岩石学报  2019, Vol. 35 Issue (10): 3161-3188, doi: 10.18654/1000-0569/2019.10.13   PDF    
东天山古弧盆体系成矿规律与成矿模式
龙灵利1,2, 王京彬1,2, 王玉往1,2, 邓小华1,2, 毛启贵1,2, 孙燕1,2, 孙志远1,2, 张忠义3     
1. 北京矿产地质研究院, 北京 100012;
2. 有色金属矿山深部资源勘查工程技术研究中心, 北京 100012;
3. 有色金属矿产地质调查中心, 北京 100012
摘要: 东天山是中亚增生型造山带的重要组成部分,随古亚洲洋的形成、演化和消亡,发育了东天山古生代弧盆体系。基于前人对东天山古生代构造演化与成矿规律的大量研究,针对以往研究相对薄弱的早古生代构造演化与成矿,本文重点论述了以卡拉塔格矿集区为代表的早古生代构造-岩浆-成矿研究新进展,从而进一步探讨了东天山古弧盆体系古生代构造演化与成矿规律。本文将东天山古弧盆体系划分为大南湖-头苏泉成矿带和阿奇山-雅满苏成矿带,又将前者划分为卡拉塔格成矿亚带和小热泉子-土屋成矿亚带;总结出其成矿具有VMS成矿系统与斑岩成矿系统共存、多种矿化类型叠加的特征;区域共发育两次大规模成矿事件,且均与大规模火山-侵入岩浆活动有关,进而构建了东天山古弧盆体系区域成矿模式;并指出东天山古生代弧-盆多方向、多期次的转换是导致该体系内VMS-斑岩型矿床共存、叠加成矿发育的主因。
关键词: 东天山    弧盆体系    构造演化    成矿规律    区域成矿模式    
Metallogenic regularity and metallogenic model of the paleo arc-basin system in eastern Tianshan
LONG LingLi1,2, WANG JingBin1,2, WANG YuWang1,2, DENG XiaoHua1,2, MAO QiGui1,2, SUN Yan1,2, SUN ZhiYuan1,2, ZHANG ZhongYi3     
1. Beijing Institute of Geology for Mineral Resources, Beijing 100012;
2. Technic Research Center for Deep Resources Exploration in Non-ferrous Metal Mines, Beijing 100012, China;
3. China Non-Ferrous Metals Resource Geological Survey, Beijing 100012, China
Abstract: The eastern Tianshan is an important part of the accretionary Central Asian Orogenic Belt (CAOB), where the eastern Tianshan Paleozoic arc-basin system was developed during the formation, evolution and closure of the Paleo-Asian Ocean. Based on a large number of the predecessors' studies on Paleozoic tectonic evolution and metallogenic regularity of the eastern Tianshan, and aimed at the relatively weakness upon researches in the past about Early Paleozoic tectonic evolution and metallogenesis, this paper focuses on the new progress of the Early Paleozoic tectonic-magmatic-metallogenic studies in the Kalatage ore cluster area, and further discusses the Paleozoic tectonic evolution and metallogenic regularity of the paleo arc-basin system of eastern Tianshan. In this paper, the Paleozoic arc-basin system of the eastern Tianshan is divided into two metallogenic belts of Dananhu-Tousuquan and Aqishan-Yamansu, while the former is further divided into the Kalatage and the Xiaorequanzi-Tuwu metallogenic sub-belts. It is concluded that this paleo arc-basin system has coexistence of VMS and porphyry metallogenic stystems. Multiple types of superimposed mineralization are widely developed in these systems. Tectonically, two large-scale metallogenic events have been developed, and both of them are related to large-scale volcanic-intrusive magmatic activities. Finally, a regional metallogenic model of the paleo arc-basin system of the eastern Tianshan is constructed, in which we propose that the multi-directional and multi-stage transformation of Paleozoic arc and basin in the eastern Tianshan is the main reason for the coexistence of VMS-porphyry deposits and superimposed mineralization in this system.
Key words: Eastern Tianshan    Arc-basin system    Geodynamic evolution    Metallogenic regularity    Regional metallogenic model    

位于新疆东部小热泉子至甘肃与新疆交界处的东天山地区,是中亚增生型造山带的重要组成部分,其构造演化与夹持于北部的西伯利亚板块和南部塔里木板块之间的古亚洲洋形成、演化和消亡过程中伴随的多块体拼合、增生-俯冲、碰撞造山紧密相关(Şengör et al., 1993; Jahn et al., 2004; Xiao et al., 2004, 2013),并形成了东天山古生代弧盆体系(肖序常等, 1991, 1992秦克章等,2002Xiao et al., 2008徐学义等,2014),聚集了丰富的矿产资源,以产出铁矿(雅满苏、红云滩、天湖、磁海等)、金矿(康西、康古尔、马头滩、梧桐窝子南等)、铜镍矿(土墩、黄山东、香山、图拉尔根等)、铜矿(红海、土屋、延东、玉海等)为显著特征(刘德权等,1992何国琦等,1994姬金生等,1994秦克章等,2002王京彬等,2006王登红等,2006木合塔尔·扎日等,2010Mao et al., 2018韩春明等,2018),是我国重要的金属矿产基地。长期以来,该区备受国内外学者的关注,在东天山大地构造单元的划分及演化(姬金生等,1994马瑞士等,1997Xiao et al., 2004; 王京彬等,2006; Deng et al., 2018; 舍建忠等,2018)、成矿区带划分、成矿模式、成矿规律研究(薛春纪等,1995王京彬等,2006冯京等,2009木合塔尔·扎日等,2010徐仕琪等,2011韩春明等,2018)、成矿预测及找矿模型(姬金生等,1996刘光海等,2000吴春明和吕新彪,2012丁建华等,2016)等方面取得了大量的研究成果。但以往对该区的研究主要聚焦于晚古生代成岩、成矿及构造演化等方面;相对而言,由于东天山早古生代地质记录保存较少,有关该区早古生代构造演化、成矿特征、成矿规律等方面的研究较为薄弱。

本文旨在前人研究基础上,总结近年来以卡拉塔格矿集区为核心的早古生代成岩、成矿研究成果(毛启贵等,2010Deng et al., 2016, 2018; 李玮等,2016龙灵利等, 2016, 2017Mao et al., 2018; 陈磊等,2018李遥等,2018; Sun et al., 2019a),综合东天山地区古生代构造-岩浆-成矿等方面的新进展,进一步探讨东天山古弧盆体系构造演化及成矿规律,构建东天山古弧盆体系区域成矿模式。

1 构造分区及特征

东天山位于中亚造山带的南缘,地处西伯利亚、塔里木板块、华北板块和东欧板块交汇处(图 1a)。根据区内主要断裂、地层、岩浆岩等展布特征,沿康古尔韧性剪切带和阿奇克库都克断裂将其划分为两大构造单元,以康古尔剪切带为界,以北为大南湖-头苏泉岛弧带,以南为阿奇山-雅满苏岛弧带(图 1b)。

图 1 东天山构造格架(a, 据Yakubchuk,2004)与矿床分布图(b, 据王京彬等,2006Deng et al., 2018; 舍建忠等,2018) Fig. 1 Map of the tectonic framework (a, modified after Yakubchuk, 2004) and deposit distribution (b, modified after Wang et al., 2006; Deng et al., 2018; She et al., 2018) in the eastern Tianshan Mountains
1.1 大南湖-头苏泉岛弧带

该带位于吐哈盆地的南缘,康古尔韧性剪切带以北地区。沿大草滩断裂又将大南湖-头苏泉岛弧带划分为卡拉塔格亚带和小热泉子-土屋亚带(图 1b)。

1.1.1 卡拉塔格亚带

该亚带位于大草滩断裂以北地区,沿卡拉塔格-大草滩一带展布,以发育早古生代地层-岩浆岩为特征,以卡拉塔格地区为典型代表。区内主要发育地层为(图 2a):(1)中晚奥陶世荒草坡群大柳沟组海相中基性火山岩夹火山碎屑岩,其下部主要为玄武岩,上部为安山质火山岩。获得侵入其中的闪长玢岩锆石U-Pb年龄为443Ma和437Ma(龙灵利等,2016)、石英闪长岩锆石U-Pb年龄为453Ma(Sun et al., 2018),以及中酸性杂岩体锆石U-Pb年龄为427~453Ma(Du et al., 2018a; Zheng et al., 2018; Sun et al., 2019a)。(2)早志留世红柳峡组海相火山沉积岩,其下部为英安质角砾凝灰岩,与下伏奥陶系安山岩呈整合或断层接触,上部为条带状凝灰岩,顶部发育块状硫化物透镜体。获得条带状凝灰岩锆石U-Pb年龄为440Ma(Deng et al., 2018),赋存其中块状黄铜矿Re-Os年龄为434~436Ma(Deng et al., 2016)。(3)早志留世卡拉塔格组海陆过渡相-陆相长英质(以英安岩为主)火山岩及火山碎屑岩,与下伏红柳峡组呈断层或不整合接触。获得侵入其中的次流纹岩锆石U-Pb年龄为439Ma(龙灵利等,2017)以及穿插这套火山岩的脉状矿黄铜矿Re-Os年龄为430Ma(Deng et al., 2016)。(4)早泥盆世大南湖组海相火山-沉积岩,主要为一套海相火山碎屑岩、火山碎屑沉积岩夹中基性火山岩和碳酸盐岩建造,与下伏早志留世地层呈不整合接触。其底部发育一套底砾岩,其中可见早古生代地层组的砾石(图 3a-d)。碳酸盐岩中产出大量的珊瑚、腕足等化石(ParaspiriferMegakozlowskiellina minimaSyringaxon sp.),是早泥盆世的重要分子(新疆维吾尔自治区地质调查院,2003)。(5)中泥盆世康古尔塔格组磨拉石建造(图 3ef),与下伏泥盆统大南湖组呈不整合接触。该组中可见Psilophyton sp.、Psilophylites ungulatus DouBarsasia sibirica(Krysht) ZalPsilophylites sp.、Barrandeinaduslians(Krejci) stur等植物化石,其在早泥盆世至中泥盆世早期较发育(新疆维吾尔自治区地质调查院,2003),综合考虑,将其初步划定为中泥盆世(亦可能为晚泥盆世)。(6)晚石炭世脐山组陆相火山-沉积岩建造,与下伏地层呈不整合接触,底部以砂泥岩、砂砾岩、粉砂岩为主,夹炭质泥岩,且含大量植物化石;顶部发育一套陆相中酸性火山岩(图 3f, g)。本次研究获得该组上部流纹岩锆石U-Pb年龄为301.1±3.4Ma(表 1图 4)。(7)中二叠世卡拉岗组陆相火山-沉积岩建造,与下伏脐山组地层呈不整合接触,主要为玄武岩、安山岩、气孔-杏仁状安山玄武岩、安山质岩屑晶屑凝灰岩。其中发育近同期的基性-超基性杂岩体。(8)晚二叠世库莱组河湖相陆源碎屑沉积建造,以黄灰色岩屑砂岩夹粉砂岩、灰黄色砂砾岩、灰黑-黑褐色炭质泥岩夹灰岩、绿灰色岩屑砂岩为主。

① 新疆维吾尔自治区地质调查院. 2003. 1:25万五堡幅(K46C00 2002)地质图及区域地质调査报告

图 2 东天山古生代典型地区综合地层柱 (a)卡拉塔格矿集区;(b)小热泉子-土屋构造亚带;(c)阿奇山-雅满苏构造带.图中年代学数据来源与文中相同 Fig. 2 Paleozoic comprehensive stratigraphic column in typical area of eastern Tianshan (a) Kalatage ore cluster area; (b) Xiaorequanzi-tuwu tectonic sub-zone; (c) Aqishan-Yamansu tectonic zone. The geochronological data sources in the graph are the same as those in the paper

图 3 东天山卡拉塔格地区地层照片 Fig. 3 Photos of litho-stratigraphies from the Kalatage district in eastern Tianshan

表 1 东天山卡拉塔格流纹岩和银帮山凝灰岩SHRIMP锆石U-Pb同位素分析结果 Table 1 SHRIMP zircon U-Pb analysis of the rhyolite from the Kalatage ore cluster area and tuff from the Yinbangshan in eastern Tianshan

图 4 东天山卡拉塔格流纹岩锆石U-Pb年龄谐和图(a)和加权平均年龄图(b) Fig. 4 Diagrams of U-Pb concordia age (a) and weighted average age (b) for zircons of rhyolite from Kalatage district in eastern Tianshan

该带内发育奥陶-泥盆纪中酸性杂岩体(花岗闪长岩、花岗斑岩、花岗岩、石英闪长岩和闪长岩),主要以岩基和岩株产出(Sun et al., 2019a),以及二叠纪基性-超基性杂岩。

1.1.2 小热泉子-土屋亚带

该亚带位于大草滩断裂以南、康古尔断裂以北地区,呈近东西向展布,主要发育石炭纪火山岩地层,以小热泉子地区的小热泉子组和土屋-延东一带的企鹅山群(组)、底坎儿组为代表(张洪瑞等,2010肖伟峰等,2011),以及少量二叠系(图 2b)。具体为:(1)早石炭世小热泉子组,为一套海相火山岩夹火山碎屑岩,主要由凝灰岩、安山岩、火山角砾岩和凝灰质角砾岩组成。该组中富含丰富的早石炭世生物化石,李华芹和陈富文(2002)获得该组中安山岩Rb-Sr年龄为313±8.5Ma,综合研究认为将其划分为早石炭世证据充分。(2)早石炭世企鹅山群(组),在土屋-延东一带分布广泛,主要以中酸性火山-碎屑岩为主,底部以玄武岩、安山玄武岩、安山岩、安山质角砾熔岩、凝灰岩为主;中部为含砾岩屑砂岩、凝灰岩、沉凝灰岩、夹玄武岩、安山岩、安山质角砾熔岩,及薄层状、透镜状灰岩;上部为砂岩、粉砂岩、角砾熔岩及复成分砾石等(Han et al., 2006; 潘鸿迪等,2013Shen et al., 2014a, b)。前人获得其中玄武岩和安山岩形成时代为323~337Ma(侯广顺等,2005苏春乾等,2009)。(3)晚石炭世底坎儿组,主体为一套海相火山碎屑沉积岩建造,部分夹有火山熔岩和灰岩,在该组灰岩透镜体中鉴定出牙形刺化石St reptognathodus suberectusIdiognathoides sinuata和类FusulinellaFusulina等分子,时代相当于晚石炭世(张洪瑞等,2010黄兴,2018)。受康古尔剪切带的影响晚石炭世地层岩石多呈片理化、糜棱岩化。(4)二叠纪地层,主要分布在区内底坎儿南部一带,主要发育早二叠世阿奇可布拉克组一套河湖相的底砾岩、砂岩、粉砂岩;在康古尔塔格一带为杏仁状玄武岩、安山岩夹少量火山碎屑岩(新疆维吾尔自治区地质局第二区域地质测量大队,1958;新疆维吾尔自治区地质矿产局第一区域地质调查大队,1988)。

① 新疆维吾尔自治区地质局第二区域地质测量大队. 1958. 1:20底坎儿幅万地质图

① 新疆维吾尔自治区地质矿产局第一区域地质调查大队. 1988. 1:20万康古尔塔格幅地质图

该带以发育晚古生代花岗岩基为特征(Allen et al., 1993; Gao et al., 1998; Jahn et al., 2000; 宋彪等,2002a),以及330~361Ma斜长花岗岩(芮宗瑶等,2002a张连昌等,2004陈富文等,2005Zhang et al., 2008)、335Ma英云闪长岩(王银宏等,2014)及325Ma石英钠长斑岩(肖兵等,2016)侵入到石炭纪火山岩地层中。最近研究发现该带内发育还420~443Ma的闪长岩-花岗闪长岩(王超等,2015Wang et al., 2016; 肖兵等,2016林涛等,2017刘帅杰等, 2018)。

1.2 康古尔韧性剪切带

夹于康古尔断裂和雅满苏断裂之间,为一套变形变质强烈的无序地层-构造岩片,其原岩主要为复理石建造和枕状玄武岩-硅质岩-泥质岩等深水组合(王京彬等,2006)。李文铅等(2005, 2008)研究确定了沿康古尔断裂存在蛇绿岩的残片,且其代表的古洋自晚寒武世-早奥陶世就开始发育;刘崴国等(2016)获得了该带内东大沟洋壳残片上覆长石岩屑锆石U-Pb年龄介于323~416Ma之间,认为323Ma可能代表了洋盆消亡的时代。该带可能代表了哈萨克斯坦-准噶尔板块和塔里木板块之间的缝合带(姬金生等,1994王京彬等,2006木合塔尔·扎日等,2009)。

该带东部发育大量的二叠纪基性-超基性杂岩体(Qin et al., 2011),可能形成于后碰撞环境俯冲交代地幔或软流圈地幔(Deng et al., 2015; Mao et al., 2008),或为地幔柱活动产物(Qin et al., 2011; Su et al., 2012),也可能是地幔柱与后碰撞造山作用叠加的结果(王京彬等,2008)。

1.3 阿奇山-雅满苏岛弧带

该带位于康古尔韧性剪切带(雅满苏断裂)和阿奇克库都克断裂之间。该带仅发育晚古生代地层(图 2c),主要包括:(1)早石炭世阿奇山组为一套海相火山岩,主要由安山岩、英安质火山岩及同成分火山凝灰岩、角砾凝灰岩等组成。获得该组火山岩U-Pb年龄为334~348Ma(苏春乾等,2009罗婷等,2012孙志远等,2018a;本文)。(2)早石炭世雅满苏组为一套碳酸盐岩沉积,主要为灰色微晶灰岩、含生物碎屑微晶灰岩、生物碎屑灰岩、沉凝灰岩、凝灰质砂岩等,含珊瑚、蜓类等生物化石。(3)晚石炭世土古土布拉克组为一套浅海相火山-沉积岩建造,以火山熔岩为主,与紫红色砂岩、凝灰质砂岩互层产出,局部夹有灰岩透镜体。前人获得该组大量火山岩定年数据,介于304~316Ma之间(宋安江等,2006Zhao et al., 2018a; 李航等,2018)。(4)二叠纪阿其克布拉克组为一套陆相火山-磨拉石建造,主要岩性为底砾岩、红色砂岩、粉砂岩夹少量玄武岩、玄武玢岩等。

该带内发育246~349Ma的花岗岩(吴昌志等,2006周涛发等, 2010张维峰等,2017)、318Ma的闪长玢岩(孙志远等,2018b),以及260~290Ma的基性岩墙(林瑶等,2014)。

1.4 中天山地块

位于阿奇克库都克断裂以南,出露的地层主要为前寒武纪基底,主要由中元古界的长城系星星峡群和蓟县系卡瓦布拉克群的片岩、片麻岩、混合岩和大理岩等组成。区内发育大量的古生代花岗岩类侵入体(尼加提·阿布都逊等,2015陈雅茹等,2019)。

2 古弧盆体系划分

根据东天山地区构造、地层、岩浆岩特征,综合前人研究成果,与构造单元相对应,以康古尔韧性剪切带(缝合带)为界,将东天山划分为两大古弧盆体系,分别为大南湖-头苏泉早-晚古生代弧盆体系和阿齐山-雅满苏晚古生代弧盆体系。

2.1 大南湖-头苏泉早-晚古生代弧盆体系

空间上位于大南湖-头苏泉岛弧带内。其中卡拉塔格亚带是该弧盆体系地质事件记录最为完好的地区,以卡拉塔格矿集区为典型代表,尤其是保存了早古生代地质记录。卡拉塔格矿集区核部发育奥陶系-志留系海相火山-沉积岩地层,其为主要赋矿围岩(图 2a)。该区早古生代火山岩具富钠特征,且与富Nb玄武岩浆具有相似性(唐俊华等,2006),其中的安山岩具有低铁钙碱系列高镁安山岩特征(李玮等,2016);岩石组成从玄武岩-安山岩-英安岩-流纹岩均有发育(表 2图 5a),以拉斑系列-钙碱系列为主,有向高钾钙碱性演化的特征(图 5b,ZK0801钻孔因位于红海VMS矿化较好的部位,围岩火山岩均不同程度发生矿化蚀变,这对主量元素特征有一定的影响,但综合矿集区火山岩其它未发表数据及前人研究成果来看,该特征普遍存在);稀土元素特征整体表现为轻重稀土分异明显,Eu具负异常,富集大离子亲石元素Ba、Th、U、K,亏损高场强元素Nb、Ta、Sr、P、Ti,表现出弧岩浆的特征(表 3图 5cd);矿集区内早志留世次流纹岩类具有相同的地球化学特征(龙灵利等,2017);综合该时期火山岩岩石组合及地球化学特征,认为其可能为岛弧环境产物。卡拉塔格矿集区外围呈环状发育晚古生代泥盆系-石炭纪火山-沉积岩建造:D-C火山岩从玄武安山岩-流纹岩均有发育,均为偏铝质钙碱性岩石(表 2图 6ab,以玉带北东地区路线剖面进行重点解剖);其微量元素和稀土元素特征较为类似,与早古生代火山岩特征可类比,表现为Rb、K等大离子元素略富集,Nb、Ta、Sr、P、Ti明显亏损(表 3图 6cd),但二者间仍存在一定的差异性,泥盆纪火山岩铕多具负异常(δEu=0.68~~0.83),而石炭纪火山岩铕异常多不明显(δEu=0.53~1.02),总得的来看二者仍表现出弧岩浆的地球化学特征(表 3图 6cd)。该矿集区内的侵入岩主要由闪长岩、石英闪长岩、花岗闪长岩及花岗斑岩组成,集中形成于427~453Ma和379~387Ma间,表现为准铝质-过铝质、低钾钙碱性-高钾钙碱性系列的岩石特征,同样具Ba、K、U等大离子元素略富集,Nb、Ta、P、Ti等亏损的弧岩浆特征(Du et al., 2018a; Mao et al., 2018; 陈磊等,2018Sun et al., 2019a),且与矿化有关的岩体表现出埃达克岩的特征(Mao et al., 2018Sun et al., 2019a)。

表 2 东天山卡拉塔格矿集区火山岩主量元素地球化学数据表(wt%) Table 2 Major element of the volcanic rocks from Kalatage ore cluster area in eastern Tianshan (wt%)

图 5 东天山卡拉塔格矿集区红海ZK0801钻孔火山岩地球化学特征图 (a) TAS图解(据Middlemost,1994); (b) K2O-SiO2图解(据Peccerillo and Taylor, 1976); (c)球粒陨石标准化稀土元素配分图(标准化值据Sun and McDonough, 1989); (d)原始地幔标准化微量元素蛛网图(标准化值据Wood et al., 1979) Fig. 5 Geochemical diagrams of volcanic rocks from the ZK0801drillhole of Honghai in Kalatage district in eastern Tianshan (a) TAS diagram (after Middlemost, 1999); (b) K2O vs. SiO2 diagram (after Peccerillo and Taylor, 1976); (c) chondrite-normalized rare earth element patterns (normalization values after Sun and McDonough, 1989); (d) primitive mantle-normalized multi-element plots (normalization values after Wood et al., 1979)

表 3 东天山卡拉塔格矿集区火山岩微量元素地球化学数据表(×10-6) Table 3 Trace element of the volcanic rocks from Kalatage ore cluster area in eastern Tianshan (×10-6)

图 6 东天山卡拉塔格矿集区D-C火山岩地球化学特征图 (a) TAS图解(据Middlemost,1994),碱性系列与亚碱性系列岩石的分界线(图中虚线)据Irvine and Baragar(1971);(b) K2O-SiO2图解(据Peccerillo and Taylor, 1976);(c)球粒陨石标准化稀土元素配分图(标准化值据Sun and McDonough, 1989);(d)原始地幔标准化微量元素蛛网图(标准化值据Wood et al., 1979) Fig. 6 Geochemical diagrams of Devonian-Carboniferous volcanic rocks in Kalatage ore cluster area in eastern Tianshan (a) TAS diagram (after Middlemost, 1999); (b) K2O vs. SiO2 diagram (after Peccerillo and Taylor, 1976); (c) chondrite-normalized rare earth element patterns (normalization values after Sun and McDonough, 1989); (d) primitive mantle-normalized multi-element plots (normalization values after Wood et al., 1979)

小热泉子-土屋亚带内的地层-岩浆则较好保存了该弧盆体系石炭纪地质事件印记。前人研究显示该亚带中石炭纪火山岩以拉斑质-钙碱性岩石为主,其具有富Nb玄武岩-高镁安山岩-埃达克岩组合特征,反映了其形成于岛弧环境,且洋壳俯冲在其中发挥重要作用(侯广顺等,2006王强等,2006张洪瑞等,2010李源等,2011)。与斑岩型矿化有关的326~361Ma斜长花岗岩、420~443Ma闪长岩-花岗闪长岩也具埃达克岩特征(芮宗瑶等,2002a张连昌等,2004陈富文等,2005Zhang et al., 2008张达玉等,2010林涛等,2017刘帅杰等,2018)。

大南湖-头苏泉岛弧带内发育的奥陶纪-石炭纪火山-沉积岩地层(见前文)反映出在该带内不同地质时期可能有海盆的存在。在卡拉塔格地区发育有早志留世红柳峡组400多米厚的沉凝灰岩,且该地层在区域上有一定的展布,在土屋-延东北侧也有一定的出露;该层位中还发育有红海大型VMS型矿床(毛启贵等,2010Deng et al., 2016邓小华等,2018),这均暗示了这一时期该区发育有海盆,其可能为一弧间盆地。早石炭世,小热泉子一带小热泉子组火山凝灰岩、凝灰质细-粉砂岩的发育及赋存于该层位中VMS型矿床的发育(李华芹和陈富文,2002刘申态等,2012张文东等,2018)同样暗示了这一时期局部海盆的存在。综合该带地质及成矿特征,推测大南湖-头苏泉岛弧带从奥陶纪到石炭纪,经历了多期弧-盆的转换,从而构成了大南湖-头苏泉奥陶纪-石炭纪弧盆体系。

2.2 阿奇山-雅满苏晚古生代弧盆体系

空间上位于阿奇山-雅满苏岛弧带内。该弧盆体系主要发育晚古生代石炭纪火山-沉积岩系,区内出露岩系主要为东西向延伸的早石炭世阿奇山组火山岩及同成分的火山沉积岩、雅满苏组碳酸盐岩,以及在区内南缘沿阿奇克库都克断裂东西向呈带状展布的晚石炭世土古土布拉克组火山熔岩(苏春乾等,2009罗婷等,2012木合塔尔·扎日等,2015孙志远等, 2016a, b)。

大量的研究资料表明,研究区内石炭纪火山岩从玄武岩-安山岩-英安岩-流纹岩均有发育,以钙碱性系列为主,具有富Na的特征(孙志远等,2018a),富集Th、U、Rb、Sr,亏损Nb、Ta、Ti、P等元素,显示弧岩浆特征(侯广顺等,2006李源等,2011孙志远等, 2016a, b王雯等,2016李航等,2018罗婷等,2019)。在阿奇山地区,早石炭世阿奇山组除发育具正常岛弧岩浆特征的火山岩外,主体火山岩具有高SiO2、Na2O、Al2O3、Sr,低MgO、Y、Yb,明显亏损高场强元素Nb、Ta的特征,显示埃达克岩特征(苏春乾等,2009)。从早石炭世到晚石炭世,研究区内火山岩有由钙碱性-高钾钙碱性演化的趋势,有由不成熟向成熟岛弧演化的特征(木合塔尔·扎日等,2015)。

近同期发育的石炭纪花岗岩类(329~336Ma)、闪长玢岩(318Ma)等侵入岩多为拉斑玄武质-钙碱性系列,同样表现出亏损Nb、Ta、Ti,富集Rb、Ba、Th等弧岩浆的特征(吴昌志等,2006Du et al., 2018b孙志远等,2018b);而二叠纪的钾长花岗岩-二长花岗岩则具高的K2O+Na2O、FeO/MgO、Ga/Al、HFSE (Zr、Hf)值和低CaO、Sr、Ba值,显示A2型花岗岩特征(Du et al., 2018b)。

在该弧盆体系石炭纪火山岩及侵入岩中发现有古老继承锆石的存在(周涛发等,2010罗婷等,2012; 张维峰等,2017),且继承锆石的年龄范围与中天山陆块和塔里木克拉通碎屑锆石所记录的岩浆事件具有相似性(罗婷等,2019),花岗岩类具古老的Nb模式年龄(1104~1195Ma,Du et al., 2018b),以及火山岩Th/Ta(1.5~6.1)、Ta/Yb比值(0.10~0.33)(侯广顺等,2006)等信息均显示了该区具有古老的陆壳基底,这一时期的岩浆岩可能形成于大陆边缘弧环境。

阿奇山-雅满苏岛弧带地质特征反映出它是一个海相地层发育的大陆边缘弧。早石炭世沉积了大于2000m厚的阿奇山组海相火山-沉积岩系,其中,在雅满苏地区厚度较大,且在雅满苏及其东部南北大沟一带可见沉凝灰岩及硅质岩层的发育,而在阿奇山一带稍薄;雅满苏组以碳酸盐岩沉积为主;晚石炭世土古土布拉克组以浅海相凝灰质碎屑岩、安山质火山碎屑岩及杏仁状玄武岩建造为主(李航等,2018)。该带内石炭纪火山岩整体从北向南、由下向上有从半深海火山沉积建造-浅海相陆缘中酸性岩建造-滨海相大陆拉斑玄武建造过渡的特征(王雯等,2016),反映了该区石炭纪有海盆的发育。而且,在海盆环境中形成大量与海相火山-沉积作用有关的铁矿床,如雅满苏火山喷流沉积型矿床、翠岭海相沉积型矿床、库姆塔格海相火山-沉积岩型矿床等(姜福芝等,2002王京彬等,2006徐仕琪等,2011)。综合阿奇山-雅满苏岛弧带石炭纪地质及成矿特征,推测该区石炭纪具弧-盆共存的格局,从而构成了阿奇山-雅满苏古弧盆体系。

3 古弧盆体系成矿规律 3.1 矿床空间分布规律

根据东天山古弧盆体系重点矿种、主要类型矿床空间上成群、成带分布的特征,结合区域构造-地质特征,与主要构造单元相对应,将东天山古弧盆体系划分为大南湖-头苏泉成矿带和阿奇山-雅满苏成矿带,其中大南湖-头苏泉成矿带又划分为卡拉塔格成矿亚带和小热泉子-土屋成矿亚带(图 1)。

3.1.1 大南湖-头苏泉成矿带

主要发育VMS型Cu(Zn)矿床和斑岩(-矽卡岩-浅成低温热液)型Cu多金属矿床。

3.1.1.1 卡拉塔格成矿亚带

发育VMS型Cu(Zn)矿、斑岩型Cu(Mo-Au)矿、浅成低温热液型Cu(Zn-Au)矿、矽卡岩型Cu-Fe矿,主要集中在卡拉塔格矿集区,赋存于早古生代O-S火山-沉积岩地层中(图 2a)。

斑岩型以玉带Cu(Mo-Au)矿床为代表,产于O2-3大柳沟组火山岩地层中(图 2a),致矿岩体为石英闪长斑岩,矿化以脉状、细脉状及细脉浸染状产于岩体上部,具有典型的硅化-钾长石化-黑云母化-青磐岩化斑岩型蚀变,且由岩体向外具面状分带(Sun et al., 2018)。

VMS型以红海Cu(Zn)矿床为代表,主要赋存在S1红柳峡组火山-沉积岩中(图 2a),层控特征明显,矿体具“上层下脉”的二元特征,块状矿体产于沉凝灰岩、长英质火山碎屑岩的顶部;矿体上盘围岩基本无蚀变,下盘蚀变较强,具较典型VMS型成矿特征(毛启贵等,2010Deng et al., 2016);成矿可划分为VMS成矿期、后期热液叠加期和表生期,热液叠加期包括钠长石化阶段、绿泥石-绿帘石阶段和石英-碳酸盐阶段(黄健瀚等,2016)。最近在红海矿床东南部发现的金岭-黄滩Au-Cu矿床,成矿与红海矿床可类比,同样赋存于S1红柳峡组中,经历了早期的海底火山喷流沉积成矿作用,形成了Cu-Zn矿体,后期又叠加了岩浆热液成矿作用,形成Au矿体,为典型的沉积-热液叠加成矿系统(邓小华等,2018)。

浅成低温热液型以红石Cu(Mo-Au)矿床为代表,矿体主要赋存在S1卡拉塔格组火山-次火山岩中(图 2a),矿体受构造控制明显,主要呈陡脉状,矿石类型主要为石英脉型和角砾型,发育梳状、晶簇/晶洞状结构;以矿脉两侧的线状蚀变为特征(邓小华等,2014),成矿可能与区内次流纹岩密切相关(龙灵利等,2017)。

矽卡岩型以西二区Cu-Fe(Au)矿床为代表,矿体沿一北西向断裂分布于O-S火山-火山碎屑岩、D1大南湖组凝灰质粉砂岩-生物碎屑灰岩及石英闪长斑岩的接触部位(图 2a),矿体与D1灰岩亲密伴生,矿体为铁铜矿体,西段以铁为主,东段为铁铜矿体;矿石类型主要有浸染状、似层状和块状矿石;矽卡岩化蚀变包括石榴子石化、透辉石化、钾化、绢云母化、硅化、绿帘石化、绿泥石化、碳酸盐化等,其中石榴子石化、透辉石化、绿帘石化、硅化与成矿最为密切;石英闪长斑岩本身也具弱的钾化、硅化、绿帘石化、绿泥石化和碳酸盐化(Mao et al., 2018)。

3.1.1.2 小热泉子-土屋成矿亚带

以发育斑岩型Cu(Mo)矿床为显著特征,主要分布在该成矿亚带的中东部(图 1)。中部以土屋、延东,赤湖,灵龙为代表。土屋-延东矿床主要赋存在C1企鹅山组火山岩中(图 2b),矿体主要分布在该地层和斜长花岗斑岩中,传统认为斜长花岗斑岩为其致矿岩体(张连昌等,2004张达玉等,2010Shen et al., 2014a, b; 王银宏等,2014),最新研究认为该矿床为早期斑岩成矿与后期热液叠加改造而成,石英钠长斑岩是导致叠加改造形成的主因(王云峰等,2016肖兵等,2016)。东部以玉海和三岔口矿床为代表,其矿体均为隐伏矿体,含矿岩体为闪长岩-花岗闪长岩,表现为(类)埃达克岩特征;矿化、蚀变特征均表现为斑岩型矿床特征(Wang et al., 2016; 张照伟等,2016林涛等,2017刘帅杰等,2018)。同时,该亚带内还发育VMS型Cu-Zn矿床,主要分布在该成矿亚带的西部,以小热泉子为代表。该矿床主要赋存在C1小热泉子组火山-沉积岩中(图 2b),矿床具“上层下脉”、“上铜下锌”特征,层控特征明显,成矿具VMS成矿期-热液期叠加的特征(刘申态等,2012张文东等,2018)。

3.1.2 阿奇山-雅满苏成矿带

该成矿带主要发育海相火山岩型Fe(Cu)矿床、IOCG型Fe-Cu(-Au)矿床、矽卡岩型Fe(Cu)矿、VMS型Cu矿床、热液脉型Cu矿床、银多金属矿床、自然铜矿床等。

海相火山岩型Fe(Cu)矿床主要产于C1阿奇山组地层中(图 2c),以火山喷流沉积型为主,矿体层控特征明显,主要呈似层状、透镜状、脉状产于矽卡岩化的火山-沉积岩中或火山岩与沉积岩的岩性界面处,往往矿区不发育可能引起矽卡岩化的侵入体。该类型以雅满苏Fe矿床为代表,矿体产于C1阿奇山组石榴子石矽卡岩中,且与矿区地层产状基本一致,矿石类型有块状、气孔状、条带状和浸染状。矿体的产出状态及矿石的组成特征,显示该矿床具有喷流沉积和火山热液叠加的成矿特征(孙志远,2018)。早期火山喷流沉积形成块状矿体,明显受地层产状控制;晚期火山热液叠加形成脉状、透镜状矿体(伴生硫化物较为发育),这与韩春明等(2018)认识较为一致,正是后期的热液活动引起围岩蚀变形成矽卡岩化(李厚民等,2014韩春明等,2018)。

IOCG型Fe-Cu(-Au)矿床,典型矿床包括黑尖山、沙泉子和多头山Fe-Cu矿床。Fe-Cu矿体呈透镜状和似层状,矿石矿物主要为铁氧化物(磁铁矿/赤铁矿)和铜硫化物(黄铜矿、斑铜矿等);矿化阶段包括早期的Fe矿化和晚期的Cu矿化阶段;黑尖山Fe-Cu矿床局部富集Au(赵联党等,2017; Zhang et al., 2018; Zhao et al., 2018b)。

VMS型Cu矿床,以银帮山Cu(Zn)矿床为代表,矿区发育纹层状含铁硅质岩等喷流沉积岩,矿石具有典型的块状和条带状构造(王京彬等,2006),矿体主要赋存在C1阿奇山组火山-沉积岩中。在发育VMS型矿化体地层的上部层位发育矽卡岩型FeCu矿化,层状矿体主要赋存在凝灰岩与大理岩之间的矽卡岩中,部分矿体受断裂控制,呈脉状展布(图 7)。

图 7 东天山银帮山矽卡岩型Fe(Cu)矿床野外露头 Fig. 7 Field outcrop of Yinbangshan skarn-type Fe(Cu) deposit in eastern Tianshan

热液脉状Cu矿床,矿体以细脉状、细脉浸染状矿化为主,矿体受构造控制明显,围岩蚀变较弱,以绿泥石化、绿帘石化为主;矿石矿物主要为黄铜矿,伴生黄铁矿不发育,以寨北山、铜鱼梁为代表(龙灵利等,2018孙志远等,2018b)。

银多金属矿床以维权为代表,产于C2土古土布拉克组中酸性-中基性火山岩、碎屑岩和碳酸盐岩中,容矿岩石为钙铁榴石矽卡岩。该矿床成矿可划分为沉积期、热液成矿期和表生期,成矿主要发生在热液期,是铁铜、钴、银3期成矿叠加的产物,钴成矿是独立的一期中高温热液成矿作用,含钴铁铜矿石是钴成矿叠加在铁铜成矿作用之上形成,含银钴铜矿石是银成矿作用叠加在钴成矿作用之上形成(李立兴等,2018)。

与玄武岩有关的自然铜矿床,自西向东有十里坡、黑龙峰、长城山、东尖峰等矿点,自然铜矿化主要发育在玄武岩、杏仁状玄武岩和凝灰岩夹层中,玄武岩是自然铜矿化重要的矿源层;以十里坡矿床为典型代表,其发育5层含铜凝灰岩层,矿石矿物主要为自然铜和砷铜矿,以浸染状自然铜为主,偶见黄铜矿和赤铜矿(王京彬等,2006袁峰等,2010张达玉等,2012)。

3.2 矿床成矿时间演化规律

卡拉塔格成矿亚带成矿时代集中在奥陶-泥盆纪(表 4)。Sun et al.(2018)获得玉带斑岩型矿床辉钼矿Re-Os年龄为449.5±4.2Ma,致矿石英闪长斑岩锆石U-P年龄为452.7±2.8Ma,使其成为东天山地区有年代学约束的最老的斑岩型矿床。红海VMS型矿床赋矿凝灰岩430.0±1.7Ma (Deng et al., 2018)和黄铜矿Re-Os年龄434.2±3.9Ma(Deng et al., 2016)限定了其形成于早志留世。红石浅成低温热液型矿床黄铜矿Re-Os年龄431.8±2.7Ma(Deng et al., 2016)以及与成矿密切相关的次流纹岩439.9±4.8Ma的年龄(龙灵利等,2017)限定了其与红海成矿时代相近。Mao et al.(2018)获得西二区矽卡岩型矿区与成矿有关的石英闪长斑岩锆石U-Pb年龄为382.1±2.4Ma,间接限定了其成矿时代为泥盆纪。

表 4 东天山古弧盆体系成矿时代统计表 Table 4 The statistical data of metallogenic ages of the paleo arc-basin system in eastern Tianshan

小热泉子-土屋成矿亚带成矿时代主要为早石炭世(表 4)。土屋-延东-延西斑岩型矿床成岩时代多集中在322~339Ma,其Re-Os成矿年龄介于319~326Ma间(芮宗瑶等,2002a陈富文等,2005张达玉等,2010;Han et al., 2014; Shen et al., 2014a, b; 王银宏等,2014肖兵等,2016);玉海矿床成矿早于土屋一带,形成于352Ma,且成矿远晚于成岩时代(430~442Ma, Wang et al., 2016)。而三岔口矿床最新研究表明其成矿时代为416Ma(林涛等,2017),反映出该成矿亚带内也发育有早古生代斑岩型矿床。小热泉子VMS型矿床主要赋存在早石炭世火山-沉积岩地层中,赋矿地层中的凝灰岩SHRIMP锆石U-Pb年龄352Ma(邓小华等,未发表资料)以及安山岩Rb-Sr年龄313Ma(李华芹和陈富文,2002)间接限定了其成矿时代为早石炭世。

阿奇山-雅满苏成矿带主要可划分出早石炭世和晚石炭世末期两期成矿事件(表 4)。早石炭世主要形成火山喷流沉积型铁矿,雅满苏铁矿床主要赋矿层位由侵入其中的辉绿岩脉限定为早于355Ma(李厚民等,2014),暗示火山喷流期成矿可能为早石炭世或更早地质时期,323Ma的石榴子石矽卡岩(Hou et al., 2014)及322Ma的黄铁矿Re-Os年龄(Huang et al., 2018)可能反映了热液叠加期成矿时代;获得红云滩铁矿床Re-Os年龄为324Ma(Sun et al., 2019b),矿体上部石英角斑岩年龄为324Ma(郑仁乔,2015),较好的限定了其成矿时代为早石炭世;银帮山上部矽卡岩型Fe-Cu矿化赋矿围岩凝灰岩335.5±2.6Ma年龄(表 1图 8)间接限定了其成矿时代为早石炭世。晚石炭世末期主要形成IOCG型Fe-Cu-Au和自然铜矿床,黑尖山矿床与磁铁矿共生的榍石U-Pb年龄310Ma(赵联党,2018),沙泉子矿床黄铁矿Re-Os年龄295Ma(Huang et al., 2013)反映该区IOCG型矿床主要形成于晚石炭世末期;自然铜矿床中与成矿有关玄武岩成岩时代介于306~309Ma间(袁峰等,2007张达玉等,2012),限定了其成矿时代为晚石炭世末期;此外,维权银多金属矿床矿区侵入297Ma花岗岩限定了其成矿上限,推测成矿发生在晚石炭世末期(王龙生等,2005)。该成矿带内热液脉型矿床其成矿时代从早石炭-晚石炭世均有发育,获得寨北山主要赋矿安山玢岩及黄铁矿Re-Os年龄均为338Ma(龙灵利等,2018孙志远等,2018a),铜鱼梁矿床与成矿密切相关的闪长玢岩U-Pb年龄为318Ma(孙志远等,2018b)。

图 8 东天山银帮山凝灰岩锆石U-Pb年龄谐和图(a)和加权平均年龄图(b) Fig. 8 Diagrams of U-Pb concordia age (a) and weighted average age (b) for zircons of tuff from Yinbangshan district in eastern Tianshan
3.3 东天山古弧盆体系成矿规律

在上述东天山古弧盆体系主要类型矿床成矿特征及时空分布特征研究的基础上,结合前人研究,进一步总结出该弧盆体系成矿具有如下特征。

VMS成矿系统与斑岩成矿系统共存。一般认为VMS型和斑岩型矿床不会在同一区域产出(Sillitoe,1999王京彬等,2006黄健瀚等,2016),但东天山古弧盆体系主要类型矿床时空分布特征显示研究区内同时发育斑岩型和VMS型矿床。以卡拉塔格矿集区为典型代表,早志留世,近同时发育了红海VMS型矿床和红石浅成低温热液矿床;小热泉子-土屋成矿亚带也同时产出土屋-延东斑岩型矿床和小热泉子VMS型矿床;阿奇山-雅满苏成矿带同时发育火山喷流沉积型铁矿(成矿特征与VMS型矿床类似)和热液脉型Cu矿床、VMS型Cu矿和矽卡岩型Fe(Cu)矿床。该现象在三江特提斯成矿域同样可见,如羊拉、老厂矿床(邓军等,2012);在西南太平洋巴布亚新几内亚现代弧盆体系中亦可见,在Lihir岛弧发育Ladolam斑岩-浅成低温热液型Au矿床(Müller et al., 2002),在Manus弧后盆地发育Solwara VMS型Cu-Zn矿床(Hannington et al., 2011; Gena,2013)。

叠加成矿作用普遍发育,在矿集区-矿床尺度内形成了多种类型的叠加成矿作用。在卡拉塔格矿集区内,从奥陶-泥盆纪,形成了斑岩型-VMS型-浅成低温热液型-矽卡岩型成矿的叠加。在矿床范围内,多期叠加成矿更为普遍,红海、金岭-黄滩、小热泉子VMS型铜锌矿床及雅满苏、红云滩等火山喷流沉积型铁矿床均具有火山喷流沉积和岩浆热液成矿叠加的特征(刘申态等,2012黄健瀚等,2016Sun et al., 2018邓小华等,2018韩春明等,2018张文东等,2018);土屋-延东斑岩型铜钼矿床具斑岩期和热液期成矿的叠加(王云峰等,2016肖兵等,2016);银帮山在早期火山喷流沉积Cu矿化基础上叠加了矽卡岩型Fe-Cu矿化;黑尖山IOCG型Fe-Cu(-Au)矿床表现为早期Fe矿化(岩浆热液)和晚期Cu矿化(盆地卤水)的叠加(赵联党等,2017);维权银多金属矿床也表现沉积期和热液期成矿的叠加,且热液期是铁铜、钴、银3期成矿叠加的产物(李立兴等,2018)。

发育两次大规模成矿事件,且均与大规模火山-侵入岩浆活动相关。早志留世,发育VMS型-(斑岩-)浅成低温热液型Cu矿床(红海、红石),赋存在早志留世火山-沉积岩中,主要分布在卡拉塔格矿集区。早石炭世,形成与早石炭世火山活动有关的VMS型Cu矿床(小热泉子)和海相火山岩型Fe矿床(火山喷流沉积型Fe矿床,雅满苏、红云滩),以及与这一时期侵入岩浆活动相关的斑岩-热液脉型Cu矿床(土屋-延东、寨北山等),分布于康古尔韧性剪切带的两侧小热泉子-土屋成矿亚带和阿奇山-雅满苏成矿带内。

4 讨论 4.1 吐哈盆地南缘存在古老微陆块残片

准噶尔板块基底组成一直存有争议,主要观点包括:由年轻洋壳和岛弧杂岩组成(Carroll et al. 1990; 王方正等,2002胡霭琴和韦刚健,2003Chen and Jahn., 2004; Zheng et al., 2007);由前寒武陆壳组成(吴庆福,1987黄汲清等,1990何国琦等,1994李锦轶等,2000Xu et al., 2015);为含有陆壳碎块的洋壳组成(肖序常, 1991, 1992李锦轶和肖序常,1999);或为底垫或底侵的二叠纪岩浆岩(韩宝福等,1998)等。对于准噶尔板块南缘的构造属性,也存在很多不同观点:如徐学义等(2014)综合前人地球物理、沉积建造、碎屑锆石年代学等成果认为在准噶尔板块的南缘存在包括前震旦纪、元古代,乃至太古代地层的古老陆块;此外,Xu et al. (2015)还在塔黑尔一闪长岩墙中发现了片麻岩、磁铁石英岩包体,在达子沟发现含有片麻岩砾石的变形奥陶纪砾岩,在双岔沟花岗岩中也发现有片麻岩的残余,并获得他们的U-Pb年龄及其中继承锆石年龄介于437~3060Ma之间,综合研究认为准噶尔陆块可能为劳伦大陆Superior地区的碎块;宋继叶等(2015)通过地球物理、航空磁测、同位素年代学及古生代研究认为包括吐哈盆地在内的准噶尔盆地具有前寒武纪结晶基底与海西期褶皱基底组成的“双层”基底结构;孙石达等(2016)研究显示吐哈盆地地壳磁性较厚且连续,具古老陆壳基地属性。近年来在吐哈盆地南缘卡拉塔格矿集区古生代火山岩、侵入岩中500~2600Ma继承锆石的发现(龙灵利等,2017Deng et al., 2018; Sun et al., 2019a),进一步显示在准噶尔板块南缘可能存在古老微陆块的残片,可能有吐哈微陆块的存在。综合前人研究资料,本文认为至少在准噶尔板块的南缘(吐哈盆地南缘一带)存在古老陆块的残片。

4.2 东天山古弧盆体系构造演化

东天山构造演化与古亚洲洋形成、演化紧密相关,但对其构造格局的认识则存在不同观点:有人认为其为塔里木古板块活动陆缘弧盆体系的一部分(马瑞士等,1993李兆丽等,2011),也有人认为它是西伯利亚、哈萨克斯坦和塔里木板块的碰撞带(李春昱等,1982李锦轶等,1992肖序常等,1992)或者是哈萨克斯坦和塔里木板块的碰撞带(姬金生等,1994周济元等,1994),还有人认为它是围绕西伯利亚板块向洋的增生弧(Şengör et al., 1993)和多次开合的手风琴运动的结果(黄汲清等,1990)等等,这些观点的形成主要源于各学者对该区受一个连续演化的洋盆还是多个洋盆的开合影响、古洋盆俯冲极性及其形成、闭合时限、最终缝合线的位置等认识的不同。

目前对东天山古弧盆体系构造演化提出的主要观点有:大南湖-头苏泉岛弧带的成因有卡拉麦里洋向南俯冲形成(肖序常等, 1992; 马瑞士等, 1997; 张连昌等, 2004张洪瑞等,2010Deng et al., 2016)、古天山洋向北俯冲在吐哈地块南缘形成的活动大陆边缘(王京彬等, 2006),以及由卡拉麦里洋和北天山洋不同时期向北和向南俯冲形成(Xiao et al., 2004; 李锦轶, 2004韩春明等,2018)等多种观点。而阿奇山-雅满苏岛弧带的形成也有多种观点,如由位于中天山和大南湖岛弧带之间的古天山洋向北俯冲形成(Xiao et al., 2004韩春明等,2018)、由双向俯冲的古康古尔洋向南俯至中天山之下形成(姬金生等,1994周济元等,2001侯广顺等,2006Wang et al., 2014)、由古康古尔洋向南俯冲至中天山地块之下形成的弧后(间)盆地(Zhang et al., 2016a)、古天山洋向北俯冲在中天山陆缘弧基础上形成的弧后盆地(罗婷等,2019)、古准噶尔洋向南俯冲形成的大南湖-头苏泉岛弧、阿奇山-雅满苏弧后盆地,构成完整弧盆体系(李源等,2011Hou et al., 2014)、裂谷成因(冯益民等,2002陈富文等,2003; Xia et al., 2003)、裂陷槽成因(芮宗瑶等,2002b王京彬等,2006),以及喀拉塔格地块北部被动陆缘沉积岩系和上覆的后碰撞火山沉积岩系(李锦轶,2004)等。对于东天山最终缝合带的位置,也存在不同认识,如位于卡拉麦里洋(马瑞士等, 1993李源等,2011)、康古尔断裂和雅满苏断裂之间的康古尔剪切带(康古尔缝合带)(姬金生等,1994王京彬等,2006)、康古尔断裂和阿奇克库都克断裂之间(康-阿碰撞缝合带)(木合塔尔·扎日等,2010)、南天山洋等(Xiao et al., 2004; 韩春明等,2018)。

本文在前人研究基础上,综合大南湖-头苏泉岛弧带地层-岩浆-成矿等最新研究进展来分析,该区岩浆岩多表现为弧岩浆的特征,部分显示埃达克岩特征;且该区火山岩、侵入岩以及成矿从卡拉塔格亚带到小热泉子-土屋亚带(从北向南)均有变新的趋势,反映了古洋壳向北俯冲的极性;同样,阿奇山-雅满苏岛弧带内石炭纪火山岩和侵入岩也表现具弧岩浆的特征,且从早石炭世-晚石炭世由北向南壳幔岩石圈有明显增厚的现象,反映了古洋壳向南俯冲的极性(木合塔尔·扎日等,2015)。结合大南湖-头苏泉岛弧带和阿奇山-雅满苏岛弧带之间沿康古尔韧性剪切带展布的康古尔塔格、大东沟蛇绿混杂岩(李文铅等, 2005, 2008刘崴国等,2016)的发育,代表了古洋盆的存在。综合分析,本文较认同古生代康古尔洋发生了向南、北两侧的双向俯冲。

向北,奥陶纪-石炭纪,在具多岛洋格局的汇聚板块边缘岛弧区,随古康古尔洋持续俯冲于发育有古老陆壳基底残片的准噶尔板块之下,在大南湖-头苏泉一带形成一“长寿弧”(大南湖-头苏泉岛弧带)。奥陶-早泥盆世,在卡拉塔格一带形成岛弧带,发育厚层的富Na的具弧岩浆特征的火山岩及火山-沉积岩系,以及部分具埃达克岩特征的中酸性侵入岩。中泥盆世(-晚泥盆世?),早期形成的岛弧与准噶尔板块南缘微陆块(吐哈微陆块?)发生碰撞,形成一套磨拉石建造。可能正是由于这次的碰撞事件诱发古康古尔洋早石炭世开始向南俯冲,形成了这一时期的南、北双向俯冲。早石炭世,随古康古尔洋继续向北俯冲,主要在小热泉子-土屋一带形成石炭纪岛弧,发育富Nb玄武岩-高镁安山岩-埃达克岩组合,叠加在奥陶-泥盆纪岛弧之上,构成了大南湖-头苏泉奥陶纪-泥盆纪和石炭纪的“长寿”的复合岛弧带。

向南,石炭纪,古康古尔洋俯冲至中天山地块之下,在其北缘形成阿奇山-雅满苏大陆边缘弧,发育巨厚的富Na的具弧岩浆特征的海相火山-沉积岩系,以及百灵山、多头山等具弧岩浆特征的花岗岩类(周涛发等,2010张维峰等,2017)。

晚石炭世末期,康古尔古洋盆最终闭合(李锦轶等,2006; Wang et al., 2007; Zhang et al., 2016),弧盆体系演化结束。

二叠纪,全区范围内磨拉石建造的发育、与地幔柱有关的基性-超基性岩杂岩、双峰式火山岩、A型花岗岩的发育,以及长英质岩浆岩中幔源组分的增加等(王京彬等,2006Chen et al., 2011; Qin et al., 2011; Su et al., 2012; Mao et al., 2014; Du et al., 2018b)进一步佐证了该区已进入后碰撞板内环境。

4.3 东天山古弧盆体系区域成矿模式

在东天山古弧盆体系主要类型矿床成矿特征、时空分布规律研究的基础上,结合东天山古弧盆体系构造演化特征,初步构建了东天山古弧盆体系区域成矿模式(图 9)。

图 9 东天山古弧盆体系区域成矿模式图 Fig. 9 Regional metallogenic model of paleo are-basin system in eastern Tianshan

自奥陶纪(>453Ma)开始,古康古尔洋向北俯冲于准噶尔板块之下,在其南缘卡拉塔格一带形成一早古生代岛弧带,且该岛弧经历了多期的弧-盆转换,形成VMS型矿床和斑岩(-矽卡岩-浅成低温热液)型矿床共存格局。中晚奥陶世,该区形成大量玄武岩、安山岩以及钙碱性花岗岩类侵入,在局部发育古老陆壳残片的岛弧环境形成与埃达克质中酸性侵入岩有关的斑岩型Cu(Au-Mo)矿床(玉带)。早志留世,随古洋壳的不断俯冲,早期形成的岛弧局部拉伸形成弧间盆地,在海底因火山喷发-热液作用形成VMS型Cu-Zn矿床(红海、金岭-黄滩),由于构造-岩浆多期活动,致使该类矿床具有火山喷流和热液叠加的成矿特征;火山活动持续作用,近同期,在岛弧环境形成与次火山岩有关的浅成低温热液型Cu(Zn-Au)矿床(红石、梅岭)。早-中泥盆世,随古洋壳的持续向北俯冲,形成钙碱性火山岩及埃达克质侵入岩,并形成与埃达克质侵入岩有关的斑岩型Cu-Mo矿床(三岔口)、矽卡岩型Fe-Cu矿床(西二区)。

早石炭世,古康古尔洋向北继续俯冲,在小热泉子-土屋岛弧带内形成弧-盆共存的格局,在海盆环境形成VMS型Cu-Zn矿床(小热泉子),在岛弧区形成系列与埃达克质中酸性侵入体有关的斑岩型Cu-Mo矿床(土屋-延东等)。同时,古康古尔洋向南俯冲,在中天山地块北缘形成海相地层发育的大陆边缘弧,并在海盆中形成火山喷流沉积型Fe矿床,与红海、小热泉子等VMS型矿床成矿特征类似,由于火山岩浆-热液的多次脉动,成矿同样具有火山喷流与热液叠加特征(雅满苏、红云滩),以及火山喷流沉积与矽卡岩型成矿的叠加(银帮山);在岛弧环境,形成于与中酸性次火山岩-侵入岩脉有关的热液脉状Cu矿床(寨北山)。

晚石炭世末,古康古尔洋逐渐闭合,形成与海相火山岩有关的IOCG型Fe-Cu-Au矿床(黑尖山、沙泉子)和自然铜矿床(十里坡、东尖峰等)。IOCG型矿床多产于克拉通或大陆边缘构造环境,与拉张背景密切相关(Hitzman,2000Groves et al., 2010);与玄武岩有关的自然铜矿床中玄武岩多为地幔柱成因(Cannon et al., 1999; Zhu et al., 2003),东尖峰等矿区玄武岩与研究区早二叠世Cu-Ni矿化基性-超基性岩具有同源特征(张达玉等,2012),而Cu-Ni矿化的基性-超基性岩可能为地幔柱活动产物(Qin et al., 2011; Su et al., 2012),推测发育自然铜矿化的玄武岩也可能有地幔柱作用的参与。这两类矿床的发育也进一步表明研究区逐渐过渡至后碰撞板内伸展环境。

早二叠世,研究区进入板内环境,形成与板内基性-超基性侵入杂岩有关的、跨构造单元面型分布的Cu-Ni矿床(约280Ma)(Qin et al., 2011王亚磊等,2015杨万志等,2017赵冰冰等,2018),这进一步表明了东天山古弧盆体系构造-岩浆-成矿事件的结束。

5 结论

(1) 东天山古弧盆体系以康古尔韧性剪切带为界,将其划分为两大成矿带:以北为大南湖-头苏泉早-晚古生代成矿带,以南为阿齐山-雅满苏晚古生代成矿带。沿大草滩断裂又将大南湖-头苏泉成矿带划分为卡拉塔格成矿亚带和小热泉子-土屋成矿亚带。大南湖-头苏泉早-晚古生代成矿带以铜矿化为主,卡拉塔格成矿亚带主要发育奥陶纪-泥盆纪VMS型、斑岩型、矽卡岩型、浅成低温热液型矿床,小热泉子-土屋成矿亚带主要发育早石炭世VMS型、斑岩型矿床。阿齐山-雅满苏晚古生代成矿带以铁矿化为主,主要发育早石炭世火山喷流沉积型矿床和晚石炭世IOCG型、自然铜矿床。

(2) 东天山地区奥陶-石炭纪随古康古尔洋向南、北两侧的俯冲,在南、北形成的两个弧-盆体系中形成早志留世VMS型Cu矿、浅成低温热液型Cu矿和早石炭世斑岩型Cu矿、火山喷流沉积型Fe矿大规模成矿;在晚石炭世末盆地闭合期形成IOCG型Fe矿、自然铜矿。二叠纪跨构造单元面状分布的岩浆型Cu-Ni矿床的发育标志着该弧-盆体系演化已结束,其为后碰撞阶段岩浆作用结果,已非该弧盆体系的产物。

(3) 东天山古弧盆体系古生代经历了多方向、多期次的弧-盆转换,导致了该体系内VMS成矿系统与斑岩成矿系统的共存,弧-盆的长期演化,岩浆的多次脉动,造成该体系内矿床具多种类型叠加的成矿特征。

致谢      笔者在项目研究工作中与陈华勇研究员、龙晓平教授进行过多次交流探讨,受益匪浅;本文是基于课题组集体研究成果的总结;杨利亚博士、赵路通博士等人对本文成文做出了有益贡献;李锦轶研究员、张连昌研究员对本文进行了认真细致的审阅,并提出宝贵修改意见和建议;在此一并表示感谢。

谨以此文向肖序常院士九十华诞表示衷心的祝贺!祝先生身体健康、寿比南山!

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