2021, Vol. 37
2. 东华理工大学地球科学学院, 南昌 330013
2. School of Earth Science, East China University of Technology, Nanchang 330013, China
龙头寨群一名系广东地质局761队4分队创名于曲江县灵溪的龙头寨山，原指粤北地区中上奥陶统的砂页岩、石灰岩及部分硅质岩，并以中部石灰岩为标志划分为下、中、上三个亚群。广东省地质矿产局(1996)在清理岩石地层单位时，将原龙头寨群下亚群上部、中亚群和上亚群分别引用江西南部的半坑组、古亭组、黄竹洞组；丁辉等(2017)在粤北始兴司前-赣南全南南迳一带创建南迳组，并将其归入龙头寨群，作为龙头寨群顶部的一个组。至此，龙头寨群自下而上进一步划分为半坑组、古亭组、黄竹洞组和南迳组。半坑组未见化石，广东省地质矿产局(1996)根据整合于其下的长坑水组含中奥陶世笔石化石(南颐, 1995)，推测其地质时代属中晚奥陶世。古亭组在粤北含牙形刺化石Cornuodus longibsis、Paltodus inconstans、Oistodus sp.等，指示的地质时代属早-中奥陶世(安太庠, 1987)；在赣南含珊瑚化石Palaeophyllum sp.、腕足类化石Ancistorhyncha sp.和腹足类化石Donaldiella sp.等，指示的地质时代属晚奥陶世(江西省地质矿产厅, 1997)。黄竹洞组在粤北未见化石，广东省地质矿产局(1996)推测其地质时代为晚奥陶世；赣南黄竹洞组下段产晚奥陶世笔石化石，上段近2000m厚的沉积碎屑岩层也未见化石，江西省地质矿产厅(1997)将黄竹洞组下段归于晚奥陶世，并推测黄竹洞组上段可能还包括早志留世沉积。南迳组为火山岩系，赣南南迳盆地安山岩和英安岩SHRIMP锆石U-Pb年龄分别为442.1±3.9Ma和439.9±3.7Ma(丁辉等, 2017)，粤北河口盆地碎斑熔岩SHRIMP锆石U-Pb年龄为443.6±5.4Ma，指示的地质时代属晚奥陶世末期-早志留世初期(巫建华等, 2012; 丁辉等, 2017; 刘帅等, 2018)。可见，粤北黄竹洞组及赣南黄竹洞组上段的地质时代归属及其与南迳组的时代关系还缺乏有效的制约。
另一方面，钦(州湾)-杭(州湾)结合带是扬子古板块与华夏微古板块的巨型构造结合带，经历了不同性质与规模的构造运动(张国伟等, 2013)，因地质构造复杂，分岐较大，特别是早古生代结合带两侧的大陆边缘属性存在不同的认识。钦-杭结合带中段由半坑组、古亭组和黄竹洞组组成的原龙头寨群，为一套细粒长石石英砂岩、绢云板岩、粉砂质板岩或千枚岩夹碳酸盐岩，上部夹含凸镜状砾岩的沉积组合，似乎显示被动大陆边缘的沉积特征。但粤北始兴-赣南全南一带南迳组火山岩晚奥陶世末期-早志留世初期的地质时代厘定(巫建华等, 2012; 丁辉等, 2017; 刘帅等, 2018)和岛弧火山岩的地球化学特征确认(丁辉, 2016; 劳玉军, 2017; 刘帅等, 2018; 马树松等, 2019)，说明钦-杭结合带中段晚奥陶世末期-早志留世初期可能属活动大陆边缘。可见，黄竹洞组地质时代以及与南迳组的接触关系的确认，是解决龙头寨群沉积构造属性和钦-杭结合带中段早古生代构造背景的关键。为此，本文以钦-杭结合带中段粤北始兴河口一带龙头寨群黄竹洞组顶部首次发现的火山岩夹层研究对象，通过野外考察、代表性地层剖面测制、火山岩岩相学研究和SHRIMP锆石U-Pb测年测定，确定黄竹洞组的地质时代，再结合上覆南迳组火山岩锆石U-Pb年龄确定黄竹洞组与南迳组的时代关系，并探讨钦-杭结合带中段早古生代的构造背景。
1 大地构造背景粤北位于扬子古板块与华夏微古板块之间的钦-杭巨型构造结合带中段(周永章等, 2012)以东，华夏微古板块西部边缘(图 1a)。钦-杭结合带自早元古代，经中、新元古代至早古生代大致经历了“三合、两开”(杨明桂和梅勇文, 1997)的构造演化。早元古代，随着全球哥伦比亚超级大陆的形成，扬子陆块与华夏陆块连为一体，形成统一的华南原始陆壳；中元古代早期，随着哥伦比亚超级大陆裂解，华南原始陆壳开始分离为以古华南洋相隔的扬子始板块和华夏微始板块(胡雄健等, 1991; 邢凤鸣等, 1992; 甘晓春等, 1995, 1996; 杨明桂和梅勇文, 1997; 李献华等, 1994, 1998; 刘锐等, 2009; 于津海等, 2009; 刘潜, 2013; 梁锦等, 2015)；新元古代早期，随着罗迪尼亚超级大陆形成，古华南洋闭合，扬子始板块与华夏微始板块拼合成统一的华南始板块(Li et al., 2007, 2008c)；南华纪-早古生代早期，随着罗迪尼亚(Rodinia)超级大陆的裂解，华南始板块沿钦杭构造带再次裂解为以洋盆相隔的扬子古板块和华夏微古板块(彭松柏等, 2006; 王鹤年和周丽娅, 2006; Yan et al., 2006; Yu et al., 2008; 何卫红等, 2014)；早古生代晚期，华南洋再次关闭形成钦杭加里东期结合带，扬子古板块与华夏微古板块再次拼合，地壳隆升遭受剥蚀，沿拼合带多数地区缺失志留纪地层，发育奥陶纪-志留纪岛弧型花岗岩、火山岩和区域绿片岩相-低角闪岩相变质作用(杨树锋等, 1995; 张芳荣等, 2009; 邢光福等, 2013; 何卫红等, 2014; 易立文等, 2014; 曾长育等, 2015; 劳玉军, 2017; 马树松等, 2019)。
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图 1 钦杭带基本构造格架(a, 据陈毓川等, 2013)和赣南-粤北地区地质简图(b) 1-第四系；2-泥盆系；3-上奥陶统-下志留统火山岩；4-寒武系-上奥陶统变质砂岩；5-燕山中期花岗岩；6-印支晚期花岗岩；7-印支早期花岗岩；8-加里东期花岗岩；9-地质界线；10-角度不整合接触；11-区域深大断裂和主要断裂；12-剖面位置 Fig. 1 The basic tectonic framework of Qin-Hang joint zone (a, after Chen et al., 2013) and geological sketch map of the South Jiangxi-North Guangdong (b) 1-Quaternary; 2-Devonian; 3-Upper Ordovician-Lower Silurian volcanic rocks; 4-Cambrian-Upper Ordovician metamorphic sandstone; 5-Middle Yanshanian granite; 6-Late Indosinian granites; 7-Early Indosinan granites; 8-Caledonian granites; 9-geological boundary; 10-angular unconformity contact; 11-regional abyssal faults and major faults; 12-section position |
粤北黄竹洞组地层出露局限，植被茂密，天然露头较少，为进一步确定黄竹洞组类复理石沉积层序，在粤北河口地区选择一段岩性出露较好的地段，测制了剖面A-A′(图 1b、图 2、图 3)，剖面起点坐标为24°45′39″N、114°05′12″E，终点坐标为24°44′03″N、114°04′58″E，剖面层序描述如下：
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图 2 黄竹洞组碳质板岩与火山岩夹层 (a)碳质板岩与火山岩互层剖面；(b)碳质板岩局部放大；(c)夹层火山岩局部放大 Fig. 2 Carbonaceous slate and volcanic interbedded of Huangzhudong Formation (a) interbedded profile of carbonaceous slate and volcanic rock; (b) fractionated gain of carbonaceous slate; (c) fractionated gain of interbedded volcanic rocks |
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图 3 粤北黄竹洞组实测地层剖面图(A-A′) Fig. 3 Geological section of the Huangzhudong Formation in northern Guangdong Province (A-A′) |
上覆地层：南迳组碎斑熔岩、流纹岩、流纹质凝灰岩(未及顶)＞69.12m
——————————————整合——————————————
黄竹洞组(O3hz) ＞430.04m
(18) 浅黄色细粒石英砂岩夹火山岩及薄层粉砂岩 98.04m
(17) 灰色碳质板岩 0.51m
(16) 流纹质 0.51m
(15) 灰色碳质板岩 0.45m
(14) 流纹岩 4.30m
(13) 灰色碳质板岩 0.85m
(12) 流纹岩、流纹质凝灰岩 4.71m
(11) 灰色碳质板岩 0.28m
(10) 碎斑熔岩、流纹岩 4.32m
(9) 灰色碳质板岩 0.34m
(8) 碎斑熔岩 2.28m
(7) 灰色碳质板岩 0.28m
(6) 透镜状流纹岩 0.27m
(5) 片理化灰色碳质板岩夹薄层灰褐色硅化粉砂岩 67.96m
(4) 浅灰色粉砂岩夹紫红色砂岩夹少量灰色碳质板岩 101.28m
(3) 黄褐色石英砂岩与浅灰色粉砂质板岩互层 57.04m
(2) 紫红色细粒砂岩和灰绿色条带状粉砂岩互层 23.10m
(1) 紫红色细粒石英砂岩(未及底) 45.08m
在实测剖面A-A′上，黄竹洞组底部主要为紫红色细粒石英砂岩、紫色细粒砂岩与灰绿色条带状粉砂岩互层、黄褐色石英砂岩与浅灰色粉砂质板岩互层、浅灰色粉砂岩夹紫红色砂岩互层为主(图 2a)，厚21.3~101.28m；中部主要为灰色碳质板岩与火山岩互层(图 2b, c)，碳质板岩厚度不大，火山岩厚度从下到上厚度有逐增趋势；顶部主要为火山岩与片理化灰色碳质板岩互层、片理化灰色碳质板岩夹薄层灰褐色硅化粉砂岩组合，局部可见透镜状火山岩，夹层火山岩与浅变质岩组合的产状一致(图 3)。黄竹洞组与上覆南迳组凝灰岩为整合接触。
3 岩相学特征粤北黄竹洞组流纹岩遭受了变质变形改造，但变质程度低，仅达低级绿片岩相，原始结构基本保存，容易识别。显微镜下观察发现，流纹岩变质作用明显，可见绢云母定向排列充填在基质中(图 4)；样品具斑状结构(图 4a)；斑晶含量约占45%，主要为石英(30%)、长石(5%)和云母(10%)；石英斑晶晶形整体较差，半自形-他形，干涉色一级白至一级黄白，波状消光，具有熔蚀现象，呈不规则港湾状(图 4a, b, f, g)；黑云母呈条带状，正交偏光下呈棕黄色和蓝色(图 4b, d)；大部分长石斑晶发生了蚀变作用，绢云母化比较明显(图 4c, d, f)；局部可见保存较好的斜长石，具聚片双晶(图 4c, d, h)，可见少量钾长石(图 4a)；基质为隐晶质(55%)，由石英、长石微晶和绢云母(白云母)定向排列组成。
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图 4 粤北黄竹洞组流纹岩显微照片 (a)斑状结构；(b)条带状黑云母；(c)长石绢云母化；(d、h)长石聚片双晶；(e、g)石英斑晶熔蚀；(f)长石蚀变. Q-石英；Pl-斜长石；Bt-黑云母；Ms-白云母；Ser-绢云母；Kfs-钾长石 Fig. 4 Rhyolitic micrographs of Huangzhudong Formation in northern Guangdong Province (a) porphyritic texture; (b) stripped biotite; (c) sericitization of feldspar; (d, h) polycrystalline twin of feldspar; (e, g) corrosion of quartz porphyry; (f) corrosion of feldspar. Q-quartz; Pl-plagioclase; Bt-biotite; Ms-muscovite; Ser-sericite; Kfs-k-feldspar |
为确定黄竹洞组夹层火山岩的地质时代，在剖面上选取火山岩新鲜样品HK101和HK102各10kg，碎样至80~120目，由南昌华地科技有限公司利用重力法、电磁法分选出锆石，在双目镜下挑选晶形和透明度较好的锆石颗粒；将样品锆石与标样锆石一起制靶固结后，用环氧树脂固定、抛光，在光学显微镜下进行锆石样品的反射光和透射光观察，在扫描电镜下拍摄阴极发光图像。透射光、反射光和阴极发光成像SHRIMP锆石U-Th-Pb同位素测定在中国地质科学院地质研究所(北京离子探针中心)完成。测试仪器为澳大利亚科学仪器公司制造的SHRIMP-Ⅱ型。详细分析流程及计算原理见宋彪等(2002)。使用Ludwig博士编写的Squid 1.0及Isopolt程序对分析数据进行处理及年龄计算。测试结果见表 1。
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表 1 黄竹洞组流纹岩SHRIMP锆石U-Pb分析结果 Table 1 SHRIMP zircon U-Pb dating of the volcanic rocks of Huangzhudong Formation |
样品HK101和HK102流纹岩中锆石均呈自形长柱状或双锥状，晶形较好，可见清晰地韵律环带(图 5)；大部分锆石长度位于120~245μm之间。样品HK101中15颗测试锆石的U含量为148×10-6~886×10-6(均值为488×10-6)，Th含量为60×10-6~284×10-6(均值为159×10-6)，Th/U值为0.28~0.46(均值0.35)；样品HK102中15颗锆石(16个测点)，U含量为142×10-6~633×10-6(均值365×10-6)，Th含量为60×10-6~349×10-6(均值为166×10-6)，Th/U值为0.33~0.63(均值为0.47)；具有岩浆成因锆石的成分特征(Williams and Claesson, 1987; Rubatto, 2002; 吴元保和郑永飞, 2004)。样品HK101的15个测试点的206Pb/238U年龄变化范围为444~427Ma，在U-Pb协和曲线上集中分布(图 6)，加权平均值为436.2±2.1Ma (MSWD=1.6)；样品HK102的16个测试点的206Pb/238U年龄变化范围为452~429Ma，在U-Pb协和图中集中分布(图 6)，加权平均年龄值为438.7±2.1Ma (MSWD=1.17)。可见，2个样品的锆石U-Pb年龄为439~436Ma，代表流纹岩的形成年龄。
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图 5 粤北黄竹洞组流纹岩锆石阴极发光图像 Fig. 5 Cathodoluminescence photos (CL) images of zircons from rhyolites of Huangzhudong Formation in northern Guangdong Province |
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图 6 粤北黄竹洞组流纹岩锆石U-Pb年龄谐和图 Fig. 6 U-Pb concordia diagrams of zircons from rhyolites of Huangzhudong Formation in northern Guangdong Province |
本文获得的龙头寨群黄竹洞组顶部流纹岩的SHRIMP锆石206Pb/238U年龄为439~436Ma，根据《国际年代地层表》(2018/08版)，中志留统/下志留统、下志留统/上奥陶统和上奥陶统/中奥陶统的界限分别划在433.4±0.8Ma、443.8±1.5Ma和458.4±0.9Ma(樊隽轩等, 2018)，指示流纹岩的地质时代属早志留世早期。考虑到黄竹洞组顶部流纹岩之下的变质沉积岩层厚约2000m，且在赣南的黄竹洞组底部产有五峰期笔石化石(江西省区域地质调查队, 1988①)以及下伏的古亭组产有晚奥陶世的牙形刺化石(安太庠, 1987)，将龙头寨群黄竹洞组的地质时代归于晚奥陶世-早志留世早期是可靠的。
① 江西省区调地质调查队. 1988. 江西省崇义地区“下关群”时代的研究报告
5.2 龙头寨群黄竹洞组与南迳组呈整合接触关系丁辉等(2017)将赣南全南一带火山岩创建南迳组时，依据南迳组以安山岩-英安岩为主夹板岩、千枚岩，而龙头寨群半坑组、古亭组和黄竹洞组以砂页岩、石灰岩及部分硅质岩为主顶部夹火山岩，且半坑组、古亭组和黄竹洞组的化石资料指示的地质时代与南迳组同位素年龄数据指示的地质时代吻合，认为黄竹洞组与南迳组为整合接触，并将南迳组归入龙头寨群。本文获得的黄竹洞组顶部火山岩夹层流纹岩SHRIMP锆石加权平均值年龄分别为436.2±2.1Ma(n=15，MSWD=1.60)和438.7±2.1Ma(n=16，MSWD=1.17)，与上覆南迳组碎斑熔岩SHRIMP锆石U-Pb年龄(443.6±5.4Ma；巫建华等, 2012)在误差范围内一致，属同期火山活动的产物，说明黄竹洞组变质岩系与南迳组的时代连续，进一步证明两者为整合接触关系。
5.3 龙头寨群具有活动大陆边缘的岩石组合特征龙头寨群半坑组、古亭组和黄竹洞组浅变质岩系主要为一套深灰色、灰色、灰绿色细粒长石石英砂岩、绢云板岩、粉砂质板岩或千枚岩夹碳酸盐岩，上部夹含凸镜状砾岩的沉积组合，由于以前未发现火山岩，似乎显示出被动大陆边缘的岩石组合特征。随着赣南全南-粤北始兴一带厚度超过500m的南迳组碎斑熔岩、英安岩、安山岩(巫建华等, 2012; 伍静等, 2014; 丁辉等, 2017)的并入，龙头寨群成为厚度超过800m的变质火山岩-沉积岩组合，显示出活动大陆边缘的岩石组合特征。特别是赣南-粤北南迳组英安岩、安山岩(丁辉, 2016; 劳玉军, 2018)和同期花岗岩(马树松等, 2019)具有岛弧岩浆岩地球化学特征的确认，更有利地证实南迳组火山岩和同期花岗岩属活动大陆边缘的产物。本文确认龙头寨群黄竹洞组流纹岩与南迳组火山岩属同期火山作用的产物，进一步证实龙头寨群具有活动大陆边缘的岩石组合特征。
5.4 钦杭结合带中段属加里东期洋壳俯冲-碰撞造山带钦杭结合带加里东期是否存在洋盆，一直是地质界关注和争论的焦点，并引发了钦杭结合带加里东期是俯冲-碰撞造山带还是板内造山造山带的争论。尽管很多地质工作者从沉积地层、岩浆岩、变质岩及构造方面提供了加里东期俯冲-碰撞造山的地质证据(Guo et al., 1989; 李曰俊等, 1993; 刘宝珺等, 1993; 殷鸿福等, 1999; 曾勇等, 1999; 吴浩若, 2000; 郭令智, 2001; 尹福光等, 2001; 马瑞士, 2006; 彭松柏等, 2006; 刘运黎等, 2009; 潘桂棠等, 2009; 许效松等, 2012; Zhao and Cawood, 2012; 覃小锋等, 2013, 2015; 陈相艳等, 2015; Zhang et al., 2015)，但因缺少与区域上广泛分布的加里东期花岗岩(楼法生等, 2005; 伍光英等, 2008; Li et al., 2010; Wang et al., 2011, 2013; Zhang et al., 2012; 王磊等, 2013)同期的岛弧火山岩或与洋壳俯冲相关的早古生代蛇绿岩证据，不具备洋-陆俯冲活动大陆边缘特征，有学者认为其属板内造山(周新民, 2003; 王德滋, 2004; 舒良树, 2006; 柏道远等, 2007; 徐夕生, 2008; 张爱梅等, 2010; 郝义等, 2010; Wang et al., 2010; Shu et al., 2011; Wang et al., 2011, 2012; Xu et al., 2011; 陈旭等, 2012; 杜远生和徐亚军, 2012)。
综合前人研究成果，钦杭结合带西南段晚奥陶世-早志留世应处于活动大陆边缘环境，存在俯冲-碰撞造山作用。蛇绿岩或岛弧火山岩作为判别洋壳俯冲-碰撞造山作用的关键性证据，云开隆起地区西北缘桂东南糯垌蛇绿岩，大爽一带形成于俯冲岛弧的弧前构造环境下的高镁-镁质玄武安山岩-安山岩(430~441Ma)(彭松柏等, 1999, 2016a, b)和俯冲-碰撞构造环境下具TTG特征的深熔花岗杂岩(443Ma)(彭松柏等, 2006; 覃小锋等, 2013)等，证实钦杭结合带西南段存在加里东期洋壳俯冲-碰撞造山作用。另一方面，在钦杭结合带东段，江西横峰、金溪出露早古生代花岗岩，由于缺少相匹配的同期火山岩系，则不具备洋陆俯冲活动大陆边缘特征(孙涛, 2006; 舒良树等, 2008)，江西弋阳、浙江龙游、闽中等地虽然发现了经历早古生代高压高温变质麻粒岩(于津海等, 2014)和高压变质石榴石角闪岩(周国庆等, 1989; 邢光福等, 2013; Zhang et al., 2015; 陈相艳等, 2015)，但高压高温变质麻粒岩和高压榴辉岩的出现并不能说明洋壳一定存在，高压高温变质麻粒岩和高压榴辉岩不限出现于俯冲造山带，且与大洋板块俯冲有关的造山带往往发育双变质带，特别是低温高压变质作用。
钦杭结合带中段虽然没有发现蛇绿岩，但存在与洋壳俯冲有关的岛弧火山岩和花岗岩。如，覃小锋等(2015)在广西桂东鹰扬关地区发现识别的早古生代志留世(415Ma)与俯冲-消减作用有关的细碧岩、石英角斑岩及相关火山碎屑岩；易立文等(2014)在粤北河口-上洞发现的早古生代晚奥陶世钙碱性英安岩(449Ma)；粤北始兴-赣南全南发现的早古生代英安岩(439Ma)、安山岩(442Ma)(丁辉, 2016; 劳玉军, 2017)、花岗岩(442Ma)(马树松等, 2019)；粤北一带和猫儿山-越岭高镁玄武岩-安山岩-英安岩和辉长岩(Yao et al., 2012; Wang et al., 2013)；湘东板杉铺埃达克质花岗闪长岩(423Ma)(许德如等, 2006)；永州-衡阳-新余发现的TTG-GG组合(何卫红等, 2014; 邓晋福等, 2016; 许华等, 2016)等均表现与活动大陆边缘的岛弧岩浆特征，揭示钦杭结合带中段存在加里东期洋壳俯冲。本文研究的钦杭结合带中段粤北始兴一带龙头寨群具有活动大陆边缘的沉积组合特征，进一步说明晚奥陶世-早志留世早期的洋盆已延伸到了钦杭结合带中段。可见，在南华纪-早古生代Rodinia大陆裂解背景下，扬子与华夏板块可能沿钦杭结合带自南西向北东方向呈剪刀叉式裂解，至少在晚奥陶世晚期-早志留世早期钦杭结合带西南段和中段已裂解形成洋盆，中-晚志留世西南段和中段发生洋壳俯冲，晚志留世末洋盆闭合形成加里东造山带。
6 结论综上所述，可得出以下结论：
(1) 龙头寨群黄竹洞组顶部流纹岩夹层2个样品的SHRIMP锆石206Pb/238U年龄分别为438.7±2.1Ma(n=15，MSWD=1.6)和436.2±2.1Ma(n=16，MSWD=1.2)，指示流纹岩的锆石U-Pb年龄为439~436Ma，地质时代属晚奥陶世末期-早志留世早期；
(2) 黄竹洞组顶部流纹岩的锆石U-Pb年龄与上覆南迳组安山岩、英安岩、流纹岩和碎斑熔岩的锆石U-Pb年龄在误差范围内一致，指示它们是同期火山活动的产物，为黄竹洞组和南迳组呈整合接触提供了年龄证据。
(3) 龙头寨群黄竹洞组顶部流纹岩及南迳组火山岩系晚奥陶世末期-早志留世早期的地质时代厘定，为龙头寨群属含有大量火山岩的活动大陆边缘沉积组合提供了依据，支持钦杭结合带中段加里东期属俯冲-碰撞造山带。
致谢 东华理工大学2016级资源勘查专业本科生黄志成和涂传辉参加了野外地层剖面测制工作；北京离子探针中心包泽民博士、孙会一博士在锆石阴极发光照相和锆石U-Pb同位素测试过程中给予了指导和帮助；匿名审稿人提出了宝贵意见；在此一并致以诚挚的感谢。
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