆—陆碰撞机制。Yang Wencai(2009)利用天然地震的S波震相的层析成像结果给出了上地幔S波速度扰动精细图像,显示苏鲁超高压变质带下方上地幔破碎带包含多个有序排列的高速团块,向东南倾斜,推测与扬子板块俯冲、以及前锋超高压变质块体拆沉及折返作用有关;但从图像上看,也可以解释为东南向倾斜的高速体为华北板块(郑洪伟等, 2020)。通过对地壳上地幔结构层析成像研究,郑洪伟等(2020)认为北苏鲁地区存在华北板块向东南俯冲的模式。
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在胶东地区的航磁异常图上(图8),沿即墨—海阳—乳山—荣成一线为明显的正磁异常,与五莲-青岛-荣成断裂带基本一致,即墨-牟平断裂带明显切割了这一正磁异常带;桃村断裂在航磁图上可明显识别出牙山岩体与院格庄岩体的左行错断。在重力异常图上(贺春艳等, 2021),海阳-荣成断裂位于正负异常的过渡带,即墨-牟平断裂带中依然是桃村断裂最为清晰。根据航磁和重力资料解译,Wu Qifan et al.(2003)认为苏鲁高压—超高压变质岩之下存在华北板块的磁性体。在区域重磁异常图上(胥颐等, 2009;郝天珧等, 2010, Li Chunfeng et al., 2012; Liu Qingsheng et al., 2015),胶东半岛南侧的千里岩隆起带与陆地上苏鲁造山带具有相似的重磁异常分布,可以认为千里岩隆起带是苏鲁超高压变质带在海域上的延伸。陈建文等(2020)认为在地震剖面中千里岩隆起之下具有明显的莫霍面反射,至南黄海盆地之下莫霍面反射消失,而根据陆域地区深反射地震剖面的结果,北侧华北板块的莫霍面反射强度同样比扬子板块内莫霍面反射更强,因此,推测千里岩隆起带深部莫霍面与扬子板块无关,可能为华北板块物质。
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图8 胶东地区航磁异常图(标示了主要断裂构造)
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Fig.8 Aeromagnetic anomaly map of Jiaodong area (the main faults marked)
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地球物理研究者多认可五莲-青岛-荣成断裂带是华北板块与苏鲁造山带的深部边界(刘光鼎, 1992;郝天珧等, 2004, 2010;胥颐等, 2009; 岳保静等, 2014),至少在千里岩隆起之下是俯冲的华北板块。但对地表露头界线仍有争议。徐扬等(2015)研究认为苏鲁超高压变质带与华北克拉通结晶基底在浅层的界线对应着即墨-牟平断裂带的地球物理踪迹,而在深部,苏鲁造山带下面隐伏有华北板块的地壳物质,华北陆块基底和苏鲁超高压变质带在深部界线与青岛—荣成重磁异常带的位置相吻合。实际上即墨-牟平断裂带是晚中生代的断裂构造,错断了青岛—荣成的磁异常带,也切割了新元古代花岗片麻岩与荆山岩群的岩性分界线,真正的地表露头界线应在牟平南侧,而且是花岗片麻岩倾伏于荆山岩群变质岩之下。
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4.2 胶北地块三叠纪俯冲的变质作用记录
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胶北地块上自变质基底到中新元古代盖层均遭受了不同程度的三叠纪变质作用改造。
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李广旭等(2016) 对采自胶北桃村断裂北西侧粉子山群和荆山岩群的4个(石榴)云母片岩样品中独居石及金红石的U-Pb同位素年代测定,揭示出胶北粉子山群和荆山岩群不仅经历了古元古代(1869~1864Ma)变质事件,而且还经历了三叠纪(218~215Ma)变质变形事件的叠加。通过金红石中Zr温度计计算得出对应变质温度为:658~680℃,表明胶北地块部分卷入了三叠纪苏鲁-大别超高压变质带的俯冲-碰撞造山过程,并遭受了角闪岩相变质作用叠加。曹汇(2016)对采自烟台东炮台西粉子山群的3个云母片岩样品中的独居石测年,获得了232~229Ma的U-Pb年龄,也认为胶北地块参与了三叠纪向下的俯冲过程。
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Liu Lishuang et al.(2018b) 采用LA-ICP-MS U-Pb测年、CL图像分析、锆石矿物包裹体的激光拉曼分析和白云母Ar-Ar测年相结合的研究方法,有效地区分了荆山岩群在古元古代(1.94~1.88Ga)和早中三叠世(252~244Ma)期间的两次变质事件,认为荆山岩群在古元古代参与了胶-辽-吉带造山事件,并在早中三叠世参与了华北克拉通与华南陆块之间的俯冲-碰撞事件,遭受了低角闪岩相变质作用。并提出沿五莲-即墨-牟平断裂带西北侧存在一条多期变质带。
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唐俊等(2004b)曾对采自南墅的粉子山群不纯大理岩中锆石SHRIMP测年,认为锆石U-Pb不一致线下交点年龄215±34Ma代表变质年龄,解释该大理岩可能是三叠纪碰撞造山后被推覆到胶北地块之上(Tang Jun et al., 2006)。
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除胶北地块变质基底卷入了三叠纪的变质变形外,其上的沉积盖层蓬莱群和芝罘群也遭受了不同程度的变形变质改造。
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新元古界蓬莱群主要出露于栖霞、蓬莱以及北部沿海长山岛等岛屿上,角度不整合覆盖在胶北地块的变质基底上,遭受了较强烈变形和低绿片岩相变质作用,主要变质岩石类型包括板岩、石英岩和大理岩等。朱光(1993)认为蓬莱群的变质作用与华北板块与扬子板块沿胶南带汇聚事件相关;Faure et al.(2001) 和Li Xianghui et al.(2007)认为蓬莱群是苏鲁造山带的推覆体。从栖霞到长山岛蓬莱群变质程度有逐渐减弱的趋势,在长山岛上蓬莱群辅子夼组石英岩展现出近水平的倒转层序(初航等, 2011;陆松年等, 2012),表明褶皱构造异常强烈,具有俯冲前陆的变形特征。
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中元古界芝罘群集中分布于烟台市区北部芝罘岛、崆峒岛等岛屿上,与新太古代花岗片麻岩呈被改造的角度不整合覆盖关系,芝罘群底部层位中保存有变质含砾砂岩和变形的交错层理(图9a)。笔者在下伏的新太古代花岗片麻岩中获得了一组2476±35Ma的不一致线上交点年龄,从芝罘群长石石英岩中获得的一组最年轻碎屑锆石年龄为1664±34Ma。芝罘群遭受了强烈韧性变形和角闪岩相的变质作用,出现白云母、钾长石、十字石、蓝晶石、夕线石、橄榄石(橄榄大理岩)等典型变质矿物,其中的基性岩墙也遭受强烈的变形变质作用而变为斜长角闪黑云片岩(图9b),局部残留有透辉石。最高变质温压条件达到0.65~0.80GPa和700~750℃(薛志忠等, 2001),变质矿物组合及变质相与烟台粉子山群云母片岩和莱西荆山岩群云母片岩遭受的三叠纪变质作用相当(李广旭等, 2016;Liu Lishuang et al., 2018b)。芝罘群长石石英岩中分选出的碎屑锆石阴极发光图像上虽能观察到不完整的浅色变质边,但未能获得有效变质年龄。而变质基性岩中分选出的锆石则均显示出变质锆石的特点,Th/U比值均＜0.08,阴极发光图上纹理不清晰,不同的程度地保存有古老锆石残核。测试数据构成的不一致线上、下交点年龄分别为208±11Ma和1841±35Ma(图10a),可分别代表古元古代末和晚三叠世的构造热事件。其中下交点附近的几个测试数据构成的不一致线下交点年龄为209±9Ma,最接近谐和线的测点206Pb/238U年龄为219±3Ma(图10b)。指示芝罘群卷入了晚三叠世华北克拉通与扬子克拉通的碰撞造山事件。
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此前,Liu Fulai et al.(2014) 曾报道辽东长海县岛屿上辽河群岩石中独居石U-Pb和白云母39Ar-40Ar定年获得了中—晚三叠世变质作用年龄数据(236.1~218.2Ma),该期变质事件与苏鲁-大别造山带的高压—超高压变质事件(235~220Ma)同时代。因此推测,华北克拉通东南缘的变质作用与华北克拉通和扬子克拉通中—晚三叠世碰撞有关,苏鲁高压-超高压变质带可能已延伸到辽东长海变质杂岩南侧。实际上,在大连一带出露的新元古代永宁群和金县群岩石也遭受了轻微的变质作用改造,粉砂岩的褶皱构造中出现了轴面劈理。由此可见,卷入三叠纪苏鲁造山带的华北大陆边缘范围将更宽广,整个胶北地块乃至包括长海县等岛屿在内的辽东半岛南部边缘都有可能纳入造山作用影响范围,展现出俯冲的被动陆缘变质变形特征。
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图9 烟台芝罘群变质长石石英砂岩中的交错层理(a)和强烈褶皱(b)
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Fig.9 Cross bedding (a) and strong folding (b) in metamorphic feldspathic quartz sandstone of the Zhifu Group, Yantai
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图10 芝罘群变质基性岩墙(样品15SD01-2)的锆石U-Pb年龄(a、b)
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Fig.10 Zircon U-Pb age (a, b) of metamorphic basic dike of the Zhifu Group in Yantai
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5 讨论
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5.1 华北克拉通东南缘新元古代岩浆活动的构造归属
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胶东地区的新元古代花岗岩形成时代界于780~700Ma之间(Ames et al., 1996; Zhou et al., 2003;唐俊等, 2004a; Zheng Yongfei et al., 2004; Hacker et al., 2006; 刘福来等, 2007;李向辉等, 2007;Tang Jun et al., 2008a, b; 王世进等, 2009; Zhang Shaobing et al., 2014; 侯建华等, 2016)。岩石成因较为复杂,包括I型、S型和A型等花岗岩类型,多数花岗质片麻岩具有髙钾钙碱性花岗岩特征,构造环境判别具有大陆弧花岗岩—同碰撞花岗岩性质,A型花岗岩则属后造山花岗岩系列(孙景贵等, 1997;薛怀民等, 2006, 2007;宋明春等, 2007),与同时代的基性岩(Zheng Yongfei et al., 2004;刘福来等, 2007, 2009)总体上构成双峰式火成岩组合。
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锆石Lu-Hf同位素特征(李向辉等, 2007; Tang Jun et al., 2008b; 刘福来等, 2009; Liu Fulai et al., 2010)显示,北苏鲁新元古代岩浆岩具有多来源性。多数花岗片麻岩锆石的εHf(t)为负值,其中一部分εHf(t)为-17~-15、tTDM2为2.9~2.7Ga, 一部分εHf(t)为-9~-7、tTDM2为2.25~2.05Ga,反映这些花岗岩来自新太古代(2.9~2.7Ga)和古元古代(2.25~2.05Ga)古老陆壳在新元古代时期的部分熔融。少量花岗片麻岩具有正的εHf(t)值(平均约为2.5),变化范围在-0.56至6.6之间,其中部分锆石的两阶段Hf模式年龄为0.94~0.81Ga(李向辉等, 2007; Tang Jun et al., 2008b),表明花岗片麻岩原岩在晚元古代形成时,有幔源岩浆底侵导致上覆太古宙—古元古代地壳物质重熔。李向辉等(2007)对威海—荣成一带花岗片麻岩的全岩Sm-Nd同位素研究也揭示荣成超高压地体的平均地壳形成年龄主要为古元古代。
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根据花岗片麻岩的锆石Hf同位素和全岩Nd同位素特征,前人研究多将花岗片麻岩的源区指向扬子陆块基底,但胶北地块也具有这种基底结构,胶北地块主要由新太古代TTG片麻岩和古元古代胶-辽-吉造山带构成,特别是靠胶北地块东南侧的胶-辽-吉造山带中存在自2.2Ga以来的多期双峰式岩浆活动(董春艳等, 2010; 刘平华等, 2013; 田京祥等, 2018; 王惠初等, 2021),造山带深部存在较广泛的幔源岩浆活动。
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自中元古代以来,华北克拉通经历过多期多阶段的裂解(翟明国等, 2014; Zhai Mingguo et al., 2015;耿元生等, 2020;相振群等, 2020),其中华北克拉通东南部徐淮—胶辽新元古代裂陷带中记录了~0.9Ga和~0.83Ga的基性岩浆活动(杨进辉等, 2004; Wang Qinghai et al., 2012;韩吉龙和王清海, 2015;Zhang Shuanhong et al., 2016; Zhu Renzhi et al., 2019),海阳所地区存在~0.83Ga基性岩墙侵入~2.85Ga太古宙花岗片麻岩中(Feng Peng et al., 2020)。在朝鲜半岛中南部地区存在~0.9Ga、~0.83Ga和~0.75Ga多期新元古代的花岗岩和双峰式火山岩(Lee et al., 1998, 2003, 2020;Peng Peng et al., 2011a; Kim et al., 2013; Oh et al., 2018)。朝鲜半岛的构造归属虽然还存在一定争议,但大多数研究者认为朝鲜半岛整体上属于中朝板块(翟明国等, 2007; Zhai Mingguo et al., 2007; 万天丰, 2001; Chang et al., 2001; Ishiwatari et al., 2001;Hao Tianyao et al., 2002, 2007),苏鲁造山带向东延伸绕过朝鲜半岛。翟明国等(2007)研究认为朝鲜半岛的3个地块(狼林、京畿和岭南地块)具有与华北克拉通相似的岩石组合与演化历史,南北朝鲜两个主要的古生代沉积盆地与华北具有很好的可比性(翟明国等, 2007; Zhai Mingguo et al., 2007, 2019)。郝天珧等(2004)对黄海及周边地球物理场特征研究认为朝鲜半岛的重力场特征与南黄海地区有较大差异,南黄海与朝鲜半岛分属于不同的地质构造单元,南黄海属于下扬子块体,而朝鲜半岛属于中朝块体。
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胶北新元古代蓬莱群的碎屑锆石记录了不同于扬子北缘的中元古代强烈的岩浆活动(Li Xianghui et al., 2007; Zhou Jianbo et al., 2008c; 初航等, 2011; 陆松年等, 2012; 王宏宇等, 2021),蓬莱群碎屑锆石主要为岩浆锆石,年龄峰值集中在~1.1Ga、~1.2Ga以及~1.6Ga。区域上,蓬莱群物源特点与朝鲜祥原超群,以及我国辽东细河群、鲁南土门群、徐淮地区淮南群等华北东南缘新元古代沉积盆地物源相似,物源主要来自华北克拉通以外的古陆(王宏宇等, 2021)。板块重建研究显示与胶北地块拼合的陆块很可能是发育格林威尔期造山带的刚果-圣弗兰西斯科克拉通(Peng Peng et al., 2011b; Peng, 2015; Cederberg et al., 2016; Xu Huiru et al., 2017; de Andrade et al., 2020)。这表明华北克拉通东南缘在新元古代之前并非大陆边缘,是新元古代时期的大陆裂解导致其与类似于刚果-圣弗兰西斯科克拉通这样的大陆分离。因此在华北克拉通东南缘出现新元古代双峰式岩浆活动并不意外。
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另一方面,华南陆块新元古代岩浆活动主要形成于830~820Ma前裂谷阶段和780~740Ma同裂谷阶段, 相伴有同时期的基性岩浆作用,属于典型的双峰式岩浆活动(Li et al, 2003; Geng et al., 2020),这些新元古代岩浆活动被认为与地幔柱引起的Rodinia超大陆的裂解有关(Li et al., 2003)。但在北苏鲁造山带中并未见到扬子陆块克拉通化过程中弧岩浆活动的迹象,也无广泛的830~820Ma的前裂谷阶段的岩浆活动。目前扬子克拉通上780~700Ma的岩浆活动主要出现扬子北缘和西缘,如果北缘的这期岩浆活动构造归属存疑,那么华南陆块上780~700Ma的岩浆活动并不普遍。
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如果不将新元古代花岗岩作为识别扬子克拉通属性的标志,那么对肥东杂岩和其中的BIF铁矿的构造归属(Ye Hui et al., 2017; 涂城等, 2021)就会提出疑问,肥东群中的BIF铁矿可能不是扬子克拉通的太古宙铁建造,而是可以与霍邱和蚌埠一带的BIF铁矿对比,肥东杂岩乃至其北北东方向延伸的张八岭群的构造归属都值得进一步研究。
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5.2 苏鲁造山带的构造配置
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胶东地区超高压榴辉岩的分布仅限于米山断裂带以东,高压-超高压变质单元并不与胶北地块直接接触。翟明国等 (2000) 曾以米山断裂、荣成断裂和石岛断裂为界将北苏鲁变质带由南向北划分为海阳所变质地块(榴辉岩化扬子陆块基底变质单元)、荣成变质地块(超高压变质单元)、威海变质地块(麻粒岩相叠加变质的超高压构造岩片)和昆嵛山边界杂岩带等4个岩石构造单元。可以归并为威海-荣成超压变质单元和昆嵛山非超高压变质单元,两者之间以米山断裂为界。
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胶北地块与昆嵛山杂岩带之间被即墨-牟平断裂带分隔。昆嵛山边界杂岩带中未见典型的榴辉岩;刘利双等(2017)报道在午极地区有退变榴辉岩(或高压麻粒岩)透镜体产于新元古代花岗片麻岩中。前文已述,即墨-牟平断裂带主要由桃村、郭城、朱吴及海阳等大致平行、走向约北东40°~45°的断裂组成,断裂面倾向东南或西北,倾角一般较陡(70°~80°),以至在同一条断裂不同地段出现反向倾斜现象。张岳桥等(2007)认为即墨-牟平断裂带在晚中生代经历了从晚侏罗世挤压左旋走滑平移、到早白垩世引张伸展、再到晚白垩世-古新世右旋走滑拉分的转变过程。沿断裂带分布的新元古代花岗片麻岩的片麻理走向与断裂走向大体一致,明显受断裂带控制,但在昆嵛山杂岩带北段龙泉—初村一带,花岗片麻岩的产状总体呈北东东走向,向北北西中等角度(20°~50°)倾斜;在南段的乳山—海阳所一带,产状与之相近,均与海阳断裂有一定的交角。
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米山断裂东侧的威海-荣成超高压岩片,含榴辉岩的新元古代花岗片麻岩的片麻理产状呈向东南突出的弧形展布;泽库至荣成一带,片麻理走向由近东西向转为北东向;文登至威海一带,片麻理走向由北东向转为近南北向,至威海北部转为北西向。伴随片麻理发育一系列韧性剪切带,片麻理均向外(向东-南东-南南东方向)中等角度倾斜,不同程度地发育一组倾向线理。这一弧形构造带很可能是原来北东走向的构造带被北西走向的韧性剪切带(威海—马道)左行剪切滑动影响的结果。蔡志慧等(2009)对荣成一带的构造解析认为该弧形构造带伴随的韧性剪切系统是超高压岩片折返挤出后,早白垩世伸展滑脱作用的构造形迹。泽库—荣成一带在航磁图上展示出负异常(图8),预示着这一带的新元古代花岗片麻岩仅仅是浅部的残片,深部可能是中生代花岗质岩石。
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青岛-海阳-荣成断裂带走向NE至近EW向延伸,可延伸到荣城以东的海域,该断裂带被后期NE向即墨-牟平断裂带切错。依据地球物理资料,青岛-海阳-荣成断裂是具岩石圈深度的深大断裂(刘光鼎, 1992),该断裂带向南陡倾(Li Chunfeng et al., 2012; Zou Zhihui et al., 2016; Zhao Weina et al., 2019)。在区域布格重力异常图中(郝天珧等, 2010; Liu Qingshen et al., 2015; 陈建文等, 2020),重力异常具有明显的分带性,青岛-海阳-荣成断裂带南侧的千里岩隆起区,重力异常呈北东—北东东向条带状断续分布,重力异常值为20~40mGal,其异常特征可以向西追索到苏鲁超高压变质带所在的位置。在海区重力异常剖面中,千里岩隆起与南北两侧盆地重力异常具有强烈差异,反映千里岩隆起带位于扬子-华北板块碰撞结合带位置(陈建文等, 2020)。
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沿海阳—荣成展布的航磁异常带对应荣成超高压岩片,而连云港-千里岩隆起的重力高异常带对应的是日照-千里岩超高压岩片,指示两个超高压岩片的物质组成有所不同。
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在海区地震剖面上(陈建文等, 2020),千里岩隆起与南黄海盆地之间界线明显,接触边界由一系列断续南倾反射组成,推测是断层面的反映,断层向下延伸,并在深度20km附近断层倾角变缓,向南黄海盆地基底内部延伸,展现出拆离带特征(对应嘉山-响水断裂)。断裂两侧深部地壳差异明显,地震测深资料表明北西侧地壳厚度达30km以上,而东南侧仅20km。重磁综合解译(Liu Qingshen et al., 2015),连云港-千里岩断裂和嘉山-响水断裂均向东南倾斜。陆地上的长丰—湖州地震剖面(Lü Qingtian et al., 2015)也揭示嘉山-响水断裂是向南东倾斜的断裂构造。地表露头上,海州群内目前保存着造山带折返期变形组构,面理向南东缓倾,矿物拉伸线理向南东倾伏,皆为上盘向北西的运动学特征(赵田等, 2014)。构成苏鲁造山带的几个高压-超高压单元呈向南东倾斜的岩片叠置产出。许志琴等(2007)对横穿苏鲁高压—超高压变质带地震反射剖面(Yang Wencai,2002)也重新解释为一系列向南东倾斜的逆冲岩片。为解释苏鲁造山带的这种结构模式,前人提出了多种碰撞造山模型(Okay et al., 1992; Yin et al., 1993;Li, 1994; Lin et al., 1995; 许志琴等, 2007;Li Sanzhong et al., 2017),其中最具代表性的是“鳄鱼嘴”式的上下地壳拆离模型。超高压岩片折返到地表浅部时,造山带已进入到构造松弛阶段,是什么动力学机制使上下地壳拆离?如果构成造山带的几个主要超高压构造单元在物质成分上与华北克拉通具有亲缘性,那么就是华北板块物质俯冲到地壳深部,是华北克拉通俯冲到扬子克拉通之下,不需要特殊的构造模型。这样苏鲁造山带就有可能由胶北地块俯冲岩片(米山断裂以西)、威海-荣成超高压逆冲岩片和日照-千里岩超高压逆冲岩片和张八岭-海州高压岩片构成(图11),代表俯冲缝合线的蛇绿混杂岩带可能在造山带的南侧。西大别南缘印支期吕王-高桥-永佳河构造混杂岩带的确定(徐扬等, 2021)为这一构想提供了支持。
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图11 苏鲁造山带简单结构模型
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Fig.11 Simple structural model of Sulu orogenic belt
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6 初步结论
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(1)五莲-即墨-牟平断裂带并非北苏鲁超高压变质带与胶北地块的初始接触界线,胶东地区新元古代花岗岩与华北克拉通胶北地块最初应为侵入接触关系,在三叠纪华北与华南板块陆-陆碰撞造山过程中遭受了强烈的变形改造。
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(2)北苏鲁超高压变质带的新元古代花岗片麻岩中存在大量胶北地块的地壳物质,包括太古宙的TTG片麻岩和少量变质表壳岩、古元古代的荆山岩群变质表壳岩和古元古代晚期的花岗片麻岩,并记录了~1.85Ga的华北克拉通化变质事件。五莲群中碎屑锆石年龄谱指示了华北克拉通的物质属性,尤其是~2.15Ga的锆石年龄信息是胶-辽-吉造山带中岩浆作用的标志。
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(3)胶北地块上晚侏罗世花岗岩中存在大量新元古代继承锆石,甚至在辽东地区中生代岩体中也存在许多新元古代继承锆石,但缺少三叠纪的弧岩浆记录。而且,胶东地区晚侏罗世花岗岩来源于加厚地壳的部分熔融,没有地幔物质添加或壳幔物质交换的证据,难以用华南板块陆壳物质俯冲到胶北地块陆壳之下解释,也与北苏鲁超高压变质带的深俯冲作用相悖。
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(4)胶北地块东南缘普遍存在三叠纪角闪岩相变质事件,不仅发生在变质基底的粉子山群和荆山岩群的岩石中,而且在沉积盖层芝罘群和蓬莱群中也有体现,指示胶北地块在三叠纪遭受了变形变质作用的改造。变质程度从东南向北西有逐渐减弱的趋势,结合地球物理信息,显示胶北地块三叠纪发生了向东南的俯冲作用。
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(5)北苏鲁新元古代花岗岩岩石成因较为复杂,包括I型、S型和A型等花岗岩类型。锆石Hf同位素和全岩Nd同位素特征显示多数花岗片麻岩来自新太古代和古元古代古老陆壳物质的部分熔融。新元古代花岗岩以古元古代为主的模式年龄并非一定将岩浆源区指向扬子克拉通基底,胶北地块也具有这种物质结构,特别是胶-辽-吉造山带中存在自2.2Ga以来的多期双峰式岩浆活动。因此,不赞成将新元古代花岗岩视为识别扬子陆块属性的标志。
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致谢:本文成文过程中,万渝生研究员、李三忠教授、刘正宏教授和刘福来研究员提出了许多中肯意见和建议,在此致以衷心感谢!谨以此文纪念程裕淇院士诞辰110周年,追思程先生对地质科学,特别是前寒武纪地质学的杰出贡献。
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注释
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❶ 山东省地质调查院.2003.烟台市幅(1∶25万)区域地质调查报告.
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摘要
苏鲁超高压变质带广泛发育新元古代花岗片麻岩,这些新元古代花岗片麻岩通常被认为与扬子克拉通具有亲缘性。本文基于新的调查资料,综合前人研究成果,提出新元古代花岗岩是华北克拉通新元古代时期大陆裂解产物、并在三叠纪华南与华北碰撞造山期间作为华北板块大陆边缘南向深俯冲的新认识。主要依据如下:① 新元古代花岗岩与华北克拉通胶北地块为侵入接触关系,五莲-即墨-牟平断裂带并非北苏鲁超高压变质带与胶北地块的初始接触界线;② 新元古代花岗片麻岩中有大量胶北地块的古老地壳物质,记录了~1.85 Ga的华北克拉通化变质事件;③ 胶北地块上晚侏罗世花岗岩中存在大量新元古代继承锆石,但缺少三叠纪的弧岩浆记录;④ 胶北地块东南缘存在三叠纪角闪岩相变质作用证据,指示胶北地块三叠纪的俯冲作用;⑤ 区域地球物理信息指示北苏鲁超高压变质带深部地壳属于华北克拉通和北东东向构造线方向。新的认识将有助于对华北克拉通新元古代构造演化和大别-苏鲁造山带形成过程的重新认识,为胶东中生代金成矿作用提供新视野。
Abstract
Neoproterozoic granitic gneisses are widely developed in the Sulu UHP metamorphic belt, which are commonly considered to have affinity with the Yangtze Craton. Based on new survey data and previous researches, this paper puts forward a new insight that the Neoproterozoic granites were the product of the continental breakup of the North China Craton in the Neoproterozoic, which deeply subducted southward as the continental margin of the Jiaobei Terrane during the Triassic collision between the South and North China blocks. Several lines of evidence are shown as follows: ① The Neoproterozoic granites intruded into the metamorphic rocks of the Jiaobei Terrane of the North China Craton, and the Wulian-Jimo-Muping fault zone is not the initial boundary between the North Sulu UHP Metamorphic Belt and the Jiaobei Terrane. ② The Neoproterozoic granitic gneisses contain a large amount of crustal rocks from the Jiaobei Terrane, recording the cratonization event of ~1.85 Ga in the North China Craton. ③ There is no Triassic arc magmatic record in the Jiaobei Terrane, but abundant Neoproterozoic inherited zircons have been identified in the Late Jurassic granites. ④ It is evident that the southeastern margin of the Jiaobei terrane underwent Triassic metamorphic event of amphibolite facies, consistent with Triassic subduction. ⑤ Regional geophysical information indicates that the deep crust of the North Sulu UHP metamorphic belt belongs to the North China Craton and its NE trending tectonic direction obliquely cut by the Wulian-Jimo-Muping fault. The new consideration will improve understanding the Neoproterozoic evolution of the North China Craton and the formation process of the Dabie-Sulu metamorphic belt, providing a new perspective for Mesozoic gold mineralization in the Jiaodong Peninsula.
