鹰扬关构造带位于湘—桂—粤三省交界之处，其地质工作始于1956至1975年1∶20万的区域地质调查工作，其中的岩石组合被命名为震旦纪或寒武纪泥砂岩。李自惠(1979)在鹰扬关构造带浅变质泥砂岩中识别出一套浅变质火山岩，称为“鹰阳关组”。在后期的区域地质调查工作中，其下部改称为“鹰扬关组”，而其上部改称为 “下龙组”或“拱洞组”。根据少量精度不高的年代学和岩石地球化学资料，前人对该套火山岩的活动时代和构造环境形成了不同认识。第一种观点认为其发育于新元古代(约819 Ma或约765 Ma)大陆裂谷环境，是华南板块对罗迪尼亚超大陆裂解的响应(周汉文等，2002；Tian Yang et al., 2020)；第二种观点认为其形成于新元古代(822～816 Ma)或早古生代(约415 Ma)汇聚大陆边缘大洋俯冲环境(覃小锋等，2015；Tian Yang et al., 2020)；第三种观点认为其沉积于新元古代(750～660 Ma)板内伸展环境(Qi Liang et al., 2021)。基于上述不同的年代学和构造环境解释，鹰扬关构造带被认为是：①新元古代或早古生代蛇绿混杂岩，代表了华夏板块与扬子板块的缝合带(殷鸿福等，1999；覃小锋等，2015；张克信等，2017；Liu Songfeng et al., 2018; 田洋等，2018；王令占等，2020)；②新元古代裂谷带(周汉文等，2002)；③新元古代至中生代多期变形叠加的陆内构造变形带(舒良树等，2020；徐先兵等，2021)。
基于最近15年来的基础地质调查、岩石地球化学以及年代学工作，笔者等在综述物质组成与年代学的基础之上，对鹰扬关构造带开展了详细的构造解析，讨论了其大地构造属性与构造演化过程。
1 物质组成
鹰扬关构造带主体呈NNE—NE向展布，其南起广西壮族自治区贺州市八步区大宁镇，北达广东省清远市连州市丰阳镇。鹰扬关构造带由码市街韧性剪切带、莲花断层与大宁韧性剪切带等边界断裂及其围限的地质体组成(图1a)，长约40 km，最宽处约10 km，整体表现为NE宽、SW窄的喇叭状。在鹰扬关构造带北部，码市街韧性剪切带与莲花断层控制NE—SW走向白垩纪码市—丰阳盆地的展布；在鹰扬关构造带中南部，NNE向码市街韧性剪切带和莲花断层收敛于大宁韧性剪切带。
图1 华南鹰扬关构造带的不同时期不同比例尺地质图
Fig. 1 Geological maps of the Yingyangguan tectonic belt measured at different scales during different periods
(a)1∶100万中南地区地质图；(b)1∶20万江永幅地质图；(c)1∶20万贺县幅地质图；(d)1∶5万桂岭圩幅地质图；(e)1∶5万大宁圩幅地质图。1—韧性剪切带；2—脆性断层；3—燕山期花岗岩；4—印支期花岗岩；5—广西期花岗岩；6—白垩系；7—泥盆系—二叠系；8—寒武系；9—震旦系；10—南华系上统；11—南华系下统；12—青白口系；13—地质剖面； PJSF：萍乡—江山—绍兴断裂；CLYCBF：郴州—临武—鹰扬关—岑溪—博白断裂；YGLNF：永州—桂林—柳州—南宁断裂；LSMF：罗甸—师宗—弥勒断裂
(a) 1∶1,000,000-scale geological map of central—southern China; (b) 1∶200,000-scale geological map of the Jiangyong region; (c) 1∶200,000-scale geological map of Hexian County; (d) 1∶50,000-scale geological map of the Guilingwei region; (e) 1∶50,000-scale geological map of the Daningwei region. 1—Ductile shear zone; 2—brittle fault; 3—Yanshanian granite; 4—Indosinian granite; 5—Kwangsian granite; 6—Cretaceous; 7—Devonian—Permian; 8—Cambrian; 9—Sinian System; 10—Upper Nanhuan System; 11—Lower Nanhuan System; 12—Qingbaikou System; 13—geological section; PJSF：the Pingxiang—Jiangshan—Shaoxing fault; CLYCBF：the Chenzhou—Linwu—Yingyangguan—Cenxi—Bobai fault; YGLNF：the Yongzhou—Guilin—Liuzhou—Nanning fault; LSMF：the Luodian—Shizong—Mile fault
鹰扬关构造带主要由千枚岩(图2a, 图3a)、板岩(图2b, 图3b)、变余砂岩(图2c, 图3c)、变余泥岩(图2d, 图3d)、变质酸性(图3e)和基性火山岩(图3f)、大理岩(图2e, 图3g)、硅质岩(图3h)以及侵位其中的花岗质岩石(图3i)和基性岩脉组成。由于缺乏良好的古生物和同位素年代学制约，在不同单位测制的1∶20万和1∶5万比例尺地质图上，鹰扬关构造带中前寒武纪地质单元被划归为不同时代的岩层，如震旦系、寒武系、南华系和青白口系(图1b—e)。
图2 华南鹰扬关构造带中不同面理的野外照片
Fig. 2 Field photographs of different foliations in the Yingyangguan tectonic belt
(a)千枚岩中的石英质条带成分分异层；(b)硅化板岩中的成分分异层；(c)变质砂岩中的黑色和白色成分分异层；(d)变余砂岩和变余泥岩的分界；(e)大理岩中的黑色变泥质条带；(f)NW向断裂中发育的硅质条带和磁铁矿层
(a) Quartz component layers in the phyllite; (b) component layers in silicified slate; (c) black and white component layers in meta-sandstone; (d) the boundary of slightly metamorphic sandstone and mudstone; (e) pelitic component layers in the marble; (f) cherty bands and magnetite beds in the NW-trending faults
图3 鹰扬关构造带中不同岩性的显微照片
Fig. 3 Micrographs of different lithology in the Yingyangguan tectonic belt
(a)由绢云母组成的千枚理；(b)由断续且平行的绢云母组成的板理；(c)不同粒度的石英组成的变余砂岩成分层；(d)不同粒度的石英和泥质组分构成的变余泥岩成分层；(e)白云母组成的变质酸性火山岩的面理；(f)变质的杏仁状玄武岩，杏仁体主要成分为石英；(g)由方解石、白云石和石英组成的白云岩；(h)主要由石英组成的变质硅质岩；(i)斑状花岗闪长岩，斑晶为斜长石、石英和黑云母
(a) Micrograph of phyllitic foliations consisting of sericite; (b) micrograph of foliations consisting of discontinuous parallel sericite; (c) micrograph of component layers in metasandstone shown by different sizes of quartz grains; (d) micrograph of component layers in mudstone shown by different sizes of quartz grains ; (e) micrograph of foliations in metamorphic acid volcanic rock composed of muscovite; (f) micrograph of metamorphic amygdaloidal basalt, and the amygdala is mainly composed of quartz; (g) micrograph of marble which is composed of calcite, dolomite and quartz; (h) micrograph of metamorphic silicalite which is mainly composed of quartz; (i) micrograph of porphyritic granodiorite, whose phenocryst is composed of plagioclase, quartz and biotite
千枚岩、板岩和变质酸性火山岩的次生面理发育，主要表现为成分分异层，如变质砂岩和千枚岩中的石英条带(图2a—c)和白云岩中的泥质条带(图2e)。次生面理与原生面理近平行，其走向以NE—SW为主，倾向SE或NW，倾角中等。变余砂岩和变余泥岩的面理以原生层理为主，表现为不同的颜色(图2d)、粒度和成分层(图2f)。原生面理走向以NW—SE为主，倾向NE或SW，倾角为低至中等角度。
在1∶5万地质图上(图1d, e)，鹰扬关构造带东侧南华纪变余砂泥岩表现为NW—SE走向向斜，其原生面理主要表现为NW—SE走向。而在鹰扬关构造带之中，原生面理少见，主要表现为次生面理，其走向主要表现为NE—SW向，倾向NW或SE，倾角为低至中高角度不等。
2 年代学综述
锆石U-Pb年代学表明鹰扬关构造带发育两期新元古代火山岩作用(表1)。早期火山岩以中—基性安山岩和玄武质岩为主，形成于822～816 Ma；晚期火山岩为双峰式火山岩，由长英质流纹岩和火山碎屑岩与基性岩组成，形成于765～753 Ma。覃小锋等(2015)利用LA-ICP-MS锆石U-Pb法测得下龙地区基性岩形成于439～415 Ma，与利用TIMS 锆石U-Pb法测得的819±11 Ma(周汉文等，2002)明显不同。但舒良树等(2020)通过重复采样和定年，认为下龙细粒辉绿岩形成于新元古代而非早古生代，且被约430 Ma高温花岗质岩浆热液所改造。该期构造热事件也得到了锆石U-Pb年龄为约419 Ma大宁岩体(程顺波等，2009)和约378 Ma的绢云母40Ar/39Ar年龄的佐证(王令占等，2019)。
碎屑锆石U-Pb年代学指示鹰扬关构造带中不纯大理岩和变余砂泥岩的最大沉积年龄为约661 Ma，且其中的凝灰岩形成于约670 Ma(Qi Liang et al., 2021)。上述年龄指示鹰扬关断裂中发育南华纪至震旦纪碳酸盐岩和泥砂岩，与华南新元古代斯图特冰期(约717～659 Ma)年龄(Zhou Chuanming et al., 2004, 2019; Lan Zhongwu et al., 2015, 2020)基本一致，指示鹰扬关构造带内不纯大理岩可能是斯图特冰期的盖帽碳酸盐岩经变质作用形成。
鹰扬关构造带中还发育广西期、印支期以及燕山期岩浆作用，如441～415 Ma的永和岩体和大宁岩体、约220 Ma的太堡岩体和160～150 Ma的禾洞岩体(表1)。绢云母40Ar/39Ar年代学表明，鹰扬关构造带还发育广西期(约378 Ma)和印支期(227～224 Ma)构造—热事件(王令占等，2019)。绢云母40Ar/39Ar的封闭温度(250～300℃; Leitch and McDougall, 1979; Hunziker et al., 1986)远远低于花岗岩中锆石的封闭温度(>800℃; Lee et al., 1997)。广西期绢云母40Ar/39Ar年龄(约378 Ma)远远小于广西期花岗岩年龄(441～415 Ma)，指示约378 Ma的绢云母40Ar/39Ar年龄可能代表的是区域花岗岩的冷却年龄。但构造带内印支期花岗岩锆石U-Pb年龄(约220 Ma)小于印支期绢云母40Ar/39Ar年龄(227～224 Ma)，指示227～224 Ma的绢云母40Ar/39Ar年龄是鹰扬关构造带印支期韧性变形的冷却年龄。
表1 华南鹰扬关构造带中原岩的形成年龄和变形—变质年龄
Table 1 Ages of deposition and deformation—metamorphism in the Yingyangguan tectonic belt
样品岩性地理位置年龄(Ma)测试方法年龄意义参考文献安山质岩石贺州八步区下龙村822±3LA-ICP-MS 锆石U-Pb火山喷发年龄Tian Yang et al., 2020安山质岩石贺州八步区下龙村822±3LA-ICP-MS 锆石U-Pb火山喷发年龄Tian Yang et al., 2020安山质岩石贺州八步区下龙村821±4LA-ICP-MS 锆石U-Pb火山喷发年龄Tian Yang et al., 2020变基性火山岩贺州八步区下龙村819±11 TIMS 锆石U-Pb火山喷发年龄周汉文等, 2002安山质岩石贺州八步区下龙村816±5LA-ICP-MS 锆石U-Pb火山喷发年龄Tian Yang et al., 2020砂岩贺州八步区芦冲口～770LA-ICP-MS 锆石U-Pb最大沉积年龄Qi Liang et al., 2021流纹质岩石贺州八步区底垌村765±3LA-ICP-MS 锆石U-Pb火山喷发年龄Tian Yang et al., 2020火山碎屑岩贺州八步区庙角村～754LA-ICP-MS 锆石U-Pb最大沉积年龄Qi Liang et al., 2021基性岩贺州八步区下龙村753±5LA-ICP-MS 锆石U-Pb火山喷发年龄Qi Liang et al., 2021凝灰岩贺州八步区庙角村670±6LA-ICP-MS 锆石U-Pb火山喷发年龄Qi Liang et al., 2021泥质灰岩贺州八步区寺田水口村～661 LA-ICP-MS 锆石U-Pb最大沉积年龄Qi Liang et al., 2021辉长岩连山县水井冲450±2LA-ICP-MS 锆石U-Pb岩体侵位年龄Tian Yang et al., 2021永和岩体连山县永和镇441±2LA-ICP-MS 锆石U-Pb岩体侵位年龄1∶5万地质报告❶大宁岩体贺州八步区大宁镇419±4SHRIMP 锆石U-Pb岩体侵位年龄程顺波等, 2009千枚岩贺州八步区下龙村378±3绢云母40Ar/39Ar冷却年龄王令占等, 2019千枚岩贺州八步区下龙村227±2绢云母40Ar/39Ar变形年龄王令占等, 2019千枚岩贺州八步区下龙村224±2绢云母40Ar/39Ar变形年龄王令占等, 2019太堡岩体连山县太堡镇220±1LA-ICP-MS 锆石U-Pb岩体侵位年龄李响等,2021a禾洞岩体连山县禾洞镇160±1LA-ICP-MS 锆石U-Pb岩体侵位年龄李响等,2021b二长花岗岩连山县上草镇159±1LA-ICP-MS 锆石U-Pb岩体侵位年龄Li Xiang et al., 2018大坪岩体连山县永和镇150±2LA-ICP-MS 锆石U-Pb岩体侵位年龄Wang et al., 2018太堡岩体连山县太堡镇150±2LA-ICP-MS 锆石U-Pb岩体侵位年龄Wang et al., 2018
3 构造解析
鹰扬关构造带中构造变形主要包括褶皱、断层和石香肠构造等，从微观到宏观尺度均有发育。宏观构造和微观变形既具有统一性，又存在一定的差别。
3.1 褶皱构造
褶皱构造主要表现在野外露头尺度(图4)和1∶5万填图尺度(图1)。新元古代岩层均不同程度地卷入了褶皱构造。其在变质砂岩、板岩和大理岩中较易识别，而在千枚岩中由于片理化发育难以识别。褶皱转折端以圆弧状为主，在板岩中表现为尖棱状。翼间角主要为30°～90°，属于开阔褶皱和中常—紧闭褶皱。根据其轴迹的方位，鹰扬关构造带中发育的褶皱以NNE—SSW走向和NW—SE走向为主。
在不纯的中—薄层泥质条带大理岩中，褶皱形态主要由弯曲的灰黑色泥质条带和白色大理岩表达(图4a、b、c)。褶皱转折端呈圆弧状，翼间角为30°～50°，属中常褶皱。在原位露头中，褶皱轴面呈中等—高角度倾向SE或NW，枢纽产状近水平，属于斜歪水平褶皱或直立水平褶皱(图5)。在桂岭镇大竹山大理石矿区，在采石中可见非原位的叠加褶皱发育。早期紧闭—同斜褶皱的轴面再次发生弯曲，形成晚期中常褶皱(图4c)。
图4 华南鹰扬关构造带中发育的褶皱变形
Fig. 4 Folds in the Yingyangguan tectonic belt
(a)永和—鹰扬关—大宁公路(323国道)旁大理岩中发育的紧闭褶皱，其翼间角为30°，轴面产状为120°∠79°；(b)八步区桂岭镇大竹山矿区中大理岩石块中发育的中常褶皱，其翼间角为46°；(c)八步区桂岭镇大竹山矿区中大理岩石块中发育的叠加褶皱，早期紧闭—同斜褶皱的轴面发生弯曲，形成晚期中常褶皱；(d)八步区大宁镇灰绿色中—厚层变余砂岩中发育的NW—SE走向中常向斜，其NE翼产状为120°∠79°，SW翼产状为87°∠57°，翼间角为67°；(e)八步区桂岭镇大竹山矿区西侧灰绿色中—薄层变余砂岩中发育的NW—SE走向开阔背斜，其东翼产状为140°∠8°，西翼产状为192°∠75°，翼间角为85°；(f)永和—鹰扬关—大宁公路(323国道)旁寺田路口砾岩中发育的圆弧状中常褶皱；(g)变质岩中由面理组成的对称状褶皱(非原位)；(h)变质岩中由面理组成的对称状褶皱(非原位)；(i)变质岩中沿面理发生顺层逆冲作用，形成不对称褶皱和膝折带；(j)千枚状板岩中沿面理发生顺层逆冲作用，形成不对称褶皱
(a) A tight fold developed in the marble beside Yonghe—Yingyangguan—Daning Highway (National Highway 323), with an interlimb angle of 30° and an axial plane occurrence of 120°∠79°; (b) the close fold developed in the marble rock in Dazhushan deposit, Guiling town, Babu district, with an interlimb angle of 46°; (c) the superimposed fold developed in the marble rock in Dazhushan deposit, Guiling Town, Babu district, and the early axial plane of the tight- isoclinal fold was bent to form the close folds; (d) the NW—SE trend close syncline occurred in thick gray-green metasandstone in Daning Town, Babu district, whose occurrences of the NE limb and SW are 120°∠79° and 87°∠57°, respectively, and their withinterlimb angle is 67°; (e) the NW—SE trend open anticline occurred in thin gray-green medium metasandstone in the Dazhushan deposit, Guiling Town, Babu district, whose occurrences of the east limb and west limb are 140°∠8° and 192°∠75°, respectively, and their withinterlimb angle is 85°; (f) a circular close fold developed in conglomerate at the Sitian road intersection beside the Yonghe—Yingyangguan—Daning Highway (National Highway 323); (g) symmetrical folds (not in situ) composed of foliation in metamorphic rocks; (h) symmetrical folds (not in situ) composed of foliation in metamorphic rocks; (i) foliation-parallel thrust occurred in metamorphic rocks resulting in asymmetric folds and kink band; (j) foliation-parallel thrust occurred in phyllitic slate and formed asymmetric folds
图5 华南鹰扬关构造带三条地质剖面图(剖面位置在图1中标示)
Fig. 5 Three structural sections in the Yingyangguan tectonic belt (the location of section is indicated in Fig. 1a)
在大宁镇北部灰绿色中—厚层变余砂岩中可见露头尺度的向斜发育，表现为转折端呈圆弧状，翼间角为67°的中常褶皱(图4d)。该向斜的NE翼产状较缓，SW翼产状较陡，枢纽近水平(169°∠12°)，表现为NWW—SEE走向的斜歪水平褶皱。在桂岭镇大竹山矿区西侧中—薄层变余砂岩中，可见露头尺度的背斜发育，其东翼产状近水平，西翼产状陡立，枢纽近水平(104°∠7°)，表现为NWW—SEE走向的斜歪水平褶皱(图4e)。在寺田路口，可见非原位砾岩中发育转折端呈圆弧状的中常褶皱，翼间角约为70°，两翼产状近对称(图4f)。综上可见，南华纪变余砂岩中发育的褶皱主要表现为走向NW—SE的中常褶皱，与1∶5万图面上南华系内发育的褶皱形态一致(图1e)。
在鹰扬关构造带中还可见由片岩和板岩中早期面理组成的褶皱，其形态表现为对称状和不对称状(图5)。对称状褶皱翼间角为45°～80°，转折端呈圆弧状(图4g、h)。不对称褶皱主要是由顺层滑动作用形成，转折端呈膝折状，指示由NWW向SEE的逆冲作用(图4i、j)。在强烈变形区，还可见不对称褶皱的短翼发育膝折带(图4i)。
3.2 断层构造
鹰扬关构造带中断层主要发育在不同岩性的接触面或构造薄弱带中。按断层走向，主要可以分为NNE—SSW向(图6a、b、d—i)和NW—SE走向断层(图6c)，且以NNE—SSW向为主(图7)；按断层运动学特征，可以划分为逆断层(图6a—d)、正断层(图6d, e)、左旋走滑断层(图6f—h)和右行走滑断层(图6i)；按断层性质，可以划分为脆性断层和韧性剪切带(图6f—h)，其中以脆性断层为主。很多断层面上都保留了多期断层活动的证据，指示鹰扬关断裂带发育了多期构造活动。
在鹰扬关构造带中，可见不同岩性的岩块之间主要表现为逆断层接触。在大桂山矿区边界可见大理岩岩块与变余砂岩之间呈逆断层接触(图6a)，断层走向NNE—SSW，倾向SE，倾角中等。断层带内发育石英片岩，远离断层带渐变为正常大理岩和变余砂岩。不对称石英布丁构造(图6a)和发育在变余砂岩中的褶皱(图4e)均指示NNE—SSW走向的逆冲作用，与露头尺度逆断层一致(图4i, 图6b, d)。在323国道旁，可见低角度变余砂岩叠覆于近直立的板岩之上，二者产状明显不一致，早期被解释为新元古代角度不整合(徐志贤等，2006)。由于缺少底砾岩，且接触面为一套强面理化变质砂岩，沿面理还发育石英条带和磁铁矿层(图3f)，因此认为变余砂岩与板岩以NW—SE走向逆断层相接触，与露头尺度逆断层一致(图6c)，不属于角度不整合。
鹰扬关构造带中正断层较为少见，断层走向以NNE—SSW向为主(图6d, e)。正断层一般叠加在早期的逆断层之上，表现为先逆后正向滑动(图6d)。
图6 华南鹰扬关构造带中不同性质断层的野外照片
Fig. 6 Field photographs of faults with different shear senses in the Yingyangguan tectonic belt
(a)大理岩与变余砂岩以NNE—SSW走向逆断层接触，石英布丁构造指示逆冲剪切；(b)节理脉指示NNE—SSW走向断层为逆断层；(c)节理脉和不对称褶皱指示NW—SE走向断层为逆断层；(d)不对称褶皱和擦痕指示NNE—SSW走向断层早期为逆断层，晚期为正断层；(e)不对称碎斑指示NNE—SSW走向断层为正断层；(f)不对称石英布丁构造指示NNE—SSW走向断层为左行走滑断层；(g)“槽中脊”型韧性擦痕与阶步指示NNE—SSW走向断层为左行走滑断层；(h)“槽中脊”型韧性擦痕与阶步指示NNE—SSW走向断层为左行走滑断层；(i)擦痕和阶步指示NNE—SSW走向断层为右行走滑断层
(a) The marble overlay on the metasandstone by NNE—SSW-trending thrust fault, and the quartz boudinage indicates thrust shearing; (b) the joint veins indicate that the NNE—SSW-trending fault is a reverse fault; (c) the joint veins and asymmetric folds indicate that the NW—SE-trending fault is a reverse fault; (d) asymmetric folds and striae indicate that the NNE—SSW-trending fault is a reverse fault in the early stage and a normal fault in the late stage; (e) asymmetrical porphyroclast indicates that the NNE—SSW-trending fault is a normal fault; (f) asymmetrical quartz boudinage indicates that the NNE—SSW-trending fault is a reverse fault; (g) the ridge-in-groove slickenside striae and step indication the NNE—SSW-striking fault is a sinistral strike-slip fault; (h) the ridge-in-groove slickenside striae and step indication the NNE—SSW-striking fault is a sinistral shear zone; (i) striae and step indication the NNE—SSW-striking fault is a right-lateral strike-slip fault
左行走滑断层在鹰扬关构造带中强烈发育，以NNE—SSW走向为主，断层面倾向SE为主，倾角较陡(图6f—h)。在断层核部可见强烈的韧性变形，不对称石英布丁构造、“槽中脊”型韧性擦痕与阶步均指示左行走滑(图6f—h)。
鹰扬关构造带中右行走滑断层较为少见，断层走向以NNE—SSW为主，高角度倾向SE，倾角近直立(图6 i)。断面上擦痕近水平(图7)，阶步指示右行走滑。
3.3 石香肠构造
鹰扬关构造带中石香肠构造也较为发育，主要表现为板岩中的石英石香肠构造和不纯大理岩中泥质条带石香肠构造(图5)。大型石英石香肠构造在露头尺度仅见一个石香肠体(图8a)，其平面形态呈椭透镜状，与围岩界线清楚；而小型石英石香肠构造在露头尺度可见多个连续的香肠体，其连线方向与层理/面理平行(图8b)，指示是垂直层面的挤压作用形成。不纯大理岩中泥质条带石香肠整体也与层面平行(图8c)，由垂直于层面的挤压作用形成。
图7 鹰扬关构造带三条构造剖面中断面、擦痕与面理产状赤平投影(等面积下半球)
Fig. 7 Stereographic projections of fault planes, fault striae and foliations in the three structural sections of
Yingyangguan tectonic belt
图8 华南鹰扬关构造带中石香肠构造
Fig. 8 Boudinage structures in the Yingyangguan tectonic belt
(a)板岩中大型石英石香肠构造；(b)板岩中小型石英石香肠构造；(c)不纯大理岩中泥质条带石香肠构造
(a) Large quartz boudinage in slate; (b) small quartz boudinage in slate; (c) boudinage in the impure mud-banded marble
4 解释与讨论
4.1 鹰扬关构造带的大地构造属性
华南板块主要是由扬子地块和华夏地块拼合形成(Charvet et al., 1996; Shu Liangshu et al., 2021)。扬子地块和华夏地块的拼合位置在华南东段较为清晰，为萍乡—江山—绍兴断裂(Zhang Zhongjie et al., 2005; Li Xianhua et al., 2009; 舒良树，2012)。由于显生宙沉积覆盖，对扬子和华夏陆块在华南西段的拼合位置存在不同认识(图1)：①郴州—临武—鹰扬关—岑溪—博白断裂(Wang Yuejun et al., 2003, 2008; Liu Songfeng et al., 2018)；②永州—桂林—柳州—南宁断裂(饶家荣等，2012; Guo Lianghui et al., 2019; 舒良树等, 2020)；③罗甸—师宗—弥勒断裂(董云鹏和朱炳全，1999; Guo Liguo et al., 2009)。
茶陵—郴州断裂两侧的莫霍面深度(Zhang Zhongjie and Wang Yanghua, 2007；)、物质组成(Wang Yuejun et al., 2003, 2008)和早古生代古地理格局差异明显(马永生等，2009; 张克信等，2017)，且发育了显生宙多期构造变形(李三忠等，2016；Xu Xianbing et al., 2021a, b)。郴州—临武断裂向南的鹰扬关和岑溪地区还发育“构造混杂岩”(彭松柏等，2006, 2016a, b; 覃小锋等，2007, 2015, 2017; Liu Songfeng et al., 2018)，指示萍乡—江山—绍兴断裂带可能经郴州—临武断裂向南过鹰扬关构造带并连接岑溪—博白断裂(Yang Xue et al., 2022)。但后期的岩石地球化学研究表明鹰扬关和岑溪地区火山岩并不是蛇绿岩成因(Wang Yuejun et al., 2018；Tian Yang et al., 2020)。最新的地球物理资料也指示萍乡—江山—绍兴断裂带向南延伸至郴州—临武断裂，但其在鹰扬关构造带北部的九嶷山地区发生向西偏转，并未向南延伸到鹰扬关构造带和岑溪—博白断裂(He Lipeng et al., 2021)。
基于对鹰扬关构造带内火山岩的形成环境和形成时代的不同认识，鹰扬关构造带的大地构造属性被解释为：①新元古代中期蛇绿混杂岩与扬子和华夏板块的分界线(田洋等，2018；王令占等，2020)；②新元古代中期裂谷(周汉文等，2002)；③早古生代绿混杂岩，代表扬子和华夏板块的分界线(殷鸿福等，1999；覃小锋等，2015；张克信等，2017)；④陆内构造变形带(舒良树等，2020；徐先兵等，2021)。
鹰扬关构造带内的主体岩性为822～816 Ma安山岩和玄武质岩(周汉文等，2002；Tian Yang et al., 2020)、765～753 Ma双峰式火山岩(Tian Yang et al., 2020；Qi Liang et al., 2021)、670～660 Ma碳酸盐岩(Qi Liang et al., 2021)、片岩、板岩与变余泥砂岩等。其中，变余泥砂岩被广西期大宁岩体和永和岩体(程顺波等，2009)所侵位，指示其形成于志留纪之前。由此可知，鹰扬关构造带确实是由新元古代至早古生代时期的不同岩性单元混杂形成。
“混杂岩(mélange)”最早由Greenly(1919)年提出，是指1∶2.5万或更大比例尺的地质填图单元，由透入性变形的基质及其内部无序的混杂岩块组成(闫臻等，2018; Festa et al., 2019; 张克信等, 2020)。按形成过程和成因机制，混杂岩可以划分为构造混杂岩、沉积混杂岩、底辟混杂岩以及复合成因混杂岩(Festa et al., 2010; 闫臻等，2018)。混杂岩可以形成于被动大陆边缘、走滑构造带、转换构造带、汇聚大陆边缘和洋壳俯冲、大陆碰撞和陆内变形等不同大地构造环境(Festa et al., 2010; 闫臻等，2018；王国灿和张攀，2019)。
不同成因的混杂岩具有不同的大地构造地质意义(Festa et al., 2010, 2012, 2019; Dilek et al., 2012; Kimura et al., 2012; 闫臻等，2018; 张克信等，2020)。构造混杂岩因普遍含有基性至超基性蛇绿岩岩块，往往被认为是汇聚板块边缘和缝合带的鉴定标志(Cawood et al., 2009; Wakabayashi and Dilek, 2011; Kimura et al., 2012)。地球化学指示鹰扬关构造带内新元古代火山岩形成于岛弧或者陆内裂谷环境(周汉文等，2002；Tian Yang et al., 2020；Qi Liang et al., 2021)，且缺少超基性岩、辉长岩、枕状熔岩以及远洋放射虫硅质岩等蛇绿岩套的组成单元，因此鹰扬关构造带内新元古代火山岩不属于蛇绿岩的组成单元，更谈不上构造混杂岩。
由于无底辟构造发育，鹰扬关构造带只可能是沉积混杂岩或者复合成因混杂岩。沉积混杂岩是无序的岩石单元，其中的外来块体通过沉积(重力)过程与基质结合和混合(Festa et al., 2010, 2012，2019)。由于鹰扬关构造带在新元古代晚期处于裂谷环境或被动大陆边缘的伸展环境(周汉文等，2002；Qi Liang et al., 2021)，822～816 Ma岛弧型火山岩、765～753 Ma双峰式火山岩和670～660 Ma碳酸盐岩在重力作用下可以混入新元古代晚期的砂泥岩之中。由于岩块与泥砂岩之间为构造薄弱面，在后期构造应力作用下，岩块与泥砂岩由于能干性不同容易呈断层接触或岩块在泥砂岩中呈石香肠体分布。由此可以认为，鹰扬关构造带在新元古代晚期伸展构造环境下属于沉积混杂岩，后经显生宙广西期、印支期和燕山期构造运动叠加和改造。
4.2 鹰扬关构造带的形成过程
构造解析表明，鹰扬关构造带内发育两类不同走向的褶皱，分别为NW—SE走向褶皱和NNE—SSW走向褶皱。在1∶5万图面上，NW—SE走向褶皱由南华系构成，且被广西期岩体侵位，指示其形成于南华系之后，志留纪之前。结合区域构造运动(舒良树，2012)，鹰扬关构造带内南华系NW—SE走向褶皱形成于广西期造山运动，其早期可能为近E—W走向褶皱，但受到后期NE—SW向褶皱叠加或NE—SW向断层的走滑牵引，使其走向改变为NW—SE向(李三忠等，2016；李智等，2019；徐先兵等，2021)。在670～660 Ma不纯大理岩之中可见早期NW—SE走向褶皱被晚期NNE—SSW走向褶皱所叠加，指示NNE—SSW走向褶皱形成于印支期或燕山期造山运动。结合区域上近东西向褶皱被印支晚期或燕山期NNE—SSW向褶皱所叠加(徐先兵等，2009, 2021；张岳桥等，2009；柏道远等，2012；Shi Wei et al., 2015; Li Jianhua et al., 2018; Wang Yuejun et al., 2021; 杨俊等，2021)，鹰扬关构造带内NNE—SSW走向褶皱形成于印支晚期或燕山期。
构造解析表明，鹰扬关构造带内发育两类不同走向的断层，分别为NW—SE走向断层和NNE—SSW走向断层(图7)。NW—SE走向断层为逆断层，其应力场与NW—SE走向褶皱一致，且其发育在南华系变余砂岩之中或其与板岩的接触边界，因此推测NW—SE走向逆断层同样形成于广西期造山作用。绢云母40Ar/39Ar年代学指示NNE—SSW走向断层形成于227～224 Ma(王令占等，2019)。运动学分析表明NNE—SSW走向断层的运动学指向主要表现为逆冲或左行走滑，其区域应力场为NW—SE挤压。区域上，NNE—SSW走向断层的褶皱—逆冲带和韧性剪切带广泛发育于雪峰山地区(Wang Yuejun et al., 2005; Chu Yang et al., 2012a, b)和武夷山地区(Xu et al., 2011; Li Jianhua et al., 2017, 2022)，是早中生代陆内变形的产物。
鹰扬关构造带内NNE—SSW走向断层还发育正断或右行走滑作用。交切关系表明，沿NNE—SSW走向断层的正断作用晚于逆冲作用，且其主要表现为脆性断层活动，指示其形成时代晚于227～224 Ma。NNE—SSW走向断层的右行走滑也是表现为脆性活动，指示其形成时代同样晚于227～224 Ma的韧性变形。区域上，NNE—SSW走向断层的脆性正断作用和右行走滑作用，主要发生在燕山期(Li Jianhua et al., 2014, 2020; Xu Xianbing et al., 2016, 2021b; Chu Yang et al., 2019, 2020)。因此，鹰扬关构造带内还叠加了燕山期构造活动。
综合物质组成、构造解析以及年代学结果，鹰扬关构造带新元古代至中生代构造演化过程如下：①新元古代中期(822～816 Ma)，鹰扬关构造带位于活动大陆边缘，接受岛弧型火山岩沉积(Tian Yang et al., 2020)，扬子与华夏陆块在约810 Ma拼合形成华南板块(Xu Xianbing et al., 2014, 2018; Yao Jinlong et al., 2019; Shu Liangshu et al., 2021)。随着罗迪尼亚大陆的裂解，华南板块内部发育陆内裂谷(Wang Jian and Li Zhengxiang, 2003; Li et al., 2008)和伸展作用(Qi Liang et al., 2021)，重力作用导致822～816 Ma 岛弧型火山岩与765～753 Ma裂谷型双峰式火山岩发生沉积混杂(图9a)。新元古代晚期，鹰扬关构造带继续接受670～660 Ma碳酸盐岩和泥砂岩沉积；②早古生代晚期(441～415 Ma)，广西期造山作用在鹰扬关构造带中形成近E—W向褶皱、逆断层和花岗岩体(图9b)；③早中生代(227～220 Ma)，印支晚期造山作用导致NNE—SSW走向褶皱和韧性剪切带的发育，鹰扬关构造带的变形样式基本定型(图9c)；④晚中生代，燕山期造山作用导致鹰扬关构造带发生活化，强烈的伸展作用和走滑作用导致NNE—SSW走向白垩纪盆地发育。
图9 华南鹰扬关构造带新元古代中晚期至早中生代构造演化模型图
Fig. 9 Tectonic evolution model of the Yingyangguan tectonic belt during mid—late Neoproterozoic to Early Mesozoic
5 结论
通过物质组成和年代学综述，结合详细的构造解析，厘定了鹰扬关构造带的构造变形序列、大地构造属性和构造演化过程。
(1)鹰扬关构造带主要由新元古代中—晚期岛弧型安山岩和玄武岩、裂谷型双峰式火山岩、盖帽碳酸盐岩与泥砂岩等物质组成，其在新元古代晚期裂谷和伸展构造背景下因重力作用经沉积混杂而形成。
(2)鹰扬关构造带主要记录了广西期(450～415 Ma)近E—W向褶皱和逆断层作用、印支晚期(227～220 Ma)NNE—SSW向褶皱和左旋韧性剪切和燕山期NNE—SSW向断层活化(正断作用和右行左滑)。
(3)结合物质组成、构造变形序列与年代学数据，建立了鹰扬关构造带新元古代中—晚期、广西期、印支晚期与燕山期等4期构造演化过程。
致谢：感谢梁承华博士在野外地质调查中给予的帮助，感谢南京大学舒良树教授和另一位审稿专家对文章提出的宝贵建议，使得文章质量得以提升。
注 释 / Note
❶ 中国地质调查局武汉地质调查中心. 2016. 1 ∶50000富川县幅、涛圩幅、桂岭圩幅、太保圩幅区域地质矿产调查报告.武汉：中国地质调查局武汉地质调查中心.
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