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作者简介:

侯明才,男,1968年生。教授,博士生导师,主要从事大地构造沉积学、含油气盆地分析、层序岩相古地理学等领域的研究。E-mail: houmc@cdut.edu.cn。

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目录contents

    摘要

    典型加里东运动指的是晚志留纪时期亚匹特斯洋关闭导致现今大西洋两侧出现的一系列区域不整合、强烈变质-变形和花岗岩侵位事件的大陆碰撞和远程推覆作用。华南在该时期也发生了明显的造山作用,但却与经典的加里东运动相去甚远。本文在系统总结了华南加里东期造山表现的基础上,通过对比典型加里东造山带,明确提出了华南加里东期“非典型”造山的概念及特征:空间上自东向西逐渐变新大规模面状花岗岩、非线状花岗岩且缺乏典型火山岛弧属性基性岩及大洋残余物,区域性角闪岩相—绿片岩相变质,缺乏典型的高温麻粒岩及线状高压—超高压变质岩带,存在多期次多阶段的空间分异但同一期次华南板块内部沉积建造连续过渡—不存在截然的空间分界线。另一方面,从探讨“非典型”造山形成的地球动力方向、来源与动力学机制的角度,提出了需要进一步解决的关键科学问题:以雪峰山—九岭山一线为界,泥盆系与前泥盆系接触关系自东向西表现为高角度不整合、低/微角度不整合向平行不整合的过渡,前泥盆系变形主要表现为从南到北由轴迹近E-W向为主转变为轴迹近NE-SW向为主的不同形态的褶皱,但仍需有效手段排除印支期或燕山期构造运动对加里东期褶皱变形的影响,对动力学机制的进一步探讨也需在此基础上进行;华南板块在早古生代“非典型”造山过程中与其他板块之间的位置关系是如何,华南板块尺度的沉积响应如何与全球尺度的构造古地理格局耦合;这一种“非典型”造山的动力学过程究竟是华南内部俯冲-碰撞/斜向碰撞-走滑造山模式,华南板块内部的板内造山,华南板块与东冈瓦纳板块俯冲-碰撞造山模式,还是东、西华夏地块之间的洋-陆碰撞造山。通过回答上述问题,可为探讨华南早古生代造山的地质过程提供重要依据,同时为理解全球不同“非典型”造山提供典型示例。

    Abstract

    The representative Caledonian Orogeny is defined as the late Silurian continent-continent collision and remote-thrusting associated with the closure of the Iapetus Ocean, resulting in a series of regional unconformities, intense metamorphism, deformation and granitic intrusions on the borders of the present Atlantic Ocean. The South China block is also considered to have experienced significant early Paleozoic movements the but bears little resemblance to the classical Caledonian Orogeny. In this paper, we propose the concept and characteristics of the “atypical” Caledonian orogenesis in South China through a comparison with representative Caledonian Orogen: ① Large-scale gradually younger westward planar and non-linear granites but lacks of typical arc-affiliated basic rocks and oceanic relics. ② Regional amphibolite-greenschist facies metamorphism with an absence of typical high-temperature granulites and linear high-ultrahigh-pressure metamorphic rock belts. ③ Spatial differentiation of multi-stages sedimentary formations, yet there were no clear boundaries and continuous transition of sediments within the block at the same stage. We also propose some crucial scientific issues that need further resolution from the perspective of the geodynamic mechanisms: ① The contact relationship between Devonian and pre-Devonian strata transitions from high-angle and low/minor angle unconformity to parallel unconformity through east to west devided by Xuefeng Mountains-Jiuling, and the deformation of pre-Devonian formations manifested in different forms of folds with axial traces from nearly E-W-oriented in the south to NE-SW in the north, however, effective means are still needed to eliminate the influence of subsequent Indosinian or Yanshanian movements, which is the basis of further discussion on geodynamic mechanisms. ② The positional relationship between South China and other plates during the early Paleozoic, and coupling relation between sedimentary records at the plate scale and the global tectonic. ③ Whether the dynamic process of this “atypical” orogenesis corresponds to a model of subduction-collision/oblique strike-slip-collision within South China, intraplate orogens, subduction-collision between South China and East Gondwana, or ocean-continent collision between east and west Cathaysia, remain to be determined. Answering these questions can provide significant insights into the geological processes of the Early Paleozoic orogenesis in South China and possibly serve as a typical example for understanding other “atypical” orogenesis globally.

  • 早古生代是全球罗迪尼亚超大陆裂解到潘基亚超大陆聚合的重要过渡时期,在这过程中发生了泛非期和加里东期地质事件,改变了全球多数板块的洋-陆格局。加里东期活动主要发生于北方大陆的边缘,450~400 Ma期间出现俯冲、碰撞、陆内造山等多种构造运动。华南在该时期也形成了泥盆系与下伏地层的区域性不整合,并发育了广泛的面状花岗质岩浆,该期构造运动奠定了其大地构造基本格局和沉积盆地演化基础。然而与经典的全球性加里东造山作用含义和特点不同,华南的加里东期造山运动缺少蛇绿岩、火山岩和同期高压变质岩记录,因此本文将其定义为“非典型”造山。随着对华南加里东期构造-岩浆-沉积演化过程研究的不断深入,这种“非典型”造山动力源和成因机制(俯冲/增生/碰撞/陆内造山)成为了众多国内外地质专家关注和研究热点,并出现了多种不同的动力学模型,而华南(扬子/华夏)板块在冈瓦纳大陆中的具体位置、与其他板块的亲缘性也存在着争议。而“非典型”造山背景下的沉积响应是理解“非典型”造山过程及其构造环境演化的重要科学问题,可为“非典型”造山成因机制提供重要依据。因此,本文拟通过华南在加里东期出现“非典型”造山具体表现的综述,对比分析不同区域出现的地层接触类型、褶皱变形样式、沉积填充差异以及仍需解决的关键问题,讨论了可能的作用类型和地球动力学过程,试图从古地理格局重建和板块重建的角度探讨“非典型”造山的研究意义。

  • 1 “加里东运动”的概念

  • 1788年,被称为“现代地质学之父”的苏格兰地质学家詹姆斯赫顿(James Hutton)为了寻找不整合的时间间断意义,在苏格兰的西卡角发现了345 Ma水平产状的泥盆纪红色砂岩直接覆盖在了425 Ma产状陡倾的志留系之上,将其定义为一次区域性上升引起的沉积间断-剥蚀。1906年,苏斯(Suess)利用在19世纪文学中常用来指代苏格兰高地的“加里东”一词(Caledonia),首次在构造意义上提出起源于挪威、穿过苏格兰并延伸至爱尔兰和威尔士在泥盆纪之前形成的“加里东山脉”。随后斯蒂尔(Stille)在1924年重新定义了“加里东运动”,认为是志留纪末期全球性众多短暂造山运动的代表之一,英国地质学家埃文斯和斯塔布尔菲尔德(Evans and Stubblefield)在1929年进一步对“加里东运动”的影响范围和时限加以了约束(McKerrow et al.,2022)。随着对岩浆-变质作用研究的逐渐深入,发现在除了英格兰—苏格兰地区的其他板块之间也存在着活跃的早古生代汇聚作用,是潘基亚超大陆形成之前的一次全球性造山作用。根据已知的年代学证据、岩浆-变质类型及其时空分布,目前普遍认为,全球自罗迪尼亚超大陆裂解之后,在早古生代主要形成了泛非造山带和加里东造山带,分别与750~530 Ma期间南方冈瓦纳大陆与 490~400 Ma期间亚欧大陆的主体集结相关。后者按照发生时间的先后顺序,可具体分为:冈瓦纳大陆边缘活动带(例如530~380 Ma东澳大利亚-塔斯马尼亚造山带)、490~390 Ma的欧洲经典加里东造山带、490~410 Ma美洲阿巴拉契亚(Appalachia)加里东期造山带和450~440 Ma中欧加里东期造山带, 460~440 Ma亚洲与原特提斯洋和古亚洲洋演化相关的加里东期造山带(图1),主要体现在陆缘的增生或活化(李三忠等,2016;任留东和王浩,2023)。

  • 而传统的“加里东造山带”是指现今北大西洋前身亚匹特斯洋盆(Iapetus Ocean)在约420 Ma闭合,陆-陆碰撞导致在该区域形成具有准同时性的东格陵兰造山带(E.Greenland Caledonides)、挪威-苏格兰造山带、阿巴拉契亚加里东造山带(具体表现见下文)。“加里东运动”可用来表示上述地区的碰撞造山运动,但在其他板块同时期的运动(例如阿巴拉契亚碰撞造山、冈瓦纳边缘的增生造山或可能的华南陆内造山)一般不用此术语。为对比直观,本文中对亚洲大陆或其他陆块此间的运动称之为“加里东期”事件或构造。全球8 个主要的加里东期造山带(挪威—苏格兰、阿巴拉契亚、东格陵兰、西伯利亚南缘、东澳大利亚—塔斯马尼亚、秦岭—祁连山、中-南天山、华南东南部华夏褶皱带)均位于北方大陆周边(图1),集中于非冈瓦纳陆块边缘,或与冈瓦纳古大陆相邻的位置。因此,加里东运动主要体现在晚寒武世至早泥盆世(490~390 Ma)仅限于现今北大西洋东、西两岸范围内的构造运动,伴随洋盆闭合、裂谷封闭、古老造山带再活化的过程表现为区域性不整合、强烈的变质-变形和花岗岩侵位,而同时期冈瓦纳大陆陆缘其他位置的增生或活化,例如,包括华南板块在内与原特提斯洋和古亚洲洋演化相关的陆块群之间或内部的复杂相互作用,则称为加里东期构造运动。

  • 2 加里东期“典型造山”主要表现

  • 加里东期“典型造山”是由亚匹特斯洋闭合导致陆-陆碰撞造山和远程推覆作用,主要形成东格陵兰岛、挪威-苏格兰、以及阿巴拉契亚造山带(图2)。

  • 东格陵兰加里东造山带位于格陵兰半岛东部,呈NE走向,长约1300 km,发育大规模的褶皱推覆体、逆冲断层,是由劳伦古陆和波罗的陆块在439~408 Ma期间斜向汇聚陆-陆碰撞形成的(Keller and Hatcher,1999)。典型特征表现在:① 早古生代地层发生褶皱变形,并造成泥盆系与下伏地层呈明显的角度不整合(White et al.,2002; Braun et al.,2007);② 发育446 Ma、438 Ma、425 Ma三期S型花岗岩、钙碱性花岗岩等酸性侵入岩(Kalsbeek et al.,2001; Augland et al.,2012);③ 发育439~414 Ma、409~360 Ma两期超高压变质榴辉岩,且加里东期碰撞花岗岩、前寒武纪沉积岩经历了430~420 Ma的高级变质作用(White et al.,2002; Dhuime et al.,2007)。

  • 阿巴拉契亚加里东造山带位于北美克拉通东缘,呈NE-SW走向,为古生代环冈瓦纳大陆北缘的阿瓦隆尼亚、卡罗莱纳、卡多姆和Meguma 等微陆块与北美克拉通在490~410 Ma期间经过多阶段陆-陆碰撞形成的增生造山带。典型特征表现为:① 区域上志留纪—早泥盆世的地层与上覆地层不整合接触,不整合面之下的地层发生强烈变形和走滑作用,之上局部发育磨拉石沉积充填(Osberg,1988);② 缝合带中发育467~462 Ma蛇绿岩套与冲断变形构造;③ 中—南段发育480~435 Ma与弧-陆碰撞作用相关的S型花岗岩和459~394 Ma的高压榴辉岩,并在局部发生绿片岩相和角闪岩相的变质作用(Wones et al.,1988; Miller et al.,2010)。

  • 图1 志留纪晚期全球古地理图及冈瓦纳大陆周缘造山带示意图(下图修改自Cawood et al.,2021

  • Fig.1 Late Silurian global paleogeography and schematic representation of Gondwana's peripheral orogens (the figure below modified after Cawood et al., 2021)

  • 挪威-苏格兰加里东造山带北东为斯堪的纳维亚造山带,南西为英国造山带。该加里东造山带发育一条NE-SW走向新元古代晚期—早奥陶世早期的蛇绿岩缝合带,即Iapetus缝合带。其中,斯堪的纳维亚造山带由波罗的陆块与4个逆冲推覆体在445~410 Ma拼合形成的(Roberts,2003)。该造山带典型特征主要表现在:① 逆冲推覆体与波罗的陆块基底呈断层接触,具有亲劳伦大陆和亲波罗的陆块混合动物群化石的砾岩层(约485~464 Ma)与波罗的板块基底呈角度不整合接触(Roberts,2003);② 505~391 Ma的榴辉岩广泛分布(Kylander et al.,2009; Janák et al.,2013);③ 发育晚寒武世—早奥陶世的岛弧火山岩和晚志留世的S型花岗岩(Tegner et al.,2005; Lundmark et al.,2008)。而英国造山带是490~390 Ma期间由劳伦大陆、波罗的陆块、阿瓦隆尼亚微陆块、以及Midland Valley岛弧拼贴形成(Atherton et al.,2002)。该造山带的特征主要有以下几点:① 中志留统—中泥盆统的砾岩与下伏下古生界呈角度不整合接触;② 北部以470~455 Ma弧-陆碰撞型S型花岗岩为主;中—南部区域以410 Ma的I型花岗岩为主(Oliver et al.,2008Hollis et al.,2013);③ 亚匹特斯洋最终关闭阶段,岩石发生区域性变质作用,变质程度主要以沸石相—绿片岩相为主,部分区域达到榴辉岩相(Soper,2009)。

  • 图2 加里东典型造山带位置(a)及地质简图(b,修改自李三忠等,2016; Highton et al.,2021

  • Fig.2 Location (a) and schematic map (b, modified after Li Sanzhong et al., 2016; Highton et al., 2021) of the typical Caledonian orogenic belt

  • 由上述可知,经典的环北大西洋—北冰洋区加里东造山带亚匹特斯洋闭合导致的多陆块之间陆-陆碰撞形成,整体表现为:具有同时性或准同时性,主要形成于志留纪至早泥盆世,局部形成于奥陶纪至志留纪;大部分区域泥盆系与下伏地层呈区域不整合接触或断层接触;发育线状分布的奥陶纪—泥盆纪S/I型花岗质岩浆岩记录;发育典型的高温变质岩及线状高压—超高压变质岩带;缝合带可见蛇绿岩等大洋残余物记录。

  • 3 华南的加里东期“非典型”造山特征

  • 由上文可知,加里东构造运动是早古生代发生的一次重要的全球性地质事件,已知全球主要发育8个与此相关的造山带。华南加里东期构造运动最初由Ting(1929)根据广西泥盆系莲花山组不整合在下古生界之上,提出以“广西运动”代表的华南区域性泥盆系与前泥盆系之间不整合事件为早古生代地壳运动。华南早古生代的造山运动呈现明显的期次性和区域不对称性,寒武系与奥陶系之间在右江、云开山、湘南地区、闽西地区形成的平行不整合被称为郁南运动(莫柱孙等,1980),奥陶系与志留系之间在云开山与雪峰山地区形成的角度不整合称为北流运动,在贵州一带形成的平行或角度不整合称为都匀运动(余开富和王守德,1995),湘赣地区形成的角度不整合称为崇余运动(卢华复,1962)(图3)。而传统意义上的广西运动则代表了浙江西部—湖南中西部形成的上志留统—下泥盆统之间的角度/平行不整合,又被称为Kwangsian 造山运动(Faure et al.,2009),或因早古生代韧性变形作用基本沿武夷山—云开山一带分布被称为武夷-云开造山运动(Lin Shoufa et al.,2024)。因此,Ting(1929)最初定义的加里东期地壳运动并不是一次具体的造山运动,而是以整个华南为区域的、自晚寒武世发生的多期次造山运动(杜远生和徐亚军,2012)。并且与其他7个造山带都记录有早古生代洋壳俯冲-火山岩浆活动-高压超高压变质作用不同,华南的加里东期造山带具有鲜明的地域特色(舒良树,2006),与经典的加里东造山作用含义和特点明显不同,因此本文将其定义为“非典型”造山,具体特征如下(陆松年,2004; 舒良树等,2008; 李三忠等,2016)。

  • 3.1 大规模面状花岗岩—非线状花岗岩

  • 华南早古生代“非典型”造山的发展和演变伴随着广泛的构造-岩浆事件。与典型洋-陆俯冲、陆-陆碰撞型造山带出现线状展布钙碱性岩浆岩不同,华南早古生代总体以大规模面状花岗岩为特征,展布在安化-溆浦-靖县-罗城断裂带与江山-绍兴断裂带之间(包含广西、广东、湖南、江西以及福建等地),出露面积超过20000 km2(图4)。岩性以强过铝质属性块状花岗岩与花岗片麻岩为主,全岩地球化学特征和Sr-Nd-Hf同位素组成多与S型花岗岩类似(徐先兵等,2009; Liu Rui et al.,2010; Wang Yuejun et al.,201020112012; Wan Yusheng et al.,2010; Yang Dongsheng et al.,2010; 张菲菲等,2011; Zhang Feifei et al.,2011; 王永磊等,2012; 程顺波等,2012; Zhong Yufang et al.,2013; Xia Yan et al.,2014; Shu Liangshu et al.,2015),形成时代为460~390 Ma,空间上由东向西逐渐变新,峰值年龄为440~430 Ma,缺乏同生火山岩和超镁铁质侵入岩,因此普遍认为这些岩石只有有限的地幔贡献,是由古—新元古界经部分熔融形成的壳源型花岗岩类,是后造山伸展和减压条件下的产物。近年来,随着对华南早古生代花岗岩研究的深入,一些与S型花岗岩同生的I型(435~415 Ma; Xia Yan et al.,2014; Kong Hua et al.,2021)、A型花岗岩(415~390 Ma; Yao Jinlong et al.,2012; Feng Shangjie et al.,2014),基性岩(452 Ma、473 Ma富闪深成岩,Zhong Yufang et al.,2014;409 Ma 桃园斜长角闪岩,Zhong Yufang et al.,2013;434~420 Ma,信宜、龙川、五华辉长岩,Wang Yuejun et al.,2013;443 Ma岑溪变基性火山岩,覃小锋等,2006; 以及441~438 Ma、431 Ma武夷辉长岩,Zhang Chuanlin et al.,2015a)和火山岩(445~435 Ma茶园山玄武岩、河口英安岩和流纹岩,Yao Jinlong et al.,2012; Zhang Xisong et al.,2017)陆续被发现。这些岩体出露面积有限、规模较小,且常与同时期的S型花岗岩相邻,仅见于零星地区,这可能是由于广泛的地壳内部形成的长英质岩浆对铁镁质岩浆的进一步上升与火山的喷发起到了密度屏障的作用(Xu Wenjing and Xu Xishen g,2015)。其中,零星分布的基性岩和玄武岩普遍存在“俯冲特征”(钙碱性亲和力、富集的 LILE 和亏损的 HFSE),但对其岩石成因和构造背景仍存在争议,其中部分学者认为它们是俯冲-碰撞后伸展-拆沉-底侵作用的产物,形成于俯冲-碰撞大陆边缘的火山弧构造背景(易立文等,2014; 覃小锋等,2015; 彭松柏等,2016; Zhang Chuanlin et al.,2016),另一部分学者认为是后碰撞伸展垮塌阶段岩石圏拆沉引起软流圈上涌和玄武岩底侵导致的变质基底或岩石圈地幔部分熔融的结果,或元古代俯冲带残留体在古生代垮塌重熔,属于板内造山的构造背景(弧岩浆岩特征继承自研究源区或受到地壳物质混染的影响)(Yao Jinlong et al.,2012; Wang Yuejun et al.,2013; Zhong Yufang et al.,2014),另外,Zhang Qiao et al.(2015b) 则提出华南早古生代零星出露的基性岩是华夏地块与“南海地块”陆陆碰撞形成的产物。总体而言,尽管对基性岩的属性存在争议,但华南早古生代巨量的过铝质花岗岩浆特征与典型“加里东”洋-陆俯冲型造山带存在明显的不同和地域特色。

  • 图3 华南寒武系—泥盆系划分和对比图

  • Fig.3 Cambrian-Devonian stratigraphic subdivision and correlation in the South China

  • 图4 华南加里东期花岗岩时空分布图(修改自Xin Yujia et al.,2020

  • Fig.4 Spatial-temperal distribution of Caledonian granites in South China (modified after Xin Yujia et al., 2020)

  • 3.2 区域性角闪岩相—绿片岩相变质——缺乏典型的高温麻粒岩及线状高压—超高压变质岩带

  • 华南早古生代“非典型”造山事件也在华夏地块形成了区域性变质和韧性变形作用,总体变质程度不高,呈NE向展布于陈蔡—武夷山—南岭—云开山一带。早期的区域变质仅见于云开山一带,形成寒武系552~487 Ma混合岩、487 Ma变粒岩等,变质级别为绿片岩相(李三忠,2016)。奥陶纪晚期开始发生区域性高级变质作用,变质级别达到角闪岩相—绿片岩相,变质时间集中于450~430 Ma,峰期为435 Ma左右(图5),显示近等温减压的顺时针P-T-t轨迹,表明了初始地壳增厚之后的快速剥蚀和冷却过程(Faure et al.,2009; Liu Rui et al.,2010; Wang Yuejun et al.,20122013)。然而,近年来在华南局部地区也陆续报道了少量早古生代高压—超高压变质岩或高温麻粒岩的出露,例如武夷浙江龙游溪口镇白石山头和周坞里超高压退变榴辉岩(邢光福等,2013; 汪建国等,2014; 陈相艳等,2015; Zhang Qiao et al.,2015; Cheng Hao et al.,2019)、赣东北弋阳高压麻粒岩(于津海等,2014)、陈蔡地区基性麻粒岩(Zhao Tianyu et al.,2017)、桃溪麻粒岩(于津海等,2014)、高州高温麻粒岩(Chen Chenghong et al.,2012)以及海南岛高角闪岩相变质岩(Zhang Hangchuan et al.,2022)。对于早古生代构造热事件中麻粒岩相高级变质作用,部分学者认为其记录了洋脊俯冲和板片窗打开高温、伸展构造背景下的演化历史与华南洋闭合有关(邢光福等,2013; 汪建国等,2014; 陈相艳等,2015; Zhang Chuanlin et al.,2015a; Cheng Hao et al.,2019; Xia Yanfei et al.,2024),而海南岛中奥陶世发生的变质作用是响应昆嵩地块-海南地块-澳大利亚板块与长山地块-华南板块-印度板块之间的碰撞(Zhang Hangchuan et al.,2022),但部分学者认为浙江龙游石榴角闪岩(退变榴辉岩)应为基性岩原岩的石榴石角闪岩,弋阳出露的基性麻粒岩其矿物组合为石榴子石+紫苏辉石+斜长石+黑云母,陈蔡地区出露的高级变质岩具有矽线石+石榴子石+黑云母+斜长石+钾长石+石英矿物组合,均指示了中压变质相系,并非超高压变质作用形成,不能作为扬子地块与华夏地块之间存在“华南洋”的证据(于津海和舒良树,2016)。总体而言,与典型“加里东”造山带具有明确的与俯冲-碰撞相关的高压—超高压不同,华南早古生代角闪岩相—麻粒岩相变质作用仅少量分布在远离江绍断裂的武夷和云开两个区域,沿断裂带一带为绿片岩相变质,是否具有可以指示洋-陆俯冲的高压变质岩仍需进一步证实。

  • 图5 东冈瓦纳北缘和华南早古生代构造热事件时空分布图(修改自Zhang Hangchuan,2022

  • Fig.5 The Early Paleozoic tectonothermal events in the northern margin of East Gondwana and South China (modified after Zhang Hangchuan, 2022)

  • 3.3 不存在截然的空间分界线——缺乏线状分布的大洋残余物

  • 一般认为,华南原始大陆在820~800 Ma期间发生伸展与裂解,在扬子地块东南缘地区形成了拉张性盆地与自北向南“台地—斜坡—盆地”的古地理格局,并在成冰纪—埃迪卡拉纪(720~538.8 Ma)盆地内发育了冰期—间冰期—稳定盖层沉积(牛志军等,2024)。前人通过对华南多个沉积序列进行研究发现,华夏地块在埃迪卡拉纪—奥陶纪期间发育一套厚约5600~7000 m的浅海笔石相泥沙质沉积序列夹碳质页岩和碳酸盐岩,但在晚奥陶世(460 Ma)开始发生区域抬升和海退、出现潮坪相沉积构造,海平面快速下降,原先的深水域显著变浅,至志留纪形成褶皱造山带海水全部退出、隆升成陆地(舒良树等,2021),华夏地块出现自南低北高至南高北低的古地理格局转变也响应了华南加里东期多期次抬升与造山运动,但转变的具体时间仍有待研究;而扬子-江南区埃迪卡拉纪—晚奥陶世形成了一个厚约3000~5400 m台地—浅海相碳酸盐岩沉积序列夹碳质岩、硅质岩组合,自晚奥陶世凯迪期(Katian,453~445.2 Ma)开始转变为以碎屑岩为主的局限海盆,志留纪晚期兰多维列世(Llandovery,443.8~433.4 Ma)晚期到罗德洛世(Ludlow,427.4~423.0 Ma)中晚期(约10 Ma)几乎空缺无沉积,扬子-江南区古地理轮廓与沉积特征发生了明显的变化,指示了扬子地块由东向西推移和隆升的前陆隆起(张海全等,2013; Shu Liangshu et al.,2014王怿等,2023),但有关扬子区海退成因究竟是华夏区(华夏地块)的隆升扩张还是与全球海平面升降相关,尚需寻找更多的证据。尽管扬子地块与华夏地块之间存在的古地理格局差异(整体从南低北高向南高北低过渡),但二者之间江山-绍兴断裂带两侧在成冰纪—寒武纪沉积相存在明显的沉积相过渡,并在奥陶纪趋于一致、不存在跳相(图6),由此部分学者认为成冰纪—早古生代扬子地块与华夏地块之间沉积域是相互连通的——完整的华南大陆。但也有学者认为扬子地块与华夏地块存在一定程度的沉积分异,指示二者之间存在的华南洋,华南原始大陆在前寒武纪—早古生代并不存在,扬子地块与华夏地块在早古生代末期拼合(详见下文)。然而,江山-绍断裂带两侧有关古大洋闭合的证据不足,缺乏线状分布的大洋残余沉积物与截然的空间分界线,这也与典型的“加里东”洋陆俯冲型造山带存在差异。

  • 3.4 构造转换界面与充填序列存在时空性差异

  • 地层接触关系与上覆地层的充填序列特征是揭示造山作用性质的重要指标。与典型的“加里东”造山发育磨拉石与区域性角度不整合不同,华南泥盆系与前泥盆系不同期次地层之间的接触关系存在显著的区域性差异,表现为:除云南弥勒—曲靖、钦防海槽等地泥盆系与下志留系呈整合接触外,华夏区泥盆系呈角度不整合覆盖在下伏地层(前寒武系—志留系)之上,而扬子区泥盆系主要呈平行不整合覆盖在志留系之上,并在空间上呈现一种由南东向北西逐渐变新、层位渐次升高的规律(图7、8)。这一种时空差异的表现形式主要以雪峰山—九岭山为界线:界线以东、以南直至东南沿海,泥盆系的碎屑岩地层主要以高角度不整合覆盖于前寒武系至志留系不同层位的地层之上,局部地区泥盆系底部可见底砾岩;界线周缘附近泥盆系以小角度不整合渐变为微角度不整合或平行不整合覆盖于寒武系—志留系之上;而界线以西、以北,泥盆系则平行不整合覆盖于志留系之上。

  • 志留纪晚期—泥盆纪,华南古地理演化进入了造山带被剥蚀夷平、逐步海侵以及盆地填充的准平原化过程(丘元禧和梁新权,2006杜远生和徐亚军,2012戎嘉余等,2019),但沉积充填序列也存在着明显的区域性差异,发生的时间和进程各不相同。根据对不整合面之上沉积充填序列、生物地层、古生物和群落古生态等特征研究发现,华南泥盆纪早期表现为南部“由南往北”与北部“西北往东南”的同步海侵过程(图9),这与加里东期构造运动造成的早—晚古生代转换时期不整合关系类型、挤压方向具有耦合性(李三忠等,2016;王怿等,2021),反映了“非典型”造山形成的隆-坳的古地理格局的差异。海侵自早泥盆世中期在华南西南地区广泛发生,在中泥盆世中晚期以后构成北西向深水盆地分割碳酸盐台地。然而,驱动华南泥盆纪海侵的机制以及自早泥盆世早期至晚泥盆世早期的海侵具体期次,海侵范围仍需要大量工作去验证和完善。

  • 4 待解决的关键科学问题

  • 4.1 下伏地层的褶皱变形样式——华南的加里东期“非典型”造山的动力方向

  • 华南大陆以雪峰山—九岭山一线为界,泥盆系与前泥盆系接触关系自东向西表现为高角度不整合、低/微角度不整合向平行不整合的过渡。不整合面之下前泥盆系的褶皱变形在排除掉后期变形之后(例如剔除不整合面之上地层的变形),能够反映其在加里东期形成时所受的构造应力方向以及不同区域构造应力的变化规律。结合前人的研究成果,本章节将华南大陆细分为不同的构造区域,针对不整合面上下地层褶皱变形情况进行概略描述和分析,进而可有助于大致了解不整合面之下地层加里东期相关的变形样式。具体分区如下,将扬子地块分为:扬子区东南缘构造带(隔槽式褶皱带)、扬子北缘(南秦岭-大别山)构造带、龙门山构造带和江南雪峰构造带(张国伟等,2013),将华夏地块划分为云开山、南岭和武夷山区(李三忠等,2016)。

  • 图6 华南中晚奥陶世—中晚志留世岩相古地理图(修改自马永生等,2009

  • Fig.6 Geographical map of South China during Middle-Late Ordovician to Middle-Late Silurian (modified after Ma Yongsheng et al., 2009)

  • (1)扬子区东南缘。扬子区东南缘,江南雪峰构造带以西的区域,以大型隔槽式褶皱(千米尺度)这类典型的薄皮构造为特征。该区域内前泥盆系与上覆地层(如二叠系)主要表现为平行不整合接触关系。在湖南张家界以南的武陵山地区、石门—桑植地区和贵州桐梓地区,均可见大量以前泥盆系(主要为志留系,少部分为奥陶系和寒武系)为核部的隔槽式背斜(如图10a),而在向斜部分,不整合面之上的地层倾角较陡,最高可达70°~90°,同时,这些地层几乎未经历变质作用(Chu Yang et al.,2012)。隔槽式褶皱轴迹整体上以NE-SW向为主,并呈现出向NW凸出的展布特征。在部分区域还可见由多个隔槽式褶皱组合形成更大规模的复式背斜(杨俊等,2021)。关于该区域内隔槽式褶皱形成的时代目前仍有争议(Chu Yang et al.,2012; Chu Yang and Lin Wei,2018杨俊等,2021),如若该区域内的隔槽式褶皱在加里东期既开始形成,则通过其几何学特征可判断该区域在加里东期所受最大主应力方向为NW-SE向。

  • 图7 华南泥盆系—前泥盆系界面类型分布图(修改自王怿等,2021

  • Fig.7 Distribution of stratigraphic interface types between Devonian and Pre-Devonian in South China (modified after Wang Yi et al., 2021)

  • (2)扬子区北缘。扬子区北缘,秦岭-大别山造山带南侧的区域,被认为是一种复合前陆变形构造带(张国伟等,2013)。该区域内前泥盆系与泥盆系主要表现为平行不整合接触关系。在变形作用方面,前泥盆系与泥盆系也展现出一致性,即表现为轴迹呈SEE-NWW向,轴面向NNE倾斜的较为紧闭的褶皱,因此推断其主要变形受加里东期之后的构造运动所控制。前人研究认为扬子区北缘在加里东末期,由于华北地块和扬子地块发生不同方向的旋转,使该区域进入伸展构造背景,形成了一系列盆-岛构造、拆离断层、同生断裂等构造,并认为其中形成的断层(同沉积断层或者走滑断层)控制着泥盆纪相关盆地的发育(方维萱等,2001)。在实际野外工作中,如在陕西西乡地区,可见中泥盆统韩城沟组(D2h)大理岩与下伏的下志留统(S1)砂岩呈现平行不整合接触关系,并发生相同的构造变形。仅通过这一观察结果不能确定在泥盆系沉积时,该区域是否受到同沉积断层或者是走滑拉分的控制。因此该地区受加里东构造运动的影响还需进一步探究。

  • (3)龙门山构造带。龙门山构造带位于扬子区西缘,松潘-甘孜地体以东,是由扬子地块西缘断裂褶皱系统和松潘-甘孜地体东缘逆冲推覆系统所组成的复杂构造带(陈虹等,2011)。该区域内前泥盆系与泥盆系主要表现为整合或者平行不整合接触关系(如图8d、e)。在变质变形作用方面,该区域内前泥盆系与泥盆系也展现出一致性,即表现为密集发育倾向NW或者SE的高角度劈理的千枚岩或者片岩,可推测其宏观上存在轴迹呈NE-SW向,轴面向NW或者SE倾斜的紧闭褶皱。根据前泥盆系与泥盆系变质变形的一致性可推断其主要变形受加里东期之后的构造运动所控制。前人研究认为扬子地块西缘在晚震旦世-早古生代总体表现为被动大陆边缘裂陷构造(王剑,2000),加里东运动在龙门山地区仅表现为不均一的振荡式上升运动,仅在局部地区造成沉积间断,但未改变区域整体的构造格局。在实际野外工作中,如在四川平武地区可见泥盆系危关群(Dwg)泥岩和下伏志留系茂县群(S2-3mx)泥岩整合接触,发育相同的倾向SE高角度劈理,且具有相似的变质程度(图10b)。根据这一观察结果可以认为,加里东构造运动在龙门山构造带影响有限,与前人结论一致。

  • 图8 华南泥盆系与下伏地层接触关系

  • Fig.8 Contact relationship between Devonian strata and underlying strata in South China

  • (a)—云南东川志留系菜地湾组与泥盆系翠峰山群呈平行不整合接触;(b)—云南大关志留系菜地湾组与泥盆系翠峰山群呈平行不整合接触;(c)—贵州独山志留系翁项组与泥盆系丹林组呈平行不整合接触;(d)—云南曲靖志留系玉龙寺组与泥盆系西山村组呈整合接触;(e)—广西荔浦寒武系水口群与泥盆系莲花山组呈角度不整合接触;(f)—广西贵港寒武系黄洞口组与泥盆系莲花山组呈角度不整合接触;(g)—广西兴安奥陶系田林口组与泥盆系莲花山组呈角度不整合接触;(h)—广东连州寒武系水石组与泥盆系老虎头组呈角度不整合接触

  • (a) —the Silurian Caidiwan Formation and the Devonian Cuifengshan Group in Dongchuan, Yunnan, are in parallel unconformity contact; (b) —the Silurian Caidiwan Formation in Daguan, Yunnan, is in parallel unconformity contact with the Devonian Cuifengshan Group; (c) —the Silurian Wengxiang Formation and the Devonian Danlin Formation in Dushan, Guizhou, are in parallel unconformity contact; (d) —the Silurian Yulongsi Formation in Qujing, Yunnan, is in conformable contact with the Devonian Xishancun Formation; (e) —the Cambrian Shuikou Group in Lipu, Guangxi, is in angular unconformity contact with the Devonian Lianhuashan Formation; (f) —the Cambrian Huangdongkou Formation and the Devonian Lianhuashan Formation in Guigang, Guangxi, are in angular unconformity contact; (g) —the Ordovician Tianlinkou Formation and the Devonian Lianhuashan Formation in Xing'an, Guangxi are in angular unconformity contact; (h) —the Cambrian Shuishi Formation and Devonian Laohutou Formation in Lianzhou, Guangdong are in angular unconformity contact

  • 图9 华南泥盆系分区图(修改自曾允孚,1993

  • Fig.9 Stratigraphic zoning map of the Devonian system in South China (modified after Zeng Yunfu, 1993)

  • (4)江南雪峰构造带。江南雪峰构造带位于鹤峰-隆山-印江断裂带以东,江绍-萍乡-钦防断裂以西(图7),其主体是NE-SW走向的一个前寒武纪岩石出露完整的构造单元。该构造带内,大致以紫云-罗甸断裂一线为界,界线以北为江南雪峰构造带主体部分,界线以南为南盘江-右江构造带。在北部江南雪峰构造带主体部分区域内,泥盆系和前泥盆系主要表现为不整合接触关系(Chu Yang and Lin Wei,2018),其中前泥盆系发育有大量轴迹为NE-SW向的近直立紧闭褶皱,而泥盆系通常发育为轴迹大致为NE-SW向的宽缓或开阔褶皱。在实际野外工作中发现,该区域内前泥盆系,如在湖南道县地区上奥陶统(O3)砂岩和大瑶山地区的中寒武统黄洞口组(Є2h)砂岩地层均变形为直立紧闭褶皱(图10c、d)。而泥盆系,如出露于大瑶山地区的下泥盆统莲花山组(D1l)石英砂岩,几乎未变形,与下伏的寒武系呈角度不整合接触关系。这些观察结果说明该区前泥盆系受到加里东构造运动的影响而发生了构造变形。在南部南盘江-右江构造带区域内,泥盆系与下伏前泥盆系呈现为角度不整合接触关系。该区域内前泥盆系主要发育轴迹为E-W向近直立的紧闭褶皱,而泥盆系变形主要为轴迹大致为E-W向的宽缓褶皱(郝义等,2010)。前人研究认为该区域内的前泥盆系构造变形可能是云开地块在晚寒武世—早奥陶世由南向北的推覆挤压的结果(杜远生和徐亚军,2012)。在实际野外工作中,在东大明山地区观察到了中寒武统黄洞口组(Є2h)发育的近直立褶皱(如图10e),其轴迹走向为E-W向。而其上覆泥盆系变形为穹窿状宽缓褶皱,翼部倾角较缓,两者呈现明显角度不整合接触,表明在这一构造区域内寒武系构造变形同样主要受加里东期构造运动控制。

  • 图10 华南前泥盆系变形现象

  • Fig.10 Deformations of pre-Devonian strata in South China

  • (a)—贵州桐梓中奥陶统宝塔组(O2b)箱状褶皱;(b)—四川丹巴泥盆系危关群(Dwg)和志留系茂县群(S2-3mx)整合接触及变形;(c)—湖南道县上奥陶统(O3)褶皱;(d)—广西大瑶山中寒武统黄洞口组(Є2h)紧闭褶皱;(e)—广西六景中寒武统黄洞口组(Є2h)褶皱;(f)—广东阳山上寒武统水石组(Є3s)斜卧褶皱

  • (a) —box folds of the Middle Ordovician Baota Formation (O2b) in Tongzi, Guizhou; (b) —conformable contact and deformation of the Devonian Weiguan Group (Dwg) and Silurian Maoxian Group (S2-3mx) in Danba, Sichuan; (c) —Upper Ordovician (O3) folds in Daoxian, Hunan; (d) —tight folds of the Middle Cambrian Huangdongkou Formation (Є2h) in Dayaoshan, Guangxi; (e) —Middle Cambrian Huangdongkou Formation (Є2h) folds in Liujing, Guangxi; (f) —oblique reclined folds of the Upper Cambrian Shuishi Formation (Є3s) in Yangshan, Guangdong

  • (5)云开地区。云开地区是位于华夏区内钦防断裂以东和四会-吴川断裂以西的区域(图7)。该区域内,泥盆系与下伏前泥盆系呈现角度不整合接触关系。该地区内前泥盆系受到了不同程度的构造变形作用,多发育紧闭褶皱、不对称褶皱、平卧褶皱等(丘元禧和梁新权,2006舒良树等,2008),褶皱轴向不稳定,以E-W和NE-SW向为主,并伴随着强烈的逆冲推覆和韧性剪切作用(舒良树,2012)。而出露在云开地区的泥盆系,如莲花山组(D1l)、信都组(D2x)等,呈零散分布,大部分以20°~40°的倾角倾斜,与下伏的前泥盆系呈明显角度不整合关系。这一现象表明云开区地区前泥盆系变形明显受加里东期构造运动的影响。

  • (6)南岭地区。南岭地区是位于华夏区内江山-绍兴断裂南段以东,河源-广丰断裂西南段以北的区域(图7)。该地区的泥盆系与下伏前泥盆系也呈现角度不整合接触关系。如在赣中南地区,形成了一个以震旦系为核部的大型复背斜,两翼为下古生界褶皱岩层,其褶皱轴近E-W向,而上覆泥盆系未被卷入褶皱变形,与前泥盆系呈不整合接触关系(舒良树,2006)。在野外实际工作中,广东阳山剖面的上寒武统水石组(Є3s)中观察到了发育在砂岩中的斜卧褶皱,褶皱轴向为NE-SW(图10 f)。而其上覆泥盆系倾角相对较低,与下伏前泥盆系呈现不整合接触关系。这一现象同样说明该区域内前泥盆系变形明显受到加里东期构造运动的控制。

  • (7)武夷山地区。武夷山地区是位于华夏区内四会-吴川断裂以东,政和-大浦断裂北东段以西的区域(图7)。该区域内,上泥盆统与下伏前泥盆系(奥陶系、寒武系)也呈现角度不整合接触(舒良树等,2008)。在该地区内,前泥盆系褶皱和断裂均十分发育,主要构造线为NE-SW向(徐先兵,2011),褶皱类型常见有紧闭褶皱、倒转褶皱等,前人计算部分区域地层最大缩短率可达67%(舒良树等,2008)。这些褶皱的形成多与区域内逆冲或者走滑韧性剪切作用有关。然而,该地区泥盆系,如莲花山组(D1l)、跳马涧组(D1t)等,与下伏的奥陶系、寒武系明显呈现角度不整合接触关系,说明加里东构造运动对该地区前泥盆系变形有明显影响。

  • 综上所述,华南大陆前泥盆系与加里东期相关变形主要表现为轴迹近NE-SW向和近E-W向的不同形态褶皱,其中轴迹近NE-SW向褶皱主要沿江南雪峰构造带主体部分分布,而轴迹近E-W向褶皱主要分布在华南大陆南部区域。若想要恢复各区域内前泥盆系褶皱变形在加里东期构造运动刚结束时的准确形态,还需借助精确的测量手段对不整合面上下的地层变形进行定量研究,进而可排除之后印支期、燕山期等构造运动的影响。在此基础上可进一步确定地层当时变形所受构造应力的方向以及不同区域构造应力的变化规律,从而探讨该时期华南加里东“非典型”造山作用的动力学机制。

  • 4.2 华南早古生代“非典型”造山过程中与其他板块之间的位置关系——华南的加里东期“非典型”造山的来源

  • “早—晚古生代转换时期华南板块与东冈瓦纳大陆的古地理关系”直接影响对其动力学过程的解释。不同学者基于对古地磁学、古生物学、岩浆岩岩石学、沉积大地构造学、变质岩岩石学等数据的解释,提出了五种不同的古地理重建模型(440~410 Ma)(图11):模型I:根据气候敏感沉积物(如蒸发岩和钙质壳)的古地理分布,将华南板块置于赤道上,其西南缘与澳大利亚板块单独连接(Boucot et al.,2013; Scotese,2021)。模型II:基于现有的古地磁数据,把华南板块置于赤道上,其东南缘与澳大利亚板块单独连接(Yang Zhenyu et al.,2004; 李三忠等,2016; Huang Baochun et al.,2018; Merdith et al.,2021)。模型III:基于对碎屑岩磁倾角(假设压实系数f=0.6)笼统校正后的古地磁数据,把华南板块置于~15°N,其东南缘与澳大利亚单独连接(Torsvik and Cocks,2016)。模型IV:基于物源分析,将位于0~5°S的华南板块东南缘与澳大利亚板块和印度板块相连接(Xu Yajun et al.,2014; Wang Lijun et al.,2021; Cawood et al.,2021)。模型V:基于沉积物源再循环的可能性认为华南板块位于赤道上并已经与冈瓦纳大陆裂离(Liu Huichuan et al.,2018; Zhao Guochun et al.,2018)。

  • “早—晚古生代转换时期“华南板块的古纬度和古方位是什么”,“华南板块与哪些地块具有亲缘关系”,这两个问题对于理解华南“非典型”造山的地质过程具有重要意义,因此,确定华南板块在志留纪晚期—早泥盆世时期的古纬度和古方位非常关键。部分学者通过对华南地区古生物化石(如造礁珊瑚、腕足类、层孔虫和牙形石)、风暴沉积(张哲等,2007; 陈世悦等,2010)、气候敏感性沉积物(Boucot et al.,2013)的半定量分析,认为华南志留纪晚期—早泥盆世位于赤道附近,但仍需进一步精确限定华南板块的古地理位置(在赤道附近多少纬度,南纬还是北纬?)。构造古地磁学是定量约束板块古纬度和古方位的最有效工具,然而目前华南板块志留纪晚期—早泥盆世时期高质量古地磁数据较少(Opdyke et al.,1987; Huang Kainian et al.,2000; 张世红等,2001)。更重要的是,目前已有的数据还存在采样地层岩石单元时代不精确(如Huang Kainian et al.,2000)、样品数量不足(样品数小于25;如张世红等,2001)、缺乏可靠的野外检验(如褶皱检验、倒转检验等;Opdyke et al.,1987)等问题,严重阻碍了对华南古地理位置演化的认识,因此,亟需可靠、有效的古地磁数据来约束华南的古地理位置以讨论与其他板块的关系。除此之外,由于古地磁无法确定古经度,对于华南板块与周缘地块的连接关系只有通过碎屑物源分析、构造带(造山带或大陆裂谷)极性、生物区系、岩浆岩带特征等手段约束。然而,华南板块缺乏早古生代火山岩证据,仅有S型花岗岩报道,且未有明确的高压变质作用证据(见上文),造成很难通过构造带-岩浆岩带等手段确定其与周缘地块的连接关系。且华南在早泥盆世发育有东冈瓦纳植物群(如石松类、蕨类),从生物区系上也无法厘清其与东冈瓦纳大陆中各地块的连接关系(Xue Jinzhuang,2011; 薛进庄,2014)。通过对前人已发表华南早古生代—泥盆纪碎屑锆石U-Pb年龄数据的统计结果可知(图12),尽管下泥盆统锆石年龄谱与志留系、中—上泥盆统碎屑锆石具有相似的年龄峰值区间,但明显不同的是出现了更多的前寒武纪格林威尔期(1300~900 Ma)和泛非期(750~500 Ma)锆石,以及较弱的450~420 Ma年轻峰值年龄信息(图12),说明志留纪—泥盆纪华南可能存在相似的物源区,可以肯定的是,早古生代至泥盆纪,包括华南板块在内的东冈瓦纳北部微地块均位于印度-澳大利亚板块的北缘(Wang Lijun et al.,2021),但华南在志留纪—泥盆纪接收的外部物源是来自南部的澳大利亚板块(图11,模式Ⅰ、Ⅱ、Ⅲ)还是来自西南部印度板块与东南部澳大利亚板块两个方向的供应(图11,模式Ⅳ),即华南与各板块之间的亲缘性仍存在争议(Xiang Lei and Shu Liangshu,2010; Duan Liang et al.,20112012; Yao Jinlong et al.,2012; Xia Xiaoping et al.,2016; Chen Qiong et al.,20162018; Xu Yajun et al.,2017; Zhang Xinchang et al.,2018; Li Chao et al.,2020; Shen Linwei et al.,2021; 冯洋洋等,2021)。另外,碎屑锆石年谱出现不同也说明了不同物源的贡献程度存在较为显著的差异,450~420 Ma的碎屑锆石在志留系、中—上泥盆统中作为主要峰值,时间跨度上与华夏地块东部强烈的花岗质岩浆活动时限一致(460~410 Ma),而在下泥盆统中占比较少。这一特征表明在泥盆纪早期,盆地内部出现地理屏障使这些岩体没有出露地表形成显著的物源贡献。然而,前人未对志留纪—泥盆纪出现这种物源贡献程度差异的原因作深入探讨,其是否与加里东期造山运动造成的褶皱形态变化,或与古特提斯洋分支-哀牢山洋盆的打开相关,仍然存在不确定性。

  • 图11 早—晚古生代转换时期东华南在冈瓦纳大陆中的重建模式图

  • Fig.11 Reconstruction model of East South China in Gondwana continent during the early to Late Paleozoic transition

  • 模式Ⅰ修改自Scotese,2021; 模式Ⅱ修改自Yang Zhenyu et al.,2004; 李三忠,2016; Huang Baochun et al.,2018; Merdith et al.,2021; 模式Ⅲ修改自Torsvik and Cocks,2016; 模式Ⅳ修改自Xu Yajun et al.,2014; Cawood et al.,2021; Wang Lijun et al.,2021; 模式Ⅴ修改自Zhao Guochun et al.,2018; 400~385 Ma重建模式修改自Xian Hanbiao et al.,2019

  • Mode I is modified from Scotese, 2021; Mode Ⅱ is modified fromYang Zhenyu et al., 2004; Li Sanzhong, 2016; Huang et al., 2018; Merdith et al., 2021; Mode Ⅲ is modified from Torsvik and Cocks, 2016; Mode Ⅳ is modified from Xu Yajun et al., 2014; Cawood et al., 2021; Wang Lijun et al., 2021; Mode Ⅴ is modified from Zhao Guochun et al., 2018; 400~385 Ma rebuild mode modified from Xian Hanbiao et al., 2019

  • 4.3 华南的加里东期“非典型”造山作用类型和地球动力学过程

  • 目前地质学家们对于华南的加里东期“非典型”造山的肇因及其板块动力学机制尚未达成共识,主要的观点包括:① 华南内部俯冲-碰撞/斜向碰撞-走滑造山模式:认为华夏与扬子地块之间的华南洋持续俯冲至早古生代,伴随着扬子与华夏地块之间的俯冲-碰撞/斜向碰撞-走滑(图13a;Hsü et al.,1990; 殷鸿福等,1999; 尹福光等,2001; Peng Songbai et al.,2012; 潘桂棠等,2016; 覃小锋等,2017; Liu Huichuan et al.,2018; 张克信等,2018; Wang Lijun et al.,202120232024; Li Longming et al.,2022)或西华夏地块与其东部一未知地块之间的陆陆碰撞(Lin Shoufa et al.,2024),并在靠近拼合带的俯冲板块上发展为周缘前陆盆地系统;② 板内造山模式:依据华夏与江南地区普遍缺乏早古生代蛇绿岩等洋壳俯冲记录与典型的高压—超高压变质岩,且从华夏地块到扬子地块为连续的沉积记录,提出华夏地块内部早古生代造山过程为板内构造体制,是冈瓦纳大陆最终聚合增生造山的构造应力引起的远程传播效应形成的陆内造山,而华南内部表现为陆内前陆盆地(图13b;Wang Yuejun et al.,20102011; 张国伟等,2013; Xu Yajun et al.,2014; Shu Liangshu et al.,2015; 李三忠等,2016; Shu Liangshu et al.,2021);③ 华南与东冈瓦纳俯冲-碰撞造山模式:认为华南板块与北羌塘地块、印支地块、华北地块组成陆块群(Asian Hun superterrane),随着原特提斯洋的关闭与冈瓦纳北缘发生碰撞,从而引起华南内部的变质变形作用(图13c;Zhao Tianyu et al.,2017);④ 洋-陆碰撞造山模式:提出华南板块东华夏大洋岩石圈受西华夏逆冲作用而发生洋-陆碰撞,形成早古生代造山带(图13d;Zhao Junhong et al.,2022),此时,扬子地区表现为弧后前陆盆地,而华夏区则表现为周缘前陆盆地。下文对上述模式进行详细介绍。

  • 图12 已发表华南寒武系—泥盆系碎屑锆石年龄谱及样品点位

  • Fig.12 The age spectrum and sample locations of Cambrian-Devonian detrital zircons from South China

  • 图13 华南加里东期造山模式图(a,修改自张克信等,2018; b,修改自Shu Liangshu et al.,2015; c,修改自Zhao Tianyu et al.,2017; d,修改自Zhao Junhong et al.,2022

  • Fig.13 Models of Caledonian orogenic in South China (a, modified after Zhang Kexin et al., 2018; b, modified after Shu Liangshu et al., 2015; c, modified after Zhao Tianyu et al., 2017; d, modified after Zhao Junhong et al., 2022)

  • (1)华南内部俯冲-碰撞造山模式。该模式的提出主要是基于对扬子和华夏地块之间华南洋盆消亡过程的不同认识。Hsü et al.(1990)较早认为华南洋盆于印支期关闭,自此华南拼合为完整板块,而下扬子和江南造山带地区发现的新元古代蛇绿混杂岩带(李献华等,1994; Shu Liangshu et al.,1996; 彭松柏等,2006)、华南东南部广泛发育的拉伸系S型花岗岩(约820 Ma,周怀玲和张振贤,1993; 薛怀民等,2010)以及赣北—浙北地区近40000 km2前震旦纪面型浅变质岩区(Wang Dezi et al.,1989; 周怀玲等,1993),均指示着华南洋盆于晋宁期开始收缩,扬子地块和华夏地块在北段沿江山-绍兴断裂带拼合,但其中段、南段仍存在一残余洋盆(殷鸿福等,1999)。根据扬子地块与华夏地块地层之间巨大的差异推断,该残余洋盆直到志留纪才消亡(潘桂堂等,2016)。因此,华南加里东期造山带是扬子地块、华夏地块由北向南沿华南洋多期次幕式拼合的产物。近年来Lin Shoufa et al.(2024)通过对比华南与阿巴拉契亚地区造山特征将华夏地块沿一条左旋走滑断层(闽西北断裂)划分为西华夏地块和东华夏地块。其中,西华夏地块(怀玉地体)与扬子地块(九岭地体)在晋宁期沿着赣东北造山带拼合在一起,而华南加里东期造山运动则是西华夏地块与其东缘另一尚未明确识别的地体(terrane PT)俯冲-碰撞造山的结果。值得注意的是,该地块在碰撞后随即发生裂离,至中生代东华夏才通过走滑运动平移至西华夏地块东侧。随后,Wang Lijun et al.(2022,2023)基于对现有古地磁、古生物、地层学及碎屑锆石数据的综合分析和重新评估又提出,扬子与西华夏在早古生代之前分别位于冈瓦纳大陆北缘的两个不同位置,受到澳大利亚板块与印度板块之间的Kuunga洋关闭(560~480 Ma)的影响,扬子地块于奥陶纪迁移至西华夏附近,之后在志留纪再通过斜向走滑的方式沿着江绍断裂带拼合在一起,二者之间的洋盆消失。尽管上述不同学者对扬子地块与华夏地块之间的关系以及华南洋的消亡过程仍存在不同的认识,但均认为华南加里东期造山运动是由于内部俯冲-碰撞形成,挑战了传统将华南视为在新元古代早期已拼合成单一完整地块并位于冈瓦纳大陆内部的观点。然而,该模式并未能对华南不存在早古生代蛇绿岩、弧火山岩、幔源岩浆岩等指示俯冲碰撞的标志产物,区域内面状分布的S型花岗岩缺乏线状花岗岩及早古生代沉积记录指示的被动大陆边缘环境等现象进行合理的解释。

  • (2)板内造山模式。该模式认为早古生代时期华南洋盆并不存在,扬子和华夏地块在新元古代就已拼合。相关证据包括,华南晋宁期蛇绿岩的发现(李献华等,1994; Shu Liangshu et al.,1996; 彭松柏等,2006)、早古生代扬子和华夏地块之间连续的碎屑物源供给、古生态变化(Wang Yuejun et al.,2010; Yao Jinlong et al.,2012; Xu Yajun et al.,2014)以及华南大范围出露的加里东期S型花岗岩(周怀玲等,1993; 薛怀民等,2010),因此华南板块在早古生代作为一个完整的个体位于冈瓦纳大陆北缘,而华南加里东期造山运动则是受远程效应控制的陆内造山作用。那么,控制华南这次陆内造山的地球动力学机制又是什么?针对这一问题,先后出现了以下几种动力学模型。① 板内俯冲模型:Faure et al.(2009)根据独居石U-Pb年代学、云母40Ar-39Ar年代学以及赣南地区加里东期构造变形研究提出,晚奥陶世时期(约460~444 Ma)华夏地块开始沿着江山-绍兴断裂带向扬子地块下部俯冲并延续至早泥盆世;② 板内仰冲模型:Li Xianhua et al.(1997,2003,2005)通过对陈蔡-武夷山地区花岗片麻岩中锆石(U-Pb)、云母、角闪石(40Ar-39Ar)进行年代学分析结合沉积盆地记录以及岩石地球化学研究,认为中奥陶世至志留纪末期华夏地块向北西仰冲并覆盖在扬子地块东南缘的新元古代盆地沉积物之上,盆地也由此经历了由裂谷盆地到前陆盆地的转变。与此同时,逆冲过程中产生的热能加上该地区中新元古代镁铁质岩浆底侵可能残留的热量,导致埋藏的沉积物与华夏基底岩石发生部分熔融,导致了造山运动末期陈蔡—武夷山地区的大规模岩浆侵入作用以及区域变质作用(片麻岩化);③ 陆内俯冲导致南华裂谷盆地准对称反转模型:舒良树等(2006)、Shu Liangshu et al.(2014,2015)通过对江南造山带以及华夏地块早古生代地层序列、变形特征和岩浆岩进行的地质学、地球化学与地质年代学的系统研究,提出在早古生代早期华南板块与东海之间可能存在一个已经消失了的“南海古陆”,奥陶纪晚期 “南海古陆”向华夏东地块南缘下部消减,同时扬子地块也向华夏地块西北缘消减,强烈的区域挤压作用导致原本发育在华夏地块两侧的正断层结构发生反转,而华夏地块内部区域(武夷山—云开山等地)则沿着这些断层仰冲,形成了区域内440~400 Ma的面状S型花岗岩;④ 板缘碰撞-陆内挤压造山模型:Xu Yajun et al.(2014,2016)根据海南岛和三亚地块的碎屑锆石物源分析认为华南板块早古生代造山运动主要分为两幕进行,第一幕为寒武纪—奥陶纪之交响应东冈瓦纳大陆沿Kuunga造山带最终闭合的郁南运动,第二幕为志留纪—泥盆纪之交澳大利亚板块东缘汇聚板块边缘的增生造山作用的构造应力持续向东冈瓦纳大陆内部传播,志留纪在华夏地块弱流变基底区域汇聚,导致华夏地区的构造反转、隆升,从而引起具有陆内挤压特点的广西运动。以上模式的提出,很好地解释了华南古生态变化、岩浆作用、构造变形、沉积物源等地质现象,但其中“消失的南海陆块”、印度与华夏地块碰撞与华夏褶皱变形之间巨大的时间间隔,以及三亚地块是否能作为整个华南加里东期造山运动的诱因等问题还需要进一步的研究。

  • (3)华南与东冈瓦纳俯冲-碰撞造山模式。Zhao Tianyu et al.(2017)对云南地区(思茅地块和保山地块)新元古代沉积物(澜沧组)中碎屑锆石进行U-Pb-Hf同位素研究发现,这些沉积物的最大沉积年龄为奥陶纪而非早先认为的新元古代,并结合碎屑锆石年龄对比以及澜沧组地层东部发现的早古生代蛇绿岩套,认为在早古生代之前澜沧地块与保山地块一起位于东冈瓦纳北缘,直到志留纪—泥盆纪,随着原特提斯洋关闭(澜沧地块与思茅地块之间)以及古特提斯洋的打开(澜沧地块与保山地块之间),才与思茅地块联系到一起。而华南板块在此过程中则是与北羌塘、印支、华北地块组成一个陆块群(Asian Hun superterrane),随着原特提斯洋的关闭,在约460~400 Ma左右与冈瓦纳大陆北缘发生碰撞,从而造成了羌塘中部、华南以及塔里木地块该时期大规模的区域变质作用。该模式以华南外部的思茅、保山地块为研究对象,很好地解释了在全球板块背景下华南板块、北羌塘、印支、华北地块古生代碎屑锆石数据之间的相似性,为研究华南加里东期“非典型”造山的性质与动力学机制提供了新的视角,但难以解释包含华南在内的亚洲陆块群新元古代—早古生代沉积记录以及碎屑锆石与冈瓦纳大陆北缘(印度板块以及澳大利亚板块等)的亲缘性。

  • (4)洋-陆碰撞造山模式。这一模式是由Zhao Junhong et al.(2022)通过对政合-大埔断裂两侧地质学、地球化学和地球物理证据结合数值模拟结果提出。在该模型中,在早古生代期间东华夏地块(政合-大埔断裂东侧)仍具有洋壳,受冈瓦纳大陆聚合的影响,西华夏地块大陆岩石圈地幔先向东俯冲至东华夏大洋岩石圈地幔之下,同时西华夏地块大陆地壳增生并逆冲于东华夏大洋板块之上(Huang Baochun et al.,2018; Zhao Junhong et al.,2022)。随后,大陆岩石圈地幔和大洋岩石圈地幔在深部发生碰撞,导致浮力较大的洋壳与俯冲的大洋岩石圈地幔分离,从而在大陆地壳下方堆叠起来,形成较厚的造山根(Kissling and Schlunegger,2018; Zhao Junhong et al.,2022),也由此造成了西华夏地块上部地壳的强烈变形以及不同程度的变质。随着碰撞的进一步发展,造山带自大洋-大陆边界逐渐往内陆迁移,延伸了约300 km(Zhao Junhong et al.,2022),最后引起了西华夏以及江南雪峰地区的陆内造山,形成了现今观察到的华南加里东期造山带(图13)。该模式很好地解释了西华夏地块前泥盆纪地层经历的强烈的变形和绿片岩相至角闪岩相变质作用、政合-大埔断裂带两侧截然不同的岩石圈结构、下方残余的俯冲板块(Xu Shan et al.,2019; Zhang Xiaole et al.,2020; Cai Huiteng et al.,2020)以及附近新发现的一套约520 Ma的洋中脊型蛇绿岩套(Li Longming et al.,2022)等现象,并解决了西华夏地块缺少俯冲记录的弧岩浆岩、高温高压变质记录等问题。然而该模式是基于数值模拟结果初次提出,且并未在世界范围内有见过类似的洋-陆碰撞的先例,还需要更多的证据或案例来进一步佐证该观点。

  • 5 结语

  • 综上,华南早—晚古生代转换时期的“非典型”造山运动形成了华南泥盆系与下伏地层之间不整合面上、下截然不同的岩浆、沉积、构造特征,而其作用类型和地球动力学过程仍存在较多观点与争议。前人的研究多以不整合面之下的早古生代地层或岩体为研究对象,利用不同特征的地化数据对其大地构造属性和构造演化进行解释。然而,从沉积学角度进行深入研究的综合分析相对较少,对“非典型”造山背景下古地理格局如何转换的问题仍不明确,针对华南“非典型”造山特征的很多关键节点不清,例如,不整合界面下伏地层变形程度和方向的空间差异、上覆地层充填结构及体系的时空差异、不整合前后沉积盆地性质、古地貌、古地理格局是如何转换等问题,制约了对早—晚古生代转换时期的“非典型”造山过程中沉积响应的准确认识。

  • 通过对不整合面上下地层的变形定量研究,恢复下伏地层加里东期的变形样式,进而可确定当时的构造应力方向以及不同区域构造应力的变化规律。而对不整合面之上沉积盆地初始沉积的形态及展布、沉积充填序列演化、沉积与剥蚀地貌分析,能够反映华南志留纪晚期盆地性质,以及加里东期“非典型”造山如何对隆-坳格局的古地貌进行改造、定型。进一步结合对泥盆纪地层物源区分布和供给量分析、以及区域性岩相古地理分析,对比不整合前后的古地理转换,从而揭示“非典型”造山过程的沉积响应,探讨华南加里东期“非典型”造山作用的动力学机制。

  • 而随着古地理的发展,地球内部的动力学系统(岩石圈板块运动与地幔柱耦合作用)与超大陆旋回、古构造域的地理变迁的耦合关系越来越受到重视,并将地质时间轴也融入到古地理的重建当中,成为当前的古地理发展的趋势,即构造古地理重建。在未来进一步讨论“非典型”造山背景下华南板块尺度的沉积响应与全球尺度的构造古地理格局具有怎么样的耦合关系,即华南板块在早—晚古生代转换时期在特提斯构造域中与周缘板块的亲缘性、摆放位置以及方向的变化,如何影响不整合面上、下沉积盆地性质、古地貌、岩相古地理格局转换,可为探讨华南早古生代造山的地质过程提供重要依据,为理解全球不同“非典型”造山提供典型示例。

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