郯庐断裂带(安徽段)内磁铁石榴角闪岩的形成条件、年代学及构造归属的探究*

聂峰　石永红　王娟　康涛　曹晟

合肥工业大学资源与环境工程学院，合肥　230009

磁铁石榴角闪岩；等压降温；锆石U-Pb年龄；郯庐断裂

1　引言

图1　研究区地质简图(a)-肥东地区(安徽段)地质图；(b)-地质剖面图Fig.1　Simplified geological sketch map of the study area(a)-geological sketch map of the Feidong area (Anhui segment); (b)-geological profile

长期以来，郯庐断裂的形成机制和演化过程一直是研究的热点，特别是该断裂与大别-苏鲁造山带在时空上、成因上的联系一直为人们所关注(Xuetal., 1987; Zhuetal., 2005, 2009, 2010)。目前，主流的观点认为郯庐断裂形成于大别-苏鲁造山带碰撞俯冲过程中(Zhangetal., 1984; Hsuetal., 1987; Watsonetal., 1987; Yin and Nie, 1993; Li, 1994; 万天丰和朱鸿, 1996; Chang, 1996; 王小凤等, 1998; Chung, 1999; Zhuetal., 2005, 2009, 2010)。另一种观点则强调郯庐断裂形成于该造山带折返之后(Xuetal., 1987; Okay and Sengor, 1992; Xu and Zhu, 1994; Wangetal., 2003; Mengetal., 2007)。近年来对郯庐断裂的研究多集中于年代学和构造地质学方面(Xuetal., 1980, 1987, 1994; Lin and Fuller, 1990; Okay and Sengor, 1992; Yin and Nie, 1993; Li, 1994; Linetal., 2005, 2009; Lin and Li, 1995; Zhang, 1997; Gilderetal., 1999; Schmidetal., 1999; Wangetal., 2003; Mengetal., 2007; Zhuetal., 2005, 2009, 2010; 朱光等, 1998, 2001, 2002, 2003, 2005a, b, 2006a, b, 2009a; 王勇生等, 2004, 2005a, b, 2006; 牛漫兰等, 2002, 2005, 2006; Zhang and Teyssier, 2013; Zhangetal., 2013; 赵田等, 2014)，多关注其不同层次的变形特征和水平错断距离(Zhuetal., 2005, 2009, 2010)。而对于郯庐主干断裂(安徽段)空间上的展布状况仍缺乏统一的认识。Xuetal. (1987)、Zhangetal. (2007, 2013a, b)、Zhuetal. (2005, 2009, 2010) 认为郯庐主干断裂位于合肥盆地东缘，即解集-阚集-王铁-桥头集以东的张八岭隆起区。但是，赵田等(2014)则认为该主干断裂处于合肥盆地内部(图1)。关于该断裂带的横向展布，多数学者认为其沿着一个狭窄的线性条带分布，并仅限于扬子地块上。上述关于郯庐断裂带空间位置的不同认识，可能是由于对张八岭隆起区岩石单元构成缺乏深入的解剖所致，特别是相关精细的变质岩石学研究的不足，影响了人们对郯庐断裂带的全面深入理解。作为切穿了华北和扬子两大板块的郯庐断裂带，其展布范围可能不仅局限于扬子板块上，横向上的范围应当较为宽阔，从而部分进入华北板块内。若如此，在走滑断裂作用下，该带内可能有来自两侧板块的岩石。为此，本文对张八岭隆起区肥东群的特征性岩石——磁铁石榴角闪岩进行了详细变质岩石学、年代学研究。研究显示，该类岩石可能来源于华北板块，推测其可能因郯庐断裂的走滑作用被卷入该带内。

2　研究剖面及样品介绍

本次研究区域位于张八岭隆起区南段肥东地块最南缘。该地块西侧为合肥盆地，东侧为全椒盆地所覆盖(图1)。根据Zhuetal. (2005, 2009, 2010)和康涛等(2013)的研究，认为该地块自西向东可分为3个单元：(1)单元-I：主体为花岗片麻岩，沿浮渣山-火龙山-尖山-后分河一线分布，其间夹有斜长角闪岩和黑云斜长片麻岩透镜体；(2)单元-II：主要为黑云斜长片麻岩，分布于太子山一线；(3)单元-III：主要由角闪斜长片麻岩、含磷大理岩、斜长角闪岩、石榴黑云母片麻岩构成，沿龙山-方集-上份叶-蛮山口分布。该地块中发育有3条NNE向韧性剪切带，每条宽度在100～200m(图1a)，均表现为左旋走滑运动特征(Zhuetal., 2005, 2009, 2010)。

重点研究的剖面位于单元-III东南缘，蛮山口北东，上份叶东南，坐标为：纬度31°46.148′和经度117°36.663′，剖面总长约200m。在该剖面上共采集23块样品，其中变形花岗岩5块，斜长角闪岩3块，石榴黑云片岩7块，磁铁石榴角闪岩8块，其中用于此次研究分析的共计4块(图1b)，分别为QT026-1、QT023-1、TF003-1和TF001-2。研究剖面为NW-SE向，由西向东出露的岩性依次为变形花岗岩、斜长角闪岩、石榴黑云片岩、磁铁石榴角闪岩、石榴黑云片岩和斜长角闪岩(图1b、图2a)。这些岩石均以单斜层形式产出，面理倾向为134°～166°、倾角47°～65°。其中磁铁石榴角闪岩夹持于石榴黑云片岩之中，其出露的宽度约40～60m，斜长角闪岩和石榴黑云片岩宽度多在20～30m(图2a)，这三类岩石紧密共生，沿走向延伸<300m，表现为构造透镜体形式。而变形花岗岩则沿走向稳定延伸，并与斜长角闪岩顺层接触，露头规模可见到微褶和长石拉长变形之特征(图2a)。

表1磁铁石榴角闪岩代表性矿物成分(wt%)

Table 1The representative mineral compositions (wt%) of magnet garnet amphibole

矿物包体基质1基质2GrtGruFe-HblGrtGruFe-HblGrtGruFe-HblSiO236.4747.9442.6436.4850.4841.2836.1750.3240.76TiO20.000.000.000.000.020.030.000.000.13Al2O319.920.4410.9320.251.1212.8020.010.9613.60FeO33.0237.8927.1733.6839.0828.1833.8139.4728.14Cr2O30.000.000.000.010.000.000.030.000.00MnO1.180.160.051.140.140.051.080.150.05MgO0.776.573.760.685.412.640.895.472.36CaO8.090.6211.457.251.2711.517.040.9911.78Na2O0.030.311.440.030.271.560.040.211.64K2O0.000.010.090.000.010.110.000.010.10Total99.4793.9497.5499.5397.7998.1699.0697.5798.55O12.0023.0023.0012.0023.0023.0012.0023.0023.00Si2.967.926.612.977.986.392.967.996.31Al1.910.092.001.940.212.341.930.182.48Fe3+0.160.000.540.120.000.560.160.000.45Ti0.000.000.000.000.000.000.000.000.02Cr0.000.000.000.000.000.000.000.000.00Fe2+2.085.232.992.175.173.092.155.243.20Mn0.080.020.010.080.020.010.080.020.01Mg0.091.620.870.081.280.610.111.300.54Ca0.710.111.900.630.221.910.620.171.96Na0.010.100.430.000.080.470.010.060.49K0.000.000.020.000.000.020.000.000.02Sum8.0015.0915.358.0014.9515.408.0014.9515.47

3　岩相学和主要矿物化学分析

由于此次研究的重点是磁铁石榴角闪岩，故矿物化学分析主要是针对该类岩石进行。矿物成分测试由合肥工业大学资源与环境工程学院电子探针实验室完成，仪器型号为JEOL JAX-8230，实验条件为：加速电压15kv，电子束流20nA，电子束斑为3μm。其中石榴石和铁闪石、铁普通角闪石结构式分别以12和23个O进行计算，Fe2+的校正则分别以电价平衡法(Droop, 1987)、全Fe2+和Si+Al+Ti+Mg+Fe+Mn=13进行估算。代表性矿物分析结果见表1。此外，文中矿物缩写据 Whitney and Evans (2010)：Grt=石榴石；Gru=铁闪石；Fe-Hbl=铁普通角闪石；Fe-Ts=铁契尔马克闪石；Qz=石英；Amp=角闪石；PL=斜长石；Kfs=钾长石；Bt=黑云母；Ms=白云母；Mag=磁铁矿；Chl=绿泥石；Ap=磷灰石。

图2　研究区岩石野外照片和显微照片(a)-主要岩性接触关系；(b)-变形花岗岩显微照片；(c)-斜长角闪岩显微照片；(d)-石榴黑云片岩显微照片；(e、f)-磁铁石榴角闪岩显微照片Fig.2　The field photos and microstructure photos in the study area(a)-contact relation of main lithology; (b)-microstructure photos of deformational granites; (c)-microstructure photos of Plagioclase amphibolite; (d)-microstructure photos of garnet biotite schist; (e, f)-microstructure photos of magnet garnet amphibole

3.1　岩相学分析

(1)变形花岗岩(样品QT026-5)：主要为钾长石(20%～25%)+斜长石(20%)+石英(30%)+黑云母(10%)+白云母(10%～15%)(图2b)。这些矿物因剪切变形作用，多表现为拉长变形之特征，粒径大小不一。其中钾长石粒径为0.2～0.5mm，斜长石粒径为0.2～0.5mm，石英粒径为0.2～0.5mm；黑云母则表现为他形-半自形，粒径约0.2～0.3mm。白云母则多为多硅白云母，Si4+多在3.08～3.12。

(2)斜长角闪岩(样品QT023-1)：组成矿物为角闪石(50%～55%)+斜长石(20%～25%)+石英(10%～15%)+黑云母(10%～15%)+磷灰石(5%)(图2c)。角闪石呈自形-半自形，鳞片状定向排列，粒径0.2～2mm，颗粒边缘发生轻微绿泥石化；斜长石为半自形-他形结构，粒径为0.1～0.3mm；黑云母半自形-他形，粒径大小～0.2mm，部分颗粒已完全退变为绿泥石，仅保留黑云母结构假象；石英他形结构，粒径大小0.2～0.5mm；磷灰石他形结构，颗粒大小为0.1～0.3mm。

图3　磁铁石榴角闪岩的石榴石X-ray mapping图、角闪石BSE图及成分剖面图(a)-石榴石X-ray mapping图；(b)-石榴石成分剖面图；(c)-铁闪石BSE图；(d)-铁闪石成分剖面图；(e)-铁普通角闪石BSE图；(f)-铁普通角闪石成分剖面图Fig.3　X-ray mapping image of garnet, BSE images of amphibole and compositional profiles from magnet garnet amphibole(a)-X-ray mapping image of garnet; (b)-compositional profiles of garnet; (c)-BSE image of grunerite; (d)-compositional profiles of grunerite; (e)-BSE image of Fe-hornblende; (f)-compositional profiles of Fe-hornblende

(3)石榴黑云母片岩(样品TF003-1)：矿物组成为石榴石(30%)+黑云母(40%)+石英(20%)+白云母(10%)+磁铁矿(5%)+磷灰石(3%)(图2d)，石榴石呈自形-半自形，粒径1～3mm，内含大量石英、云母、磷灰石包体，包体主要分布于核部，边部无包体；黑云母为自形-半自形结构，粒径大小0.2～1mm。白云母为自形-半自形，粒径0.2～0.5mm，夹持于黑云母之间；石英呈他形，粒径0.2～3mm；磁铁矿呈自形，粒径0.2～0.3mm。

(4)磁铁石榴角闪岩(样品TF001-2)：该类岩石是本次分析的重点岩石，其矿物组合为石榴石(10%～15%)+铁普通角闪石(20%～25%)+铁闪石(25%～30%)+磁铁矿(25%～30%)+石英(10%～15%)+磷灰石(1%～3%)(图2e, f)。石榴石呈半自形-他形，粒径约为0.5～5mm，内部包含铁闪石、铁普通角闪石、磁铁矿、石英包体(图2e, f)，其多破裂，裂隙之中常常被绿泥石所充填；铁闪石以基质和包体两种形式存在，其中基质中的的铁闪石呈他形，粒径0.1～0.5mm；铁普通角闪同样以包体和基质两种形式存在，基质中的铁普通角闪石为他形，粒径0.1～1mm，其边缘或裂隙常常被绿泥石所替代；石英为他形，粒径0.1～2mm；磁铁矿呈自形-他形，粒径0.1～3mm；磷灰石为他形，粒径0.1～0.2mm。

图4　矿物成分图(a)-石榴石成分三角图；(b)-铁闪石成分图；(c)-铁普通角闪石成分图Fig.4　Compositional diagrams of the metamorphic minerals(a)-compositional triangle of garnet; (b)-compositional diagrams of grunerite; (c)-compositional diagrams of Fe-hornblende

3.2　磁铁石榴角闪岩主要矿物化学分析

为了较为精确地揭示该类岩石中主要矿物成分变化特征，以及准确评价其P-T演化过程，本次研究对其中的石榴石、角闪石进行了细致的成分剖面研究。研究显示：

(1)石榴石：在X-ray Mapping 图中(图3a)，其无明显的环带特征，颜色较为均匀。但在成分剖面中(图3b)，石榴石显示了轻微的核、边结构。自核部至边部，铁铝榴石组分逐渐增高(64%核→73%边)，镁铝榴石组分轻微增高(3%核→5%边)，钙铝榴石组分则略微降低(15%核→11%边)，锰铝榴石组分较为平坦。同样地，在成分三角图中(图4a)，核、边成分也略显差异，其中铁铝榴石组分逐渐增高，镁铝榴石组分和钙铝榴石组分相对较低。但就总体而言，石榴石成分变化似乎并不显著，这意味着其可能处于快速生长条件下，并已达到均一化程度。

(2)角闪石：该类岩石具有铁闪石和铁普通角闪石两种闪石，且两者都以包体和基质形式存在(图2e)。对基质中的铁闪石和铁普通角闪石的定量分析显示，无论是在矿物颜色方面，还是矿物成分方面，这两个闪石均较为均匀，没有明显的环带特征(图3c-f)。其中铁闪石中的Fe2+、Mg2+和Al3+成分十分平坦，没有早期或后期变质作用的叠加。稍有不同的是铁普通角闪石Al3+自核部至边部轻微降低(2.5核部→2.0边部)。参照Hammarstrometal. (1986)、Hollisteretal. (1987)、Johnsonetal. (1989)和Schmidt. (1992) 的研究，我们推测这也许反映的是一种降压的过程。然而，从成分剖面看(图3f)，这种退变降压可能并不显著。此外，以基质和包体形式存在的两种闪石的成分也没有显著的成分差异(图4b, c)。其中基质和包体的铁闪石成分变化基本位于同一个区域(图4b)，略有差异的是包体中的Mg/(Fe2++Mg)比值略高于基质的Mg/(Fe2++Mg)。对于包体中的铁普通角闪石其严格位于Fe-Hbl区域，而基质中铁普通角闪石主体位于Fe-Hbl区域，部分落入Fe-Ts区域(图4c)。

4　磁铁石榴角闪岩峰期变质P-T条件评价

依据岩相学和矿物化学分析(图2e, f、图3)，大致可以判定磁铁石榴角闪岩可能具有两个阶段的变质矿物组合：①阶段：Grt-I(核部)+Gru(包体)+Fe-Hbl(包体)+Qtz(包体)+Mag(包体)；②阶段：Grt-II(边部)+Gru(基质)+Fe-Hbl(基质)+Qtz(基质)+Mag(基质)+Ap磷灰石(基质)。据此，本文对其进行了细致的温压评价。在成分选取方面，参照成分剖面的分析(图2e, f、图3)，①阶段变质的成分选取石榴石核部，以及石榴石包体中的铁闪石、铁普通角闪石进行计算；②阶段变质的成分选取石榴石边部，基质中的铁闪石、铁普通角闪石核部或近边部的成分进行计算。同时，为保证分析计算的统计意义，本次研究在基质中共选取12个矿物对，包体中选取6个矿物对进行温压估算。基于Worley and Powell (2000)、Powell and Holland (2008)和魏春景等 (2009) 的研究，此次P-T条件的评价选用了Thermocalc version 3.33 (Holland and Powell, 1998) 平均温压法(av-PT)进行，计算结果见表2。由于①和②阶段的矿物组合基本类似，因此，这两个阶段的PT值基本是由6条独立反应线限定：

表2磁铁石榴角闪岩P(GPa)-T(℃)条件

Table 2TheP-Tconditions for magnet garnet amphibole

样品TPσTσPσfit包体17000.662490.673.2226880.672150.592.6636520.661790.532.4946440.842080.602.8956180.791620.472.2666160.851680.462.06基质76030.941780.442.1085970.631960.802.3196110.791310.361.67106300.591680.482.00116150.691510.411.82126140.801470.391.73136110.771460.391.78146370.841490.381.80156320.711440.401.78166430.511470.431.71176320.531470.421.64186120.941520.711.74

图5　磁铁石榴角闪岩峰期变质P-T条件图Fig.5　Plot of metamorphic peak P-T conditions of the magnet garnet amphibole

1) 10py+21fact=10gr+15grun+6tr

2) 4parg+12q=2gr+cumm+ts+2gl

3) 42parg+114q=14py+28gr+9cumm+21gl+12H2O

4) 7alm+12parg+36q=7py+6gr+3grun+3ts+6gl

5) 12parg+36q=2py+4gr+3tr+3ts+6gl

6) 3py+14gr+3grun+12q+12mt=11alm+12andr+3ts

对比石永红等(2009)对肥东群的研究，本次磁铁石榴角闪岩的变质条件明显高于他们的结果，但接近于王娟等(2014)确定的华北板块的东部陆块中的五河群变质条件。结合确定的变质年龄2450～2490Ma(见后述)和等压降温P-T样式分析(图5、图6g)，该类岩石变质特征十分类似Zhao and Zhai (2013)确定的2.5Ga变质事件和演化过程。换言之，该岩石可能源于华北板块。

5　锆石U-Pb定年

本次对磁铁石榴角闪岩(样品TF001-2)进行了锆石U-Pb定年。锆石单矿物挑选工作由河北省地勘局廊坊实验室完成，样品重约15kg，共挑选出约200单颗锆石。锆石制靶由合肥工业大学LA-ICPMS洁净实验室完成，锆石阴极发光(CL)照相由桂林理工大学电子探针实验室完成，仪器型号XM-Z09013TPCL。锆石U-Pb定年分析由合肥工业大学LA-ICPMS实验室完成，实验条件：激光器工作频率为10Hz，其中激光剥蚀束斑为32μm，信号有效采集时间为50s，每分析测试5个样品点测两次标准锆石91500。锆石数据处理采用ICPMSDateCal7.5软件(Ludwing, 2003)和ISOPLOT程序，单个测点同位素年龄的误差为1σ，加权平均年龄具有95%置信度。此外，锆石中矿物包体的测定由中国科学技术大学地球和空间科学学院拉曼实验室分析完成，仪器型Thermo Fisher DXR。年龄分析数据见表3。

根据显微镜下的透、反射光的研究，样品TF001-2中的锆石多为浑圆状或短柱状，自形程度较低，粒径50～300μm，长宽比为2:1～1:1。CL图像显示，锆石多为斑杂状分带、面状结构、云雾状分带，无震荡环带(图6a-c)。此外，这些锆石常具有较多的矿物包体，拉曼光谱分析显示这些包体多为角闪石和磷灰石(图6a-d)。

由于锆石粒径相对较小和激光剥蚀束斑较大的原因，本次锆石U-Pb定年仅获得了40个数据点，其中3个数据点为谐和年龄，其余数据点为不谐和年龄(表3)。3个谐和年龄的锆石的Th/U比值分别为0.09、0.11和0.15，基本上小于或约等于0.1，年龄分别是2473±15Ma、2490±18Ma和2450±15Ma，加权平均年龄为2469±49Ma(MSWD=1.5，n=3)(图6g)。而37个不谐和年龄的锆石的Th/U比值0.1～0.4(多为0.1)，其年龄范围为2350～2490Ma，均位于不协和线上，上交点年龄为2458±25Ma(图6g)。结合CL图像分析，这些锆石应均为变质锆石(吴元保和郑永飞, 2004)，故它们的年龄代表的是变质年龄。尽管，这里的上交点年龄并不能准确再现该变质事件的精确年龄，但其具有重要的参考价值。参照3个谐和年龄来看(图6g)，上交点年龄与其十分类同，这意味着3个谐和年龄应该能较为确切地反映某一变质事件年龄。参照Gebaueretal. (1997)、Hermannetal. (2001)、吴元保和郑永飞(2004)、Liuetal. (2004, 2011)、Liuetal. (2007) 和Zheng (2008)的研究，并根据此次拉曼光谱和定年分析结果，我们认为这3个谐和年龄反映的是①和②阶段变质作用年龄，因为这3个年龄均是在含角闪石和磷灰石矿物包裹体附近区域获得的(图6a-d)，而这些包体在①和②阶段变质矿物组合均普遍发育。

表3样品TF001-2锆石U-Pb定年分析数据

Table 3The zircon U-Pb date of the sample TF001-2

测点号232Th(×10-6)238U(×10-6)ThU206Pb(×10-6)同位素年龄(Ma)同位素比值207Pb206Pb1σ207Pb235U1σ206Pb238U1σ207Pb206Pb1σ207Pb235U1σ206Pb238U1σ140.91980.206596.902414112261142093110.15610.00108.26550.13100.38350.0024210.41090.096151.822422162265142093100.15690.00148.30660.12580.38360.0021312.995.30.135644.662456172246142031130.15890.00178.13460.12640.37040.0028431.61590.199375.952439142266132077130.15840.00138.31800.11730.38020.0028519.81840.107283.342439132227131997100.15840.00127.96370.11670.36310.0022620.21280.157643.542358181936151563150.15100.00155.73390.09640.27440.0029757.12630.2169112.1239810214210187970.15470.00097.24760.08410.33830.0014865.52250.2912111.9243910229311212790.15830.00098.56540.10500.39080.0020935.11590.220863.91239416209013179190.15420.00146.83180.09750.32020.00191037.31960.190383.82240511217113192580.15530.00117.47980.10450.34790.00171152.62550.206092.762350121992131662100.15020.00106.10990.08870.29420.00191227.31970.138481.84235012211313187680.15020.00107.01570.10210.33780.00171327.21650.165073.722388172189151979100.15380.00167.63820.12990.35940.00221419.71410.139562.932381132190161987130.15310.00117.63970.13510.36110.00261565.42370.2763111.7241611222116201290.15630.00107.91000.14390.36620.00191613.71070.128948.572422152250192060200.15680.00148.16750.17150.37660.00441730.02240.134198.342388112195161991150.15370.00107.68290.13760.36180.00321825.82330.1104101.73236112216414195970.15140.00117.42660.11450.35510.00161950.53730.1352139.4241610205214170680.15630.00096.54820.10370.30300.00172025.42310.109990.4823892112106171823170.15380.00106.95810.13660.32680.00362110.11100.092555.392473152378172265140.16160.00149.40490.17180.42100.00322216.61160.143148.972403172156161902120.15510.00157.35870.13450.34320.00252324.12080.115590.2723698217114196580.15200.00127.48140.11740.35630.00162410.189.50.113446.272490182387162267120.16330.00179.49700.16720.42150.00272510.41110.093150.802453192271172070130.15980.00138.36580.15790.37870.00272652.92270.2325103.72406112209172001110.15520.00107.80290.14490.36390.00232712.11050.115746.892417-1842240222038260.15640.00158.07690.19880.37190.00562831.41590.197864.85237717210714183990.15280.00146.96390.11210.33010.00182911.597.10.118248.282484152350152193120.16270.00149.11850.15150.40520.00253013.01050.124750.502450182292162116160.15950.00178.55960.15460.38850.00343116.01170.137352.16238315220115200680.15320.00137.74210.12510.36510.00183242.82430.176392.772444122083151732120.15890.00126.78100.11220.30820.00253316.11090.148155.882450152361142258110.15930.00149.22890.13820.41940.00253423.11480.156369.232455152302162128200.16000.00148.64880.14990.39120.00443528.11910.147180.92238914216013193380.15290.00127.39220.10850.34970.0017361052690.3899126.12408202214142006100.15560.00137.85270.11890.36510.00213713.11020.129046.572410162257172085200.15580.00148.23670.15430.38190.00433813.91480.094051.302376172010171662120.15250.00156.24260.11960.29410.00233927.31890.144485.332398212199171987140.15470.00197.71640.14210.36100.00294030.11470.205166.402413122219152009140.15590.00117.88970.12980.36570.0030

注：测点21、24、30三组数据为锆石谐和年龄数据

图6　样品TF001-2锆石CL图、包体拉曼光谱及U-Pb定年谐和图Fig.6　CL image, Raman spectra and concordia plots of zircons from sample TF001-2

6　磁铁石榴角闪岩构造归属讨论

目前，人们普遍认同郯庐断裂(安徽段)是华北和扬子板块的重要边界断裂，其左旋走滑错距长达>500km。主断裂严格地呈狭窄的线性条带发育于扬子板块内(Xuetal., 1987; Zhuetal., 2005, 2009, 2010; Zhangetal., 2007, 2013a, b; 朱光等, 2009; 赵田等, 2014)，出露的宽度～5km(图1)，而华北板块并未受到郯庐断裂明显的改造和影响。换言之，郯庐断裂带内的物质均由扬子板块构成，没有任何源于华北板块的物质。

通常认为华北和扬子板块的物质差异主要体现在年龄方面。Zhao and Zhai (2013) 的研究表明，华北板块最终拼合在1.85Ga完成，其内部出露有极少量的始太古(3.8～3.6Ga)岩石地块和部分2.8～2.7Ga初生陆壳。并强调华北板块主体是由2.6～2.5Ga高级片麻岩和低-中级花岗岩-绿岩构成，同时指出在～2.5Ga时期，华北东、西部陆块普遍经历了绿片岩相至麻粒岩相的逆时针等压降温变质作用，反映了源于地幔岩浆的底侵作用过程(Zhaoetal., 1998, 1999a, b; Zhao and zhai, 2013)。而1.95～1.85Ga变质年龄则反映了华北板块上西部、中部和东部陆块的彼此之间碰撞俯冲时限。具体到郯庐断裂西侧的华北东部陆块(图1中的插图)，Zhao and Zhai (2013) 认为该陆块在2.2～1.9Ga形成陆内裂谷(张秋生, 1988; Lietal., 2004, 2005, 2006)，形成Longgang和Nangrim 2个块体，并于1.9Ga时间俯冲碰撞拼合完成。相比较而言，扬子板块的岩石年龄具有较广的年龄范围，根据前人的研究其大致可分为7个年龄区间3.3～2.9Ga、2.7～2.5Ga、2.0～1.7Ga、～1.0Ga、850～650Ma、480～400Ma和245～200Ma(Hackeretal., 1998, 2006; Qiuetal., 2000; Ratschbacheretal., 2003, 2006; Wuetal., 2004; Zhengetal., 2007, 2008; Chenetal., 2003, 2009; Zhangetal., 2006; 郑永飞和张少兵, 2007; Gaoetal., 2011; 魏君奇等, 2012)，其中后三个年龄范围在扬子板块内普遍发育，而前三个较老的年龄在扬子板块上出露极少，且2.7～2.5Ga反映的是角闪岩相的变质事件。

对比本次张八岭隆起区的肥东群中的磁铁石榴角闪岩的年代学和变质岩石学的研究来看，磁铁石榴角闪岩中的3颗变质锆石的谐和年龄在2450～2490Ma，加权平均年龄为2496±49Ma，其十分接近于华北板块的～2.5Ga的变质年龄。而其他37颗变质锆石的不谐和年龄变化也较为单一，基本上在2350～2484Ma范围(表3)，这暗示了该岩石类型可能源于华北板块。然而，根据Qiuetal. (2000)和魏君奇等(2012)的研究，该年龄也同样落入扬子板块的2.7～2.5Ga的范围，似乎该岩石具扬子板块的亲缘性。对此，本文没有较为明确的结论。这里也许可以假设两种情形：(1)磁铁石榴角闪岩属于华北板块物质，由于郯庐断裂的左旋走滑作用，其呈构造透镜体的形式被卷入郯庐断裂带内；(2)该岩石本身就归属于扬子板块，可能是郯庐断裂带(安徽段)内出露的最老的岩石。

然而，结合地质背景、构造地质学和变质岩石学的研究，本次研究更倾向于前一种认识。主要理由是：(a)从地质背景来看，磁铁石榴角闪岩在华北东部陆块(安徽段)的五河杂岩和霍邱群中广泛发育该类岩石(安徽省地质矿产局, 1987; 杨晓勇等, 2012)，而安徽境内的扬子板块则没有这类相关类型岩石的确证。这暗示了该类岩石可能的物源来自于华北板块；(b)在年龄变化方面，磁铁石榴角闪岩的年龄十分单一，基本在～2.5Ga时间段(表1)，缺乏任何类似于扬子板块的较为年轻的年龄(850～650Ma、480～400Ma和245～200Ma)。且该年龄十分接近郯庐断裂西侧华北东部陆块的年龄(Liuetal., 2009; 许文良等, 2006; 杨晓勇等, 2012; 图1中插图)，这从另一个侧面反映了该岩石具华北板块亲缘性；(c)从变质P-T演化来看，磁铁石榴角闪岩显示了轻微的等压降温特征(图5)，与Zhao and Zhai (2013)阐述的华北东、西部陆块在～2.5Ga发生的源于地幔岩浆的底侵事件十分吻合。此外，该岩石的变质P-T条件也十分类似于五河群中石榴角闪岩的变质条件(王娟等, 2014)，明显不同于肥东群的变质条件(石永红等, 2009)；(d)构造地质学分析显示，磁铁石榴角闪岩及其围岩是呈构造透镜体产于变形的花岗岩之中，周边被糜棱岩所限定(图1b)。其面理和线理与郯庐断裂带中韧性剪切带的面理和线理呈大角度相交，暗示了其可能为一个外来的构造块体，并非原地物质。基于本次研究的结果，我们认为张八岭隆起区的肥东群中的磁铁石榴角闪岩可能来源于华北板块，由于郯庐断裂的左旋走滑作用被构造并置于扬子板块中。进一步地，可以推测郯庐断裂东侧界限位于方集-蛮山口以东的全椒盆地中，结合赵田等(2014)研究可以看出，该断裂在横向上(安徽段)的宽度至少在10～15km范围(图1)。

致谢感谢朱光教授在本文撰写过程中的支持与帮助；感谢吴春明教授和林伟研究员对本文的审阅及意见。

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