2016, Vol. 32
2. 云南地质工程勘察设计研究院, 昆明 650041;
3. 安徽大学资源与环境工程学院, 合肥 230601
2. Yunnan Institute of Geological Engineering Survey and Design, Kunming 650041, China;
3. School of Resources and Environmental Engineering, Anhui University, Hefei 230601, China
众所周知，华北与华南板块在中三叠世发生碰撞造山，两者之间形成了著名的秦岭-大别-苏鲁造山带(Zhang et al., 2009; Wu and Zheng， 2013)，并且大别和苏鲁造山带被郯庐断裂带大规模左行错开(图 1; 朱光等， 2006，2009; Zhu et al., 2009; Niu et al., 2015)。郯庐断裂带起源于华北与华南板块的碰撞造山过程中已被多数学者所认同(Lin and Fuller， 1990; Yin and Nie， 1993; Chang，1996; 万天丰和朱鸿，1996; Gilder et al., 1999; 肖文交等，2000; 张岳桥和董树文，2008; Zhu et al., 2009; 朱光等， 2004，2009)，但是其起源方式以及这两大板块的碰撞过程却长期存在着不同的认识。介于大别与苏鲁造山带之间的郯庐断裂带张八岭隆起段，显然是揭示这些重要问题的关键地带，具有重要的研究价值。
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图 1 郯庐断裂带中-南段及其周缘地质简图 Fig. 1 Geologic sketch map of the middle-southern segments of the Tan-Lu Fault Zone and its adjacent areas |
郯庐断裂带张八岭隆起段构成了西侧华北板块与东侧扬子板块之间的断裂边界，正确认识该段断裂带的深部结构也是理解其起源方式的重要方面。然而，前人在这方面却存在着很大的认识上分歧，分别有陡立的走滑边界(Zhang et al., 1984; Watson et al., 1987; 张岳桥和董树文，2008; Zhu et al., 2009)、撕裂断层边界(Li，1994)、西倾的俯冲板块边界(Lin and Fuller， 1990; Yin and Nie， 1993; Gilder et al., 1999; 肖文交等，2000; Xu et al., 2002b)、深部华北地壳向东挤入的“鳄鱼咀”样式(Su et al., 2013)等观点。这些不同的观点反映了人们对该断裂带起源及华北与华南板块碰撞方式截然不同的认识。正确认识该断裂带的深部结构显然是解决这些认识上分歧的重要突破口。
岩浆活动能够将深部地质信息带至地表，壳源岩浆中的锆石U-Pb年龄及地球化学特征往往记录了丰 富的地壳属性与演化信息(Hartmann，2001; Wu et al., 2008; Wang et al., 2011; Zhang et al., 2015a)。本文利用张八岭隆起带及旁侧出露的晚中生代岩浆岩的继承锆石年龄数据，再结合地球化学与地球物理资料，讨论其深部的岩浆源区属性与特征，综合分析该断裂带的深部结构，为理解其起源方式提供重要的信息。
2 地质背景郯庐断裂带张八岭隆起段也称为张八岭隆起带，是华北和华南板块之间特殊的板块构造边界，也是郯庐断裂带在大别和苏鲁造山带之间出露的部位(图 1)，断裂带平面上将两大造山带左行错开约550km。该隆起带总体呈NNE向展布，其西侧为华北板块上的合肥盆地，两者浅部以西倾的控盆正断层为界；其东侧为扬子板块(华南板块北部)上的下扬子前陆变形带。
2.1 张八岭隆起带概况张八岭隆起带总体上是一个变质岩出露带，带内主要出露低级变质的张八岭群和高级变质的肥东杂岩(图 2)。以北纬32°为界，张八岭隆起带大致可以分为南、北两段。其北段主要出露张八岭群，而南段主要出露肥东杂岩(在肥东杂岩东侧也有零星张八岭群出露)。张八岭群可以分为下部的西冷组和上部的北将军组，两者在剖面上自下而上变质程度逐渐降低(Zhang et al., 2007)。其中西冷组主要为一套中-高绿片岩相的中-酸性变火山岩，其原岩主要为流纹岩、安山岩与凝灰岩，原岩时代为748~754Ma(Zhao et al., 2014)；北将军组主要是低绿片岩相的浅变质碎屑岩，以千枚岩与浅变质砂岩为主。肥东杂岩主要为一套低-中角闪岩相的高级变质岩(张青等，2008; 石永红等，2009; 聂峰等，2014)，包括黑云斜长片麻岩、角闪斜长片麻岩、斜长角闪岩、角闪岩组成的正变质岩和白云石大理岩、云母片岩组成的副变质岩两大系列，肥东杂岩内正变质岩的原岩时代为800~745Ma(Zhao et al., 2014)。张八岭群与肥东杂岩变岩浆岩的新元古代原岩时代显然指示它们属于扬子板块的岩石(Zhao et al., 2014)。
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图 2 张八岭隆起带北段地质图及采样位置(据Zhang et al., 2007; 张青等，2008修改) Fig. 2 Geologic map of the northern Zhangbaling uplift belt，showing sampling localities(modified after Zhang et al., 2007，2008) |
此外，在张八岭隆起带北段，张八岭群东侧还依次出露有震旦系、寒武系和奥陶系(图 2)。其中下震旦统的岩性和变质程度(低绿片岩相)皆与北将军组类似，自下而上为周岗组(Z1z)千枚岩和浅变质粉砂岩、砂岩，苏家湾组(Z1s)含砾千枚岩、千枚岩等浅变质冰碛岩系。上震旦统自下而上为未变质的陡山沱组(Z2d)泥岩、泥灰岩与灰岩，灯影组(Z2d)白云岩。寒武-奥陶系地层为未变质的碳酸盐岩夹碎屑岩。这些震旦-奥陶系也明显指示属于扬子板块海相盖层。
张八岭隆起带为一个多期叠加的构造变形带，记录了郯庐断裂带的多期活动。在隆起带北段，张八岭群与下震旦统中主要发育上盘向SSW运动的印支期平缓韧性滑脱构造(Lin et al., 2005; Zhang and Teyssier， 2013; Zhao et al., 2014)，其面理产状平缓而多变，局部有晚期(晚侏罗世)脆性平移断层的叠加。在隆起带的南段，其北部广泛发育晚侏罗-早白垩世初NNE向左行走滑韧性剪切带，早期构造被完全置换；而南部同期NNE向走滑韧性剪切带局部存在，其间仍保留有早期NEE-SWW向组构(Zhu et al., 2005; Zhao et al., 2014)。
早白垩世时期，中国东部开始进入大规模伸展构造背景之下，张八岭隆起带及周缘受区域伸展活动的控制(Zhu et al., 2010，2012)，发育了断陷盆地和大规模的岩浆活动(图 1)。在张八岭隆起带的西缘，发育了NNE走向、西倾的大型正断层，控制了旁侧合肥盆地的发育。在张八岭隆起带北段东侧，还发育有早白垩世滁州火山岩盆地(谢成龙等， 2007，2009; 马芳和薛怀民，2011)和滁州岩体，而其西缘自北向南依次发育了早白垩世管店岩体、瓦屋刘岩体和瓦屋薛岩体(牛漫兰，2006; 资锋等，2008; Liu et al., 2010; 曹洋等，2010; 周力等，2014)。在张八岭隆起带的南段，也发育有一系列早白垩世花岗质岩体(牛漫兰等， 2008，2010; Liu et al., 2010)，并有局火山岩出露。此外，在巢湖中庙至南岸的庐江地区，沿郯庐断裂带也零星分布有一些早白垩世火山岩(谢成龙等， 2008a，b)。
2.2 岩浆岩发育特征张八岭隆起带北段的滁州火山岩盆地，位于滁州市的西部，出露面积约80km2，呈NNE向展布(图 2)。盆地西部直接覆盖在震旦系灯影组之上，南部和东部不整合在下古生界地层之上，上部局部见上白垩统张桥组红层。该套火山岩分为上、下两个组。下部红花桥组以河湖相沉积为主，夹陆相中基性火山岩，厚度达260m；上部黄石坝组以陆相火山岩为主，夹河湖相沉积，厚度达2200m。火山岩类型主要包括安山岩、粗安岩、英安岩、辉石安山岩等，并有大套的安山质凝灰岩发育(谢成龙等，2009)，其喷发时限为132~116Ma(谢成龙等，2007; 马芳和薛怀民，2011)。
张八岭隆起带北段西侧的管店岩体、瓦屋刘岩体和瓦屋薛岩体，皆以狭长带状平行于张八岭隆起带西缘呈NNE向展布(图 2)。岩体侵位于张八岭群变质岩中，与围岩侵入接触关系清晰，其中瓦屋刘岩体西侧和瓦屋薛岩体东侧主要为白垩纪红层覆盖。野外工作发现这些岩体未受郯庐走滑剪切带的影响，且受后期构造变形和破碎作用影响较小。这些岩体的岩石类型包括二长岩、石英二长岩和花岗岩等。管店岩体、瓦屋刘岩体和瓦屋薛岩体的侵位年龄分别为132Ma(资锋等，2008)、128Ma和120Ma(牛漫兰，2006)。最近在瓦屋刘岩体南端新发现的藕塘岩体，可能为瓦屋刘岩体的一部分，其侵位年龄为129~125Ma(Hu et al., 2014)。
张八岭隆起带南段的晚中生代岩体，零星出露于南部的肥东杂岩中(图 3)，主要分布在锦张村、黑虎山、白马山、尖山、永丰水库、西花村、西徐村北等地。这些侵入体沿郯庐断裂带呈北北东向展布，岩体和变质岩的侵入接触关系明显。往往以岩株或小岩体的形式产出，主要岩石类型为二长花岗岩和正长花岗岩，其岩体侵位年龄为127~103Ma(牛漫兰等，2008)。
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图 3 张八岭隆起带南段地质图及采样位置 Fig. 3 Geologic map of the southern Zhangbaling uplift belt，showing sampling localities |
庐江段火山岩带主要发育于巢湖中庙至庐江万山镇一带，该地区也发育有张八岭群变质岩，因而可以看作是张八岭隆起带在巢湖以南的延伸部分。该火山岩带介于下扬子区的庐枞火山岩盆地与大别山北侧的北淮阳火山岩带之间，呈串珠状沿郯庐断裂带的西边界呈NNE向分布(图 4)，指示火山喷发明显受郯庐深大断裂的控制。该处火山以喷溢作用为主，火山机构明显，为一系列独立的火山锥，主要岩石类型包括流纹岩、粗面岩和玄武岩、碱玄岩等，具有典型的双峰式火山岩的特征，火山喷发时间为125~93Ma(谢成龙等，2008b)。
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图 4 郯庐断裂带庐江段地质图及采样位置 Fig. 4 Geologic map of the Lujiang segment of the Tan-Lu Fault Zone，showing sampling localities |
上述沿张八岭隆起带分布的晚中生代岩体或火山岩盆地，多数呈NNE向展布，或沿NNE向呈串珠状分布。野外观测发现，这些岩浆岩本身并未受到区内广泛发育的NNE向左旋走滑构造所切割，指示岩浆活动发生于晚侏罗世-早白垩世初区域大规模走滑活动之后。锆石定年结果表明岩浆活动时间在132~93Ma之间，指示为早白垩世期间的岩浆活动产物。野外岩浆岩展布方位显示岩体侵位与火山喷发明显受NNE向的张八岭隆起带控制，为隆起带之下的地壳或壳-幔混源的岩浆产物(谢成龙等， 2008a，2009; 资锋等，2008; Liu et al., 2010; 牛漫兰等，2010; Su et al., 2013)，岩浆活动记录了深部的源区属性与演化信息。
3 样品特征与分析方法 3.1 样品特征本文所选样品分别采自张八岭隆起北段滁州火山岩盆地(简称滁州火山岩)、南段早白垩世岩体和庐江段火山岩带(简称庐江火山岩)。对这些岩浆岩样品进行LA-ICP MS锆石U-Pb年代学测试，获取了岩体侵位年龄和火山喷发年龄，同时发现这些岩浆岩样品中往往含有大量的继承锆石。对其中部分样品进行了古老继承锆石的测年工作，获取了继承锆石的年龄数据。
滁州火山岩未见明显的变形、变质现象，样品均较新鲜。本次所选样品均为红色至暗灰色致密块状火山熔岩，所有样品均为斑状结构或似斑状结构，斑晶含量较低。基质多为细小的长石新晶和玻璃质构成，二者共同组成玻晶交织结构，有时呈粗面结构。测试中选择样品TLC04、TLC05和TLC10进行了继承锆石的年代学分析工作。其中TLC04为粗面岩、TLC05为英安岩、TLC10为粗安岩。
张八岭隆起南段岩体主要为花岗岩类，样品皆未遭受明显矿化和蚀变。所采集定年样品中，TLF02和TLF06为二长花岗岩，TLF03、TLF09和TLF11为正长花岗岩。这些样品皆为块状构造，具细粒花岗结构、似斑状结构或花岗结构。样品中主要矿物包括酸性斜长石、钾长石、石英及少量的黑云母组成，副矿物主要为磷灰石、锆石、榍石、褐帘石和磁铁矿等。
庐江段火山岩的岩性差异较大，本次进行继承锆石年代学分析的样品包括2个粗面岩样品(TLL03、TLL04)和1个玄武岩样品(TLL06)。样品TLL03具斑状结构(斑晶含量<4%)，斑晶为透长石、斜长石和少量角闪石，基质为大量碱性长石和少量石英组成的粗面结构或间隐结构。样品TLL04具斑状结构、流动构造，斑晶主要为透长石和斜长石，基质为隐晶质或玻晶交织结构，主要为大量细小的石英和长石颗粒。TLL06具斑状结构，基质为粗玄结构；斑晶含量较少(低于3%)，主要为少量的斜长石、辉石、橄榄石和磁铁矿，基质主要由大量斜长石微晶、似长石类、辉石及少量磁铁矿、玻璃质等组成。
3.2 分析方法所选样品的锆石U-Pb定年工作采用LA-ICP MS法完成，分为选样、制靶、阴极发光照相、上机测试和数据后处理5个步骤。对野外采集的岩石样品经碎样机破碎后，采用浮选和电磁选等方法分离出单颗粒锆石，并在双目镜下手工挑纯以除去其他副矿物。然后选择晶形完好、无裂隙、色泽度好的锆石颗粒粘于环氧树脂表面，固化后抛光至锆石露出三分之二左右，进行透射光和反射光照相，依据照相结果选择晶型特征良好的锆石进行阴极发光照相，以了解锆石内部结构。上述选样工作在河北省区域地质矿产调查研究所实验室然完成，制靶和阴极发光照相工作在中国科学院地质与地球物理研究所实验室完成。
根据阴极发光照射结果，选择环带结构清晰的锆石颗粒进行U-Pb年代学测试，该工作在西北大学大陆动力学实验室完成的。其中ICP-MS 主机型号为PE公司的Elan 6100DRC，配套的激光剥蚀系统为GeoLas 200M深紫外193nm ArF 准分子激光剥蚀系统。测试中采用激光斑束直径为30μm，年龄外标采用哈佛大学标准锆石91500。
测试数据的后处理工作利用Glitter(4.0版)软件进行，普通铅校正采用Andersen方法(Andersen，2002)进行，年龄分析及成图采用Isoplot(Ver.3.70)进行(Ludwig，2012)。测试中的误差标准为1σ，具体的实验流程参见袁洪林等(2003)和Yuan et al.(2004)。
4 分析结果本次所分析张八岭隆起带上的晚中生代岩浆岩，除庐江段的玄武岩和流纹岩样品未见古老锆石外，其余样品皆含有古老继承锆石。这些继承锆石大多具有较高的自形程度(庐江段火山岩中继承锆石普遍遭受显著熔蚀而呈浑圆状或不规则状，且普遍具有变质壳)，多为短柱状或长柱状，轴比在3：2~3：1之间，明显比新生岩浆锆石粗大，多为无色或浅黄色，透明度较高。阴极发光照相显示，这些锆石多具有清晰的内部结构(图 5)，往往发育岩浆振荡环带，并具有典型的核幔结构，且往往具有多期岩浆核(有时为变质核)，核部常为半自形-他形，其外部一般具有较薄的增生边，内部有时存在暗色包体。对上述继承锆石进行年代学分析，共获取了110个分析点的有效数据(表 1)。
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图 5 张八岭隆起带晚中生代岩浆岩中部分继承锆石阴极发光图 Fig. 5 Some cathode luminescence(CL)images of selected inherited zircons in the Late Mesozoic igneous rocks from the Zhangbaling uplift zone |
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表 1 张八岭隆起带晚中生代岩浆岩中继承锆石U-Pb年代学分析结果 Table 1 Inherited zircon U-Pb geochronology data for the Late Mesozoic igneous rocks from the Zhangbaling uplift belt |
本次分析的锆石样品中，所有分析点获得的锆石Th/U比值中，仅有1个点小于0.2，大多数分析点的Th/U值在0.5以上(表 1)，且所分析锆石岩浆环带清晰，指示这些继承锆石多为岩浆成因(Belousova et al., 2002; Hoskin and Schaltegger， 2003)，为早期地壳演化的产物。所获得年龄数据中(大于1.0Ga的锆石取207Pb/206Pb年龄，小于1.0Ga的锆石取206Pb/238U年龄)，各分析点的谐和度绝大部分在80~110之间，表明年龄数据较谐和(Gee et al., 2015; Tsunogae et al., 2015)，可信度较高。
张八岭隆起北段滁州火山岩样品获得的38个继承锆石年龄中，除1个分析点的年龄较小外(757±4Ma)，其余皆大于1.9Ga，主要分布在2.0~2.5Ga之间(表 1、图 6a-c、图 7a)，还有少数锆石具有3.0Ga以上的年龄，其中最大的年龄为3281Ma。南段岩体样品中，由于新生岩浆锆石数量较多、颗粒较大，因而其中的继承锆石比例较小，5个花岗岩样品中仅获得9个继承锆石的有效数据。这9个数据的锆石年龄皆大于1.0Ga(表 1、图 7b)，除1颗锆石具有1.3Ga年龄外，其余8个点年龄均在2.2~2.6Ga之间。庐江段火山岩样品中共获取63个继承锆石分析数据，其中样品TLL03(图 6d)和TLL04(图 6e)中的继承锆石年龄主要分布于0.5~3.1Ga和0.2~2.6Ga之间，最大年龄分别为3091Ma和2646Ma，并含有新元古代和三叠纪年龄信息(表 1)。庐江段样品TLL06(图 6f)以含有大量新元古代锆石为特征，13个点的年龄在624~748Ma之间，另有1颗锆石还具有209Ma的年龄。
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图 6 张八岭隆起带晚中生代岩浆岩单样品继承锆石年龄频率分布图 Fig. 6 Frequency distribution of inherited zircon ages of the Late Mesozoic igneous rocks along the Zhangbaling uplift belt |
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图 7 张八岭隆起带各区段晚中生代岩浆岩继承锆石年龄频率分布图 Fig. 7 Frequency distribution of inherited zircon ages of the Late Mesozoic igneous rocks along each parts of the Zhangbaling uplift belt |
放射性同位素是记录地壳多期演化的有效载体，其中Sr、Nd、Pb、Hf、O等同位素是最常用的地壳演化示踪剂。然而，由于岩浆混染、混合及新生地壳物质的加入等因素的影响，全岩同位素体系在示踪地壳演化中往往具有不确定性，且无法识别出精细的地壳多阶段演化过程(刘富等，2009; Ali et al., 2015; Kröner et al., 2015)。由于锆石具有较高的结晶温度和热稳定性，在地壳演化中能够很好的保存下来，因而是示踪大陆地壳演化的最佳研究对象，利用锆石中的Hf-O同位素组成、U-Pb年龄均能有效识别关键的地壳演化阶段和过程(Zhang et al., 2006a; Wu et al., 2008; 焦文放等，2009)，其中继承锆石U-Pb年龄记录的信息最为直观和丰富，已成为研究大陆地壳演化阶段、鉴别陆壳属性的最重要手段之一(Hartmann，2001; Wang et al., 2011; Zhang et al., 2012; Huang et al., 2013; Liu et al., 2013)。
华北与华南板块在前印支期具有不同的地壳演化历史，因而具有显著不同的地壳物质特征。华北板块具有较老的地壳生长和再造历史，普遍出露有太古宙地壳岩石，具有高达3.8Ga的古老锆石年龄(吴福元等，2005)，并具有~3.2Ga、~2.5Ga、~1.8Ga等主要时间段的锆石年龄，对应于华北陆壳增生与再造的几个关键阶段(Zhao et al., 2004; Zheng et al., 2004; 沈其韩等，2005; 刘敦一等，2007; Grant et al., 2009; 刘富等，2009; 万渝生等，2010; 董春艳等，2010; 第五春荣等，2012; Diwu et al., 2013; Liu et al., 2013; 胡波等，2013; Wang et al., 2014a，2014b; Shan et al., 2015)。华北板块以~2.5Ga为最主要年龄阶段，2.7Ga以上的锆石尽管存在但比例偏少(沈其韩等，2005; 刘敦一等，2007; Grant et al., 2009)，并缺乏新元古代锆石年龄信息。
关于华南板块，早期的研究认为较为缺乏太古宙-古元古代年龄信息，往往以含有大量新元古代锆石年龄信息为特征(Wu et al., 2006; Zhang et al., 2006b; Zheng et al., 2007; Wang et al., 2015)。新元古代锆石年龄信息已广泛被当作识别华南板块的标志(Wu et al., 2012; 薛怀民等，2012; Yang and Zhang， 2012; Yang et al., 2014)。然而，近十余年来，华南板块上陆续发现了大量太古宙锆石(Zhang et al., 2006b; Zheng et al., 2006; Zheng and Zhang， 2007; 焦文放等，2009; Tang et al., 2012; Zhang and Zheng， 2013; Guo et al., 2014; Li et al., 2014c; Wang et al., 2015; Zhao et al., 2015)，因而目前普遍认为华南板块也具有太古宙基底。另外，华南板块上古元古代锆石也不断被报道，指示也经历过古元古代(~2.0Ga)地壳生长事件(Zhang et al., 2006a; Zheng et al., 2007; 彭敏等，2009; Tang et al., 2012; Zhang and Zheng， 2013; Wang et al., 2015)。但是，尽管华南板块也具有古老的地壳基底年龄信息，其分布特征却与华北板块具有较大的差异。在扬子陆块发现的太古宙-古元古代锆石年龄谱中，~2.5Ga锆石年龄与~2.0Ga、~2.9Ga年龄往往具有大致相当的分布比例(Zheng and Zhang， 2007; Zhang and Zheng， 2013)，或者缺乏~2.5Ga锆石年龄信息(Tang et al., 2012; Li et al., 2014a)；而华北板块则以~2.5Ga为最主要的峰值年龄(沈其韩等，2005; Grant et al., 2009; Shi et al., 2012; Liu et al., 2013; Shan et al., 2015)，其比例明显高于其他阶段年龄信息。
5.1.1 张八岭隆起北段位于张八岭隆起带北段东侧的滁州火山岩，3个样品中的继承锆石年龄皆在~2.5Ga附近分布最广，且形成最强的概率分布峰值(图 6a-c、图 7a)，显示具有华北地壳古老锆石的年龄分布特征(沈其韩等，2005; Grant et al., 2009; Shi et al., 2012; Liu et al., 2013; Shan et al., 2015)。各样品小于2.5Ga的数据在谐和图上形成了不一致线，指示这些锆石曾在1.8Ga时经历过华北板块标志性的峰期变质事件(Zheng et al., 2004; 董春艳等，2010; Liu et al., 2013)而发生了铅丢失。在TLC04样品中，还发现一颗新元古代(757±4Ma)的锆石。由于滁州火山岩发育于张八岭隆起东侧，其下伏地层包括了原岩时代为新元古代(Zhao et al., 2014)的张八岭群和肥东杂岩，推断该颗新元古代锆石为岩浆喷发过程中于浅部捕获的扬子陆壳锆石。此外，滁州火山岩具有低的εNd(t)值(-22.8~-13.4)、低的放射性成因Pb(其中206Pb/204Pb(t)=15.896~16.689、207Pb/204Pb(t)=15.273~15.417、208Pb/204Pb(t)=36.170~37.00)等特征(谢成龙等，2009)，也指示其源区属于华北板块(Liu et al., 2010; Su et al., 2013; Yang et al., 2014)。综上所述，滁州火山岩虽地表位于扬子板块上，但其具有华北地壳岩浆源区特征。
张八岭隆起带北段西缘的晚中生代瓦屋刘、瓦屋薛和管店岩体，也以含大量太古宙-古元古代继承锆石，但未发现新元古代锆石(牛漫兰未发表数据)，也指示源区为华北陆壳。张八岭隆起带北段晚中生代岩体皆以低的全岩εNd(t)值(-18~-12)、低的全岩放射性成因Pb和低的锆石εHf(t)值(-26~-16)为特征(资锋等， 2007，2008; Liu et al., 2010; 曹洋等，2010; Su et al., 2013; Wang et al., 2013; Yang et al., 2014)。这些特征显示张八岭隆起带北段晚中生代岩体与同期滁州火山岩一样，皆具有华北下地壳源区特征(Su et al., 2013，图 8a、图 9a，b、图 10a)。值得指出的是，部分学者依据华北和下扬子地壳在同位素特征上有重叠区域而认为不能依此判别块体属性(Zeng and Yan， 2014)。但是，从晚中生代岩浆岩的大量统计数据来看，华北和扬子板块(下扬子区)同位素重叠区域较小(图 8、图 9、图 10)，因而从统计学的角度仍然能够有效区分岩浆的源区归属。
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图 8 张八岭隆起带各区段晚中生代岩浆岩全岩εNd(t)值分布图 下扬子地区Nd同位素数据引自Chen et al., 2001; Xu et al., 2002a; 王元龙等，2004; Wang et al., 2003，2004，2006; 谢智等，2007; 袁峰等，2008; Li et al., 2009; Hou et al., 2010; 薛怀民等， 2009，2010; 赵海杰等，2010; 王斌等，2012; Xie et al., 2012; 闫峻等， 2005，2012; Su et al., 2013; 汪晶等，2014；华北板块Nd同位素数据巫祥阳等，2003; 杨进辉等，2003; Zhang et al., 2004; 胡芳芳等，2005; 杨德彬等，2006; 李全忠等，2007; 闫峻和陈江峰，2007; Liu et al., 2012; Yang et al., 2004，2010，2012; 柯昌辉等，2013; Li et al., 2014b；张八岭隆起带Nd同位素数据引自Chen et al., 2001; 童劲松等，2008; 资锋等， 2007，2008，2011; 谢成龙等， 2008a，b，2009; Liu et al., 2010; 牛漫兰等， 2002，2010; Su et al., 2013 Fig. 8 Distribution diagrams of εNd(t)values for the Late Mesozoic igneous rocks along the Zhangbaling uplift belt |
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图 9 沿张八岭隆起带不同区段晚中生代岩浆岩全岩206Pb/204Pb(t)、208Pb/204Pb(t)值分布图 数据来源参见图 8中Nd同位素数据部分文献及闫峻等(2003) Fig. 9 Distribution diagrams of 206Pb/204Pb(t) and 208Pb/204Pb(t)values for the Late Mesozoic igneous rocks along the Zhangbaling uplift belt |
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图 10 张八岭隆起带不同区段晚中生代岩浆岩锆石εHf(t)值分布图 下扬子地区Hf同位素数据刘园园等，2009; 侯可军和袁顺达，2010; 胡劲平和蒋少涌，2010; Wu et al., 2012; Yang and Zhang， 2012; 李瑞玲等，2012; 闫峻等，2012; 张俊杰等，2012; Su et al., 2013; Wang et al., 2013；华北板块Hf同位素数据胡芳芳等，2005; 徐义刚等，2007; 杨德彬等， 2006，2007; 郭波等，2009; Liu et al., 2012; 高昕宇等，2012; 林博磊和李碧乐，2013; 刘跃等，2014；张八岭隆起带Hf同位素数据资锋等，2008; Su et al., 2013; Wang et al., 2013 Fig. 10 Distribution diagrams of zircon εHf(t)values for the Late Mesozoic igneous rocks along the Zhangbaling uplift belt |
位于张八岭隆起南段的晚中生代岩体，所获取的仅有的9个继承锆石年龄数据中，主要为古元古代早期年龄信息(2.2~2.5Ga)，仅有一颗锆石具有中元古代年龄(1.3Ga)，且未见新元古代锆石年龄信息(表 1)。这些锆石年龄在~2.5Ga附近形成概率分布峰值(图 7b)，指示其岩浆源区可能为华北板块。该处岩体具有较低的全岩εNd(t)值(-25~-12)、锆石εHf(t)值(-23~-18)和全岩放射性成因Pb等特征(Liu et al., 2010; 牛漫兰等，2010; Su et al., 2013; Wang et al., 2013)，也与华北板块内部同期岩浆岩类似，而与下扬子地区同期岩浆岩高Pb、高εNd(t)、高εHf(t)的特征明显不同(图 8b，9c，d，10b)。然而，最近在该带早白垩世岩脉中发现大量新元古代锆石(未发表数据)，指示部分岩浆岩也具有扬子地壳源区的特征。因而，我们认为张八岭隆起南段晚中生侵入岩可能兼具有华北和扬子板块的岩浆源区。
5.1.3 庐江段庐江段火山岩位于巢湖南岸至庐江之间，属于张八岭隆起带的南延部分。该带3个火山岩样品中，皆含有大量的新元古代锆石(图 6d-f、图 7c)，指示为扬子地壳源区。样品TLL03和TLL04中还含有古元古代-太古宙锆石年龄(图 6d，e)，其中样品TLL04缺乏~2.5Ga年龄信息，也表明该样品具有扬子陆壳源区特征。而TLL03样品在2.5Ga附近形成最强分布峰值，指示其可能还兼有华北陆壳源区的特征。样品TLL06中含有新元古代继承锆石(年龄皆小于800Ma)，但不含古元古代-太古宙锆石，也指示源区属于扬子陆壳。而在全岩Nd、Pb同位素分布图上(图 8c、图 9e，f)，庐江火山岩样品除落入典型的下扬子岩浆岩区及其与华北板块的叠置区域外，也有部分样品落入华北岩浆源区内，表明部分火山岩可能还含有华北源区特征。
此外，作为大别造山带东北缘的庐江段，其中样品TLL04和TLL06中还具有209Ma和237Ma的中、晚三叠世年龄信息(图 7、图 8)。样品TLL03还具有211Ma的不一致线交点年龄。这些皆指示庐江火山岩的岩浆源区还遭受了印支期造山事件的影响。这些特征与大别-苏鲁造山带内的同期岩浆岩具有相似性(赵子福等，2013)。但是，北部的张八岭隆起带南段与北段则均未发现印支期造山事件年龄信息。
综上所述，沿张八岭隆起带分布的晚中生代岩浆岩显示了不同的岩浆源区属性。其北段具有华北地壳岩浆源区特征，南段兼有华北和扬子地壳源区特征，而更南部的庐江段则明显具有扬子地壳源区特征(部分样品可能受后期走滑事件影响而卷入有华北源区物质)。
5.2 主边界断层产状张八岭隆起带浅部所出露变质的张八岭群与肥东杂岩，原岩主要为火山岩或侵入岩，具有新元古代年龄(图 11，Zhao et al., 2014)，属扬子板块岩石。因而，该带浅部扬子与华北板块的边界位于隆起带西缘。西侧华北板块浅部的合肥盆地，充填了厚达8km的侏罗-古近系(Zhu et al., 2009)，下伏古生代海相盖层。由此可见，该隆起带西侧华北板块在上地壳为低电阻率的沉积层，而隆起带本身为高电阻率的正变质岩，从而可以利用电法剖面有效地识别出华北与扬子板块之间的边界产状及其变化。
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图 11 张八岭隆起带变质岩中锆石年龄频率分布图 数据来源据Zhao et al., 2014; 赵田等，2014 Fig. 11 Frequency distribution of zircon ages for metamorphic rocks from the Zhangbaling uplift belt |
胜利油田完成的三条张八岭隆起带电法剖面分别切过北段、南段与庐江段(图 12)。这些剖面显示现今郯庐断裂带的主边界断裂位于张八岭隆起西缘，代表了华北与扬子板块的断裂边界。该边界带浅部为西倾的盆缘正断层，局部见(图 12)盆地反转期逆冲断层的切割。而在浅部正断层之下，该主边界断层在电法剖面上明显呈现为高、低阻体之间的界线，代表了深部(上地壳范围内)华北与扬子板块之间的边界状态。这三条不同位置的电法剖面，显示了边界断面产状沿走向上发生了明显的变化。在张八岭隆起带北段(图 12a，EMAP365线，E-W向剖面)，主边界断层表现为向SE倾斜、断面倾角中等，指示深部华北板块作为下盘向东显著延伸至张八岭隆起带所在的扬子板块之下。在张八岭隆起带南段(图 12b，EMAP340线，E-W向剖面)，主边界断层也向SE倾斜，但断面倾角明显变陡，地震剖面也清楚的反映了这一特征(Zhang et al., 2015b)。在南部庐江段(图 12c，EMAP748，S-N向剖面)，主边界断层转变为向NW倾斜，且断面倾角陡立，在张八岭隆起之下不再有华北陆壳的插入。
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图 12 张八岭隆起带EMAP电法二维连续介质反演剖面解释及其位置图(据董波等，2005; Zhang et al., 2015b) Fig. 12 2D continuum inversion EMAP electrical profiles across the Zhangbaling uplift belt(after Dong et al., 2005; Zhang et al., 2015b) |
上述电法剖面清楚地显示了张八岭隆起带西缘华北与扬子板块边界断层的产状及其空间变化。该产状由北部向SE中等倾斜、中部向SE陡倾转变为南端向NW陡倾(图 13)。这种陡倾的特征及倾向的变化与斜向汇聚边界相吻合。而其北部倾角变缓可能与接近苏鲁造山带而受影响所致。
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图 13 郯庐断裂带张八岭隆起段产状变化示意图 Fig. 13 Attitude variation model for the Zhangbaling uplift segment of the Tan-Lu Fault Zone |
需要说明的是，尽管电法剖面反映的是张八岭隆起带现今的地壳结构状况，但区域上印支造山运动以后的构造事件主要为晚侏罗世期间滨太平洋构造域下的NNE向的左行平移活动，该构造事件对晚三叠世的构造形迹并未产生根本性破坏，地表露头构造现象清楚的记录了两者的叠加关系。因而现今的地壳结构应能大致代表印支期以来的总体地壳结构状况。
5.3 深部结构与岩浆源区变化的原因尽管上述电法剖面涉及的地壳深度仅有15km(上地壳)，但各剖面下部边界断层稳定的产状可以推断其在下地壳与岩石圈地幔内应具有相似的状态。郯庐断裂带已有的大量地球物理勘探及其对幔源岩浆的控制(朱光等，2002)，指示其应切穿了整个岩石圈。作为华北与扬子板块之间的边界断层，郯庐断裂带也应是岩石圈断裂。
通过对比分析发现，上述电法剖面揭示的地壳深部结构信息，与晚中生代岩浆岩继承锆石揭示的信息相吻合，不但揭示了岩浆源区沿走向上变化的原因，也共同限定了张八岭隆起带的深部结构。电法剖面显示张八隆起南段与北段郯庐主边界断层皆向SE倾(图 13)，并且向北倾角变缓。这一深部结构使得张八岭隆起带浅部为扬子地壳，而深部为华北地壳，从而下地壳源区就为华北地壳(图 14)。随着向SE倾的主边界产状变陡，会出现华北与扬子下地壳源区的并置。张八岭隆起北段晚中生代岩浆岩显示的华北地壳源区及南段显示的华北与扬子地壳源区的混合显然与其产状北缘缓南陡相吻合。该板块边界断层在庐江段转变为向NW陡倾，从而该段深部皆为扬子地壳，并与其中晚中生代岩浆岩显示扬子陆壳源区相吻合。由此可见，正是由于郯庐边界断层在深部产状的变化，导致了深部结构的变化，从而造成了岩浆源区的相应变化。
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图 14 郯庐断裂带张八岭隆起北段示意剖面与岩浆源区模式图(位置见图 12d) Fig. 14 Schematic cross-section and magma source model for the northern Zhangbaling uplift segment of the Tan-Lu Fault Zone(location seen in Fig. 12d) |
通过本次工作的综合分析，显示郯庐边界断层产状沿走向上出现了明显变化，并且总体以陡倾为特征。这一产状特征不支持其为西倾俯冲边界(Xu et al., 2002b)或“鳄鱼咀”式边界(Su et al., 2013)观点。这一倾向与倾角的较大变化与典型的平移断层特征(如陆内转换断层)也不吻合，平移断层一般具有产状陡立而稳定的特征。该边界总体陡立且产状多变的现象与斜向汇聚边界特征相吻合。斜向汇聚边界的走滑运动使其产状陡立，但常利用原始边界而发育又使其会产状多变。由此可见，郯庐断裂带的深部结构支持其印支期属于华北与扬子板块之间的斜向汇聚边界，与前人提出的华北与扬子板块的嵌入式碰撞模式(Yin and Nie， 1993)或嵌合式碰撞模式(Zhao et al., 2014)相吻合。
张八岭隆起带变质岩属于被错移的大别造山带岩片还是扬子板块边缘上原地的岩层以往也存着不同的观点(Xu et al., 1987; Xu and Zhu， 1994; 张青等，2008)。最近Zhao et al.(2014)通过其中变岩浆岩的锆石定年及其与上覆地层年代与变形上的连续性，认为它们属于扬子板块边缘原地变形、变质的岩层，代表了斜向汇聚边界上的变形-变质带。本次晚中生代岩浆岩继承锆石分析发现，张八岭隆起南、北段皆没有三叠纪的继承锆石，与大别造山带内同期岩浆岩内大量三叠纪继承锆石形成鲜明对照(陈道公等，2001; Zhao et al., 2007; Liu and Liou， 2011; 赵子福等，2013; Chen et al., 2015)。这也支持张八岭隆起变质岩属于扬子板块边缘原地变质岩层的观点。而庐江段三叠纪继承锆石的存在应是其紧邻大别造山带的结果。
6 结论(1)继承锆石年龄分布特征特征表明，张八岭隆起带北段晚中生代岩浆源区为华北下地壳；南段兼有华北与扬子地壳源区特征；而隆起带以南庐江段则以扬子地壳源区为特征。晚中生代岩浆岩的Nd-Pb-Hf同位素特征也支持这一观点。
(2)锆石年龄反映的地壳结构信息，也得到了电法剖面的印证。电法剖面揭示，华北与扬子板块之间的郯庐断裂深部边界具有变化的产状。张八岭隆起北段向SE中等倾斜，南段向SE陡倾，而更南部庐江段侧转变为向NW陡倾。这种板块边界产状决定了张八岭隆起带之下具有华北地壳，而庐江段之下皆为扬子地壳，从而导致了晚中生岩浆源区的相应变化。
(3)郯庐断裂深部产状特征，支持其印支期应为斜向汇聚边界，符合华北与扬子板块的嵌入式碰撞模式。张八岭隆起带上晚中生代岩浆岩内三叠纪继承锆石的缺失也支持其为斜向汇聚边界，并指示隆起带上变质岩应为扬子板块西缘原地变形、变质岩层。
致谢 感谢中国科学院地质与地球物理研究所马玉光、毛骞等，西北大学第五春荣、戴梦宁等为分析测试工作提供的大量帮助。野外工作得到了向必伟和胡召齐博士的帮助，审稿人在审稿过程中付出了辛勤的劳动，在此一并表示感谢。
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