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中央造山系横亘于中国大陆中部，近东西向延伸约5000 km，自西经昆仑造山带和祁连造山带，向东连接秦岭-大别造山带（图1）。作为中国大陆完成主体拼合的主要结合带，中央造山系不仅代表了中国南北地球物理和深部结构的重要边界（Ma Xinyuan，1989; Liu Guangding，1992; Yuan Xuecheng，1996），也是中国南北地质、地理、气候、环境、水文和生态的天然界线（Dong Yunpeng et al.，2019，2022a，2022b）。最新研究表明，中央造山系以多块体、多阶段复合造山为特征，由华北和塔里木等北方陆块群、华南和羌塘等南方陆块群以及柴达木等具有过渡性质的陆块于古生代—早中生代长期拼合而成（Zhang Guowei et al.，1995，2001; Xu and Cui，1996; Yang Jingsui et al.，2010; Xu Zhiqin et al.，2011; Dong Yunpeng et al.，2011a，2021，2022a; Dong and Santosh，2016），并遭受晚中生代—新生代强烈的陆内构造改造（Zhang Guowei et al.，2001; Dong Yunpeng et al.，2016，2021）。各陆块间不同的物质组成和结构构造导致昆仑、祁连、秦岭-大别等造山带具有复杂的构造格局和时空演化过程（Yang Jingsui et al.，2009，2010; Dong Yunpeng et al.，2011a，2019，2021，2022a）。
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本文基于近年来秦岭、祁连、昆仑造山带大量的蛇绿混杂岩、岩浆作用和变质作用的岩石、构造、地球化学和同位素年代学资料，概括总结了沿中央造山系原特提斯、古特提斯扩张、俯冲闭合的时空演化过程，为更好地理解东亚大陆拼贴的构造和地球动力学提供线索。
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1 中央造山系构造格架
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中央造山系西段包括北部的祁连造山带和南部的昆仑造山带。北部的祁连造山带夹持于阿拉善地块（华北克拉通）和柴达木地块之间，呈北西-南东向延伸约1000 km，宽约300 km。北缘以龙首山断裂为界与阿拉善地块相依，南侧以柴达木北缘断裂为界与柴达木地块相隔，西侧被阿尔金走滑断裂截切与塔里木克拉通毗邻。在东侧，祁连造山带以宝鸡-天水断裂与秦岭造山带相接，并沿六盘山弧形断裂带向北东逆冲推覆于鄂尔多斯西南缘之上。祁连造山带及其邻区自北向南可以划分为北祁连构造带（含走廊过渡带）、中祁连构造带、南祁连构造带、欧龙布鲁克地块和柴北缘构造带五个构造单元（图2），记录了阿拉善、柴达木及其之间的中祁连、欧龙布鲁克地块复杂的早古生代俯冲—增生—碰撞造山过程（Xiao Wenjiao et al.，2009; Song Shuguang et al.，2013，2014，2017; Zhang Jianxin et al.，2017; Yu Shengyao et al.，2021）。
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图1 中央造山系与中国大陆及其邻区主要陆块构造配置关系
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Fig.1 Tectonic framework of the Central China Orogenic Belt, China continent and its adjacent areas
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南部的昆仑造山带呈东西向延伸约2500 km，以北东东向阿尔金走滑断裂为界，昆仑造山带可分为东昆仑造山带和西昆仑造山带。西昆仑造山带北临塔里木克拉通，西接帕米尔高原。西昆仑造山带及其邻区以库地-其曼于特缝合带和麻扎-康西瓦缝合带为界，自北向南可依次分为西昆仑北带（塔里木南缘）、西昆仑中带、巴颜喀拉浊积岩带和甜水海地块（Pan Yusheng，1990; Jiang Chunfa et al.，1992; Yang Shufeng et al.，1999; Xiao and Wang，2004; Xiao Wenjiao et al.，2009; Dong Yunpeng et al.，2021）。西昆仑造山带总体形成于塔里木、西昆仑中带和甜水海之间长期的俯冲—增生—碰撞造山过程（Dong Yunpeng et al.，2021）。东昆仑造山带北接柴达木地块，南邻巴颜喀拉构造带（有学者称之为松潘-甘孜地块），东以共和盆地为界与秦岭造山带相接，西以阿尔金走滑断裂与西昆仑造山带分割（Jiang Chunfa et al.，1992; Li Rongshe et al.，2016; Pei Xianzhi et al.，2018）。东昆仑造山带自北向南发育祁漫塔格-香日德、阿其克库勒湖-昆中和木孜塔格-布青山-阿尼玛卿三条蛇绿混杂岩带。以此为界，可以将东昆仑造山带及其邻区分为北祁漫塔格构造带、昆中构造带、昆南构造带和松潘-甘孜构造带四个构造单元（图3）（Dong Yunpeng et al.，2018a，2021）。祁漫塔格-香日德蛇绿混杂岩带向西被阿尔金走滑断裂错断后可与西昆仑造山带的库地-其曼于特缝合带相接，而阿其克库勒湖-昆中和木孜塔格-布青山-阿尼玛卿蛇绿混杂岩带则对应于西昆仑造山带的麻扎-康西瓦缝合带。东昆仑造山带主要形成于柴达木、羌塘和松潘-甘孜的相互作用，经历了古生代—早中生代长期的俯冲—增生造山过程（Dong Yunpeng et al.，2018a，2019，2021）。
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图2 祁连造山带及邻区地质简图（据Dong Yunpeng et al.，2021修改）
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Fig.2 Geological map of the Qilian Orogen and its adjacent areas (modified from Dong Yunpeng et al., 2021)
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图3 东昆仑造山带及邻区地质简图（据Dong Yunpeng et al.，2018a修改）
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Fig.3 Tectonic outline of the East Kunlun Orogen and its adjacent areas (modified after Dong Yunpeng et al., 2018a)
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祁连和昆仑造山带之间的柴达木地块是一个独立的微陆块，记录了前寒武纪形成、早古生代造山运动及随后的陆内构造演化过程。柴达木地块多数地区覆盖巨厚的新生代地层，前新生界岩石主要分布于南部地区，包括古元古代高级变质基底和上覆奥陶系—志留系、中—上泥盆系、石炭系—下二叠系、中—上三叠统和侏罗系盖层（Wang Guocan et al.，2006; Jin Zhijun et al.，2004; Zhang Jianxin et al.，2013; Dong Yunpeng et al.，2022a）。钻井资料（Cheng Feng et al.，2017）显示，柴达木地块内部同样发育有与地块南部和东昆仑造山带北部类似的古—新元古代基底岩系、古生代地层和晚古生代侵入岩。
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在中央造山系东段，秦岭-大别造山带呈东西向延伸近2500 km，北侧沿灵宝-鲁山-舞阳断裂向北逆冲于华北南缘之上，南侧沿勉略-巴山-襄广断裂向南逆冲于华南北缘之上（Zhang Guowei et al.，2001; Dong Yunpeng et al.，2011a）。秦岭-大别造山带及其邻区以洛南-栾川断裂、商丹缝合带和勉略缝合带为界，自北向南依次划分为华北南缘、北秦岭构造带、南秦岭构造带和华南北缘四个构造单元（图4）（Dong Yunpeng et al.，2011a; Dong and Santosh，2016）。该造山带是由华北、南秦岭和华南陆块分别于早泥盆世、中—晚三叠世由北向南沿商丹和勉略缝合带俯冲碰撞形成（Zhang Guowei et al.，1995，2001; Meng and Zhang，1999; Dong Yunpeng et al.，2011a，2021，2022a; Dong and Santosh，2016）。印支期后，秦岭-大别造山带转入陆内造山，突出地表现为晚侏罗世—早白垩世华北、华南分别向造山带之下陆内俯冲，奠定了扇型抬升造山的特征（Yuan Xuecheng，1996; Zhang Guowei et al.，2001; Dong Yunpeng et al.，2011a，2021; Dong and Santosh，2016）。
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现有研究表明，中央造山系分布有大量的蛇绿岩、相关俯冲碰撞的岩浆和变质作用记录，约束了原特提斯和古特提斯构造演化过程（图5）。中央造山系北部的祁连造山带和北秦岭主要形成于原特提斯洋俯冲碰撞造山过程（Song Shuguang et al.，2013，2014，2017; Zhang Jianxin et al.，2017; Xiao Wenjiao et al.，2009; Dong Yunpeng et al.，2011a; Dong and Santosh，2016; Yu Shengyao et al.，2021）。相比之下，中央造山系南部则经历了更为复杂的演化过程。西段的东昆仑造山带经历了从早古生代到三叠纪原特提斯-古特提斯洋持续的俯冲—增生造山过程（Dong Yunpeng et al.，2018a，2021，2022a），而东段的南秦岭构造带则记录了古特提斯洋沿勉略缝合带的俯冲碰撞造山作用（图6）（Zhang Guowei et al.，2001; Dong Yunpeng et al.，2011a，2021，2022a; Dong and Santosh，2016）。
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2 中央造山系北部原特提斯造山作用
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中央造山系北部祁连造山带和北秦岭广泛记录了原特提斯造山作用（Dong Yunpeng et al.，2021）。祁连造山带北祁连构造带（蛇绿混杂岩带）、南祁连构造带（增生杂岩带）相当于北秦岭商丹缝合带（蛇绿混杂岩带），代表了原特提斯洋缝合带（图5）。北秦岭构造带为秦岭商丹带早古生代原特提斯洋向北俯冲的活动大陆边缘，二郎坪蛇绿混杂岩带代表了弧后盆地缝合带（Dong Yunpeng et al.，2021）。
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2.1 原特提斯洋扩张
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中央造山带西段的北祁连构造带以广泛分布寒武纪—奥陶纪蛇绿混杂岩、洋岛火山岩、岛弧火山岩和侵入岩以及相关变质记录为特征（Xia Linqi et al.，1996; Feng Yimin，1997; Xiao Wenjiao et al.，2009; Xu Zhiqin et al.，2011; Song Shuguang et al.，2013）。在熬油沟、玉石沟、边马沟、祁连县、老虎山、大岔大坂、九个泉和扁都口等地区（图5），出露有大量代表北祁连洋岩石圈残片的E-MOR或N-MOR型蛇绿岩，主要由橄榄岩、辉长岩、辉绿岩、枕状玄武岩和放射虫硅质岩组成（Hou Qingye et al.，2005; Tseng et al.，2007; Xia Xiaohong et al.，2012; Song Shuguang et al.，2013; Yu Shengyao et al.，2021）。玉石沟蛇绿岩的辉长岩SHRIMP锆石U-Pb年龄为548~529 Ma（Song Shuguang et al.，2013）; 祁连县蛇绿岩中的玄武岩锆石U-Pb年龄为499±6 Ma（Wu Peng et al.，2012）和497±7 Ma（Tseng et al.，2007）; 九个泉和老虎山蛇绿岩中的辉长岩时代分别为490±5 Ma（Xia and Song，2010）和448.5±4.7 Ma（Song Shuguang et al.，2013）; 大岔大坂蛇绿岩中的辉长岩SHRIMP锆石U-Pb年龄为517±4 Ma（Xia Xiaohong et al.，2012）; 扁都口蛇绿岩中的辉长岩时代为479±2 Ma（Song Shuguang et al.，2013）。洋岛玄武岩主要分布于熬油沟地区（Xiao Xuchang et al.，1978; Zhang Zhaochong et al.，2001; Song Shuguang et al.，2013），其SIMS锆石U-Pb年龄为600±7 Ma（Xu Xin et al.，2015），辉长岩SHRIMP锆石U-Pb年龄为501.4±4.3 Ma（Xiang Zhenqun et al.，2007）和495±4 Ma（Song Shuguang et al.，2013）。这些年代学资料约束北祁连洋至少存在于600~448 Ma（图6a、c）。
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南祁连构造带主要由被肢解的早古生代蛇绿岩、俯冲相关火山-沉积岩和少量增生的前寒武纪基底组成（Yan Zhen et al.，2019）。蛇绿混杂岩主要出露于党河南山、大道尔吉、木里和拉脊山（图5）。具E-MOR或N-MOR性质的蛇绿岩主要分布于拉脊山和清水地区，主要岩石组合为蛇纹石化橄榄岩、辉石橄榄岩、辉长岩、块状和枕状熔岩以及少量硅质岩（Hou Qingye et al.，2005; Song Shuguang et al.，2013; Zhang Yuqi et al.，2017; Fu Changlei et al.，2018; Yan Zhen et al.，2019）。拉脊山蛇绿岩中辉长岩的锆石U-Pb年龄为525±3 Ma（Zhang Yuqi et al.，2017），辉绿岩形成时代为491.0±5.1 Ma（Fu Changlei et al.，2014）; 清水蛇绿岩中辉长岩和玄武岩的锆石U-Pb年龄介于534~440 Ma（Pei Xianzhi et al.，2005; Dong Yunpeng et al.，2011b）。这些年龄信息限定南祁连洋至少存在于534~440 Ma期间（图6a、c）。
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图4 秦岭造山带及邻区地质简图（据Dong Yunpeng et al.，2011a修改）
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Fig.4 Tectonic outline of the Qinling Orogen and its adjacent areas (modified from Dong Yunpeng et al., 2011a)
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图5 中央造山系及邻区构造单元区划图以及主要蛇绿岩分布位置（据Dong Yunpeng et al.，2022a修改）
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Fig.5 Simplified tectonic map showing the tectonic division of the Central China Orogenic Belt and adjacent areas, and the locations of the major ophiolites (modified from Dong Yunpeng et al., 2022a)
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N-WKB、C-WKB和S-WKB—分别为西昆仑北带、中带和南带; N-QMTB、 C-EKB和 S-EKB—分别为东昆仑北部祁漫塔格构造带、昆中带和昆南带; NQLB、 CQLB和SQLB—分别为北祁连、中祁连和南祁连构造带; S-NCB、NQB和SQB—分别为华北南缘、北秦岭、南秦岭构造带
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N-WKB, C-WKB and S-WKB—Northern, Central and Southern West Kunlun belts, respectively; N-QMTB, C-EKB and S-EKB—Northern Qimantagh, Central and Southern East Kunlun belts, respectively; NQLB, CQLB and SQLB—Northern, Central and Southern Qilian belts, respectively; S-NCB, NQB, and SQB—southern margin of the North China Block, North and South Qinling belts
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图6 中央造山系西段祁连、昆仑造山带和东段秦岭造山带原-古特提斯构造演化模式图（据Dong Yunpeng et al.，2022a）
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Fig.6 Tectonic models showing the evolutionary history from the Proto-Tethys to Paleo-Tethys across the Qilian and Kunlun Orogens of the western Central China Orogenic Belt, and the Qinling Orogen of the eastern Central China Orogenic Belt (after Dong Yunpeng et al., 2022a)
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QTB、SKL、CKL和QDB一分别为羌塘地块、昆南带、昆中带和柴达木地块; SQLB、CQLB、NQLB和ALT一分别为南祁连构造带、中祁连构造带、北祁连构造带和阿拉善地块; MBAM、 AKM 和QXS一分别为木孜塔格-布青山-阿尼玛卿蛇绿混杂岩带、阿其克库勒湖-昆中蛇绿混杂岩带和祁漫塔格-香日德缝合带; SCB、SQB、NQB和NCB一分别为华南板块、南秦岭构造带、北秦岭构造带和华北板块; MLS、SDS、ELPS和KPS一分别为勉略揵合带、商丹缝合带、二郎坪揵合带和宽坪缝合带
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QTB，SKL，CKL and QDB-Qiangtang Block，South Kunlun Belt，Central Kunlun Belt and Qaidam Block; SQLB，CQLB，NQLB and ALT一Southern Qilian Belt，Central Qilian Belt，Northern Qilian Belt and Alxa Terrane; MBAM，AKM and QXS-Muztagh-Buqingshan-Anemaqen ophiolitic mélange zone，Aqikekulehu-Kunzhong ophiolitic mélange zone and Qimantagh-Xiangride suture; SCB，SQB，NQB and NCB-South China Block，South Qinling Belt，North Qinling Belt and North China Block; MLS，SDS，ELPS and KPS-Mianlue suture，Shangdan suture，Erlangping suture and Kuanping suture
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中央造山带东段的北秦岭商丹缝合带可与北祁连构造带和南祁连构造带对比（Dong Yunpeng et al.，2021）。商丹缝合带含有大量蛇绿混杂岩（图5），主要由一系列断续出露于鸳鸯镇、武山、关子镇、伯阳、唐藏、岩湾、下黑湾、黑河、小王涧、丹凤和信阳地区的蛇绿岩残片和俯冲相关火山岩组成（Zhang Guowei et al.，1995，2001; Dong Yunpeng et al.，2011a，b，2013，2021）。蛇绿岩残片包括具有成熟洋中脊性质的关子镇、小王涧、丹凤资峪N-MOR型蛇绿岩，以及来自过渡或初始扩张洋中脊的武山、鸳鸯镇、岩湾、唐藏E-MOR型蛇绿岩（图5），以不同程度发育变质橄榄岩、辉长岩、（枕状）玄武岩、斜长花岗岩和硅质岩为特征，代表了商丹洋大洋岩石圈的残留（Zhang Guowei et al.，2001; Dong Yunpeng et al.，2011a，2011b; Dong and Santosh，2016）。年代学研究显示，关子镇蛇绿岩中的辉长岩锆石U-Pb年龄为471±1.4 Ma（Yang Zhao et al.，2006）和534±9 Ma（Li Wangye，2008），斜长花岗岩形成于517±8 Ma（Li Wangye，2008）; 岩湾蛇绿岩中的辉长岩锆石 U-Pb年龄为517.8±2.8 Ma（Dong Yunpeng et al.，2011b），玄武岩为483±13 Ma（Chen Junlu et al.，2008）和523±26 Ma（Lu Songnian et al.，2003）。结合丹凤蛇绿岩中玄武岩伴生硅质岩内寒武纪—奥陶纪放射虫化石记录（Cui Zhilin et al.，1995），这些年代学资料约束商丹洋至少在 534~471 Ma已经演化为成熟的大洋（图6b、d）。
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2.2 原特提斯洋俯冲消减
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北祁连洋的俯冲极性仍存在北向（Song Shuguang et al.，2013）、南向（Xiao Wenjiao et al.，2009）或双向（Wu Cailai et al.，2006）的争议。但综合不同岩性单元的时空对比，特别是北祁连构造带残留的SSZ型蛇绿岩残片和高压-低温变质岩，以及北祁连构造带和中祁连构造带内大量的俯冲型花岗岩记录，我们认为北祁连洋更可能是向南俯冲于中祁连地块之下（Dong Yunpeng et al.，2021）。在北祁连构造带，SSZ型蛇绿岩残片主要分布于大岔大坂和扁都口地区（图5），以发育变橄榄岩、辉长岩、玄武岩、安山岩、玻安岩和硅质岩为特征（Zhang Qi et al.，1997; Song Shuguang et al.，2013）。大岔大坂蛇绿岩中的玻安岩锆石U-Pb年龄为505±8 Ma和487±9 Ma（Xia Xiaohong et al.，2012; Song Shuguang et al.，2013）; 扁都口蛇绿岩中的安山岩锆石 U-Pb年龄为479±3 Ma（Guo Zhouping et al.，2015）和460±1 Ma（Yu Jiyuan et al.，2010）。高压-低温变质岩以清水沟、香子沟和百经寺等地区发育的榴辉岩和蓝片岩为特征，原岩包括N-MORB、E-MORB和OIB（Song Shuguang et al.，2013; Yu Shengyao et al.，2017）。榴辉岩的两期变质年龄为502~489 Ma和468~463 Ma（Zhang Jianxin et al.，2007; Yu Shengyao et al.，2017），蓝片岩的两期变质年龄为528~485 Ma和466~462 Ma（Cheng Hao et al.，2016; Yu Shengyao et al.，2017），蓝片岩中多硅白云母的40Ar/39Ar年龄介于462~446 Ma（Zhang Jianxin et al.，1997; Liou et al.，1998; Liu Yongjiang et al.，2006）。结合北祁连构造带和中祁连构造带内天水、景泰、祁连县等地区出露的大量516~460 Ma的俯冲型花岗岩（Song Shuguang et al.，2013; Chen Yuxiao et al.，2014; Yu Shengyao et al.，2015; Zhang Jianxin et al.，2015），上述年代学资料约束北祁连洋南向的俯冲作用至少存在于528~446 Ma期间（图6a、c）。
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南祁连洋向北的俯冲作用形成了南祁连构造带内众多断续分布的SSZ型蛇绿岩、俯冲相关火山岩和侵入岩。SSZ型蛇绿岩分布在大道尔吉和木里地区（图5），主要由蛇纹石化橄榄岩、（堆晶）辉长岩、玄武岩、安山岩、斜长花岗岩和硅质岩组成（Huang Zengbao et al.，2016; Yan Zhen et al.，2019）。大道尔吉蛇绿岩中堆晶辉长岩的 Sm-Nd 等时线年龄为 441±58 Ma（Huang Zengbao et al.，2016）; 木里蛇绿岩中辉长岩的锆石U-Pb年龄为521.9±3.7 Ma（Yan Zhen et al.，2019），斜长花岗岩形成于525.3±3.1 Ma（Yan Zhen et al.，2019）。俯冲相关火山岩和侵入岩以党河南山、木里和拉脊山地区出露的辉长岩、玄武岩、安山岩和安山玢岩为特征，木里辉长岩形成时代为539~453 Ma（Yan Zhen et al.，2019），拉脊山玄武岩年龄为456±2 Ma（Wang Tao et al.，2016）。在南祁连构造带以南的柴北缘，除超高压—高压变质岩外，还保存有大量与俯冲相关的火成岩，以中基性火山岩为主，部分为酸性火山岩和埃达克质岩（Wang Huichu et al.，2003; Shi Rendeng et al.，2004）。代表性的岩石包括滩间山群流纹岩（486±13 Ma; Wu Cailai et al.，2001）、绿梁山变玄武岩（464.2 Ma; Wang Huichu et al.，2003）、赛什腾山变安山岩（514.2±8.5 Ma; Shi Rendeng et al.，2004）和柴北缘岛弧型花岗岩（496~445 Ma; Wu Cailai et al.，2001; Wang Huichu et al.，2005）。综合上述资料共同限定南祁连洋的俯冲至少存在于539~441 Ma（图6a、c）。
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商丹洋于523~420 Ma向北俯冲，一方面在商丹缝合带形成了系列俯冲相关火山岩，另一方面在北秦岭构造带形成了大量的俯冲型辉长岩和花岗岩体，同时，这一俯冲作用也进一步导致了二郎坪弧后盆地的扩开（Dong Yunpeng et al.，2011a，2019，2021; Dong and Santosh，2016）。商丹缝合带俯冲相关火山岩分布于下黑湾、小王涧、黑河等地（图5），岩石类型为玄武岩和玄武质安山岩，时代为523~472 Ma（Lu Songnian et al.，2003; Yan Quanren et al.，2008; Dong Yunpeng et al.，2011b）。北秦岭构造带中俯冲型辉长岩自西向东依次包括鸳鸯镇辉长岩（457±3 Ma; Li Wangye，2008）、关子镇辉长岩（507±3.0 Ma和499±1.8 Ma; Pei Xianzhi et al.，2005）、百花辉长岩（434±1.5 Ma; Pei Xianzhi et al.，2007）、厚畛子辉长岩（475±4 Ma; Liu Junfeng et al.，2007）、拉鸡庙辉长岩（422±7 Ma; Liu Junfeng et al.，2009）和富水辉长岩（514~490 Ma; Lu Songnian et al.，2003; Su Li et al.，2004; Li Huimin et al.，2006）。俯冲相关I型花岗岩以北秦岭西部455~434 Ma的草川铺、阎家店、王家岔、唐藏、涝峪闪长岩-花岗岩（Lu Songnian et al.，2003; Pei Xianzhi et al.，2007; Chen Junlu et al.，2008; Wang Hongliang et al.，2009），以及东部488~420 Ma的丹凤、商南花岗岩（Lu Songnian et al.，2003; Wang Tao et al.，2009）为主要代表。这些同位素年代学研究资料限定商丹洋的北向俯冲至少存在于523~420 Ma（图6b、d、f）。
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商丹洋的持续俯冲导致弧后盆地沿二郎坪一线扩开（图6b、d、f），形成了系列蛇绿岩残片和俯冲相关火山岩（Dong Yunpeng et al.，2011a）。蛇绿岩普遍具E-MOR性质，出露于伯阳、二郎坪等地，岩石类型为枕状玄武岩、块状玄武岩和放射虫硅质岩，时代为448~443 Ma（Li Wangye，2008; Dong Yunpeng et al.，2011a），标定了二郎坪弧后盆地的存在。俯冲相关火山岩主要分布于草凉驿、鹦鸽咀、湾潭和火神庙等地区，以不同程度发育超基性岩、辉长岩、变质玄武岩、安山岩和流纹岩为特征（Zhang Guowei et al.，2001; Yan Quanren et al.，2007; Chen Junlu et al.，2008; Dong Yunpeng et al.，2011a）。草凉驿地区俯冲型玄武岩锆石U-Pb年龄为472±11 Ma（Yan Quanren et al.，2007）; 湾潭地区俯冲型枕状玄武岩锆石U-Pb年龄为467±7 Ma（Lu Songnian et al.，2003）。结合区域509~480 Ma的高压—超高压变质作用（Yang Jingsui et al.，2003; Wang Han et al.，2011; Liu Liang et al.，2013）、侵入二郎坪蛇绿混杂岩带的461~459 Ma西庄河、张家大庄和五垛山I型花岗岩（Guo Cailian，2010; Dong Yunpeng et al.，2011a）及441~436 Ma二郎坪、四棵树、灰池子和漂池S型花岗岩（Li Wuping et al.，2001; Lu Songnian et al.，2003; Wang Tao et al.，2009），上述同位素年代学资料标定二郎坪弧后盆地于509 Ma之前已经打开，经历了509~469 Ma的南向俯冲，并在441~436 Ma最终关闭（图6b、d、f）。
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2.3 原特提斯洋闭合与造山
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北祁连洋的闭合被一系列碰撞型花岗岩、高压-低温变质岩和构造-沉积事件所记录。北祁连构造带和中祁连构造带金佛寺、董家庄、白石崖和托莱南山等地分布的440~415 Ma的碰撞相关二长花岗岩和钾长花岗岩（Tseng et al.，2009; Song Shuguang et al.，2013; Yu Shengyao et al.，2015; Chen Shiyue et al.，2016），指示北祁连洋的关闭应该发生于晚志留世。这一认识与北祁连构造带内洋壳型蓝片岩的俯冲折返和退变质作用时限一致，例如，九个泉地区洋壳型蓝片岩和石榴石角闪岩的多硅白云母40Ar/39Ar年龄为423~410 Ma（Zhang Jianxin et al.，1997; Lin Yihui et al.，2010）。考虑到上泥盆统老君山群造山磨拉石角度不整合覆盖于北祁连构造带早古生代单元之上（Dong Yunpeng et al.，2021），上述资料印证了北祁连洋在晚志留世—早泥盆世闭合（图6e）。
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南祁连构造带南侧柴北缘构造带高压—超高压变质岩研究表明，祁连与柴达木之间在早古生代经历了大洋关闭、大陆的深俯冲及超高压变质岩石折返过程（Song Shuguang et al.，2014）。柴北缘高压—超高压变质岩以出露于鱼卡、绿梁山和锡铁山等地的榴辉岩、含柯石英片麻岩和石榴石橄榄岩为代表（Mattinson et al.，2007; Zhang Jianxin et al.，2010; Song Shuguang et al.，2014）。含柯石英片麻岩和石榴橄榄岩超高压变质时代为430~420 Ma（Song and Yang，2001; Xiong Qing et al.，2012; Song Shuguang et al.，2014），并于400 Ma发生折返（Song Shuguang et al.，2014），记录了南祁连洋的关闭过程。结合上泥盆统牦牛山组磨拉石覆盖于上述单元之上等证据，推断南祁连洋同样于晚志留世—早泥盆世关闭（图6e）。
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秦岭造山带原特提斯商丹洋的闭合被证明发生在早泥盆世（Dong Yunpeng et al.，2011a，2021; Dong and Santosh，2016），但也有一些学者认为商丹洋的闭合以北秦岭不同区段的 514~485 Ma的高压—超高压变质岩所记录的陆壳俯冲为标志（Yang Jingsui et al.，2002; Chen Danling et al.，2004; Liu Liang et al.，2009，2013，2016）。然而考虑到这些所谓的高压—超高压变质岩石主要出露于商丹缝合带北侧的秦岭岛弧基底岩系中，而且商丹缝合带内还存在更为年轻的蛇绿岩记录、北秦岭大量523~420 Ma俯冲相关的岩浆作用，以及至今未见深俯冲上覆板块，我们认为北秦岭514~485 Ma的高压—超高压变质岩可能仅是商丹洋内微陆块俯冲的产物（Dong Yunpeng et al.，2021）。相比之下，北秦岭构造带内广泛分布的420~400 Ma的S型花岗岩（Zhang Hongfei et al.，1996; Li Wuping et al.，2001; Dong Yunpeng et al.，2011a）、南秦岭中上泥盆统双向物源的碎屑锆石年龄、中泥盆统与下伏地层间明显沉积间断（Dong Yunpeng et al.，2013）以及南北秦岭的差异变质变形和隆升历史（Liu Guohui et al.，1993; Dong Yunpeng et al.，2018b），共同限定商丹洋的关闭应发生于早泥盆世（图6f、h）。
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3 中央造山系南部西段:原-古特提斯昆仑洋连续增生造山
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中央造山系南部东段和西段具有不同的原特提斯、古特提斯造山作用与过程（图6）。西段的东昆仑造山带表现为北羌塘和柴达木地块之间连续演化的原特提斯-古特提斯洋北向俯冲—增生造山过程（Dong Yunpeng et al.，2018a，2019，2021），而东段则以志留纪—三叠纪南秦岭构造带与华南板块之间的古特提斯勉略洋的扩张-关闭为特征（Dong Yunpeng et al.，2011a; Dong and Santosh，2016）。
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3.1 原-古特提斯昆仑洋
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东昆仑造山带保存有原-古特提斯洋长期俯冲、增生、闭合的地质记录（Dong Yunpeng et al.，2018a）。现有的研究揭示，代表东昆仑地区主大洋的昆仑洋最早可能形成于新元古代罗迪尼亚超大陆裂解，并最晚于早古生代开始持续向北俯冲，形成了早古生代的沟-弧-盆体系（Dong Yunpeng et al.，2018a，2019，2021; Pei Xianzhi et al.，2018）。虽然以祁漫塔格-香日德蛇绿混杂岩为表征的弧后盆地在早泥盆世前关闭，但作为原特提斯洋主体的昆仑洋却演化为古特提斯洋，在短暂停歇之后继续俯冲至早三叠世。这一连续的演化过程，自北向南分别形成了阿其克库勒湖-昆中蛇绿混杂岩带、木孜塔格-布青山-阿尼玛卿蛇绿混杂岩带及两者之间的昆南增生杂岩带（Dong Yunpeng et al.，2018a）。
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阿其克库勒湖-昆中蛇绿混杂岩带在长石山、清水泉和可可科特地区断续出露代表过渡洋中脊的E-MOR型蛇绿岩残片（图5），岩石组合主要为蛇纹岩、辉长岩、辉绿岩、块状和枕状玄武岩，局部伴生少量放射虫硅质岩，代表了昆仑洋古老大洋岩石圈的残片（Yang Jingsui et al.，1996; Wang Guocan et al.，1999; Bian Qiantao et al.，2002; Li Huaikun et al.，2006; Li Rongshe et al.，2008; Wei Bo，2015; Qi Xiaopeng et al.，2016）。同位素年代学研究显示，长石山蛇绿岩中的辉长岩锆石U-Pb年龄为509±6.8 Ma（Feng Jianyun et al.，2010）和537±3.5 Ma（Qi Xiaopeng et al.，2016）; 清水泉蛇绿岩中的辉长岩和玄武岩年龄介于481~422 Ma（Yang Jingsui et al.，1996; Lu Songnian，2002; Li Huaikun et al.，2006; Wei Bo，2015），辉绿岩年龄为436±1.2 Ma（Ren Junhu et al.，2009）。这些年代学资料限定昆仑洋至少在537~436 Ma期间已经演化为成熟的大洋（图6a、c、e）。
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木孜塔格-布青山-阿尼玛卿蛇绿混杂岩带发育N-MOR型蛇绿岩残片和洋岛玄武岩（Dong Yunpeng et al.，2018a; Yue Yuangang，2022）。N-MOR型蛇绿岩残片主要分布于德尔尼和布青山等地区，岩石类型包括蛇纹石化橄榄岩、条带状堆晶及块状辉长岩、辉绿岩（墙）、块状辉长岩、枕状及块状玄武岩、斜长岩及放射虫硅质岩等（Yang Jingsui et al.，1996; Bian Qiantao et al.，2002; Li Ruibao et al.，2015; Pei Xianzhi et al.，2018; Yue Yuangang et al.，2022）。德尔尼蛇绿岩的玄武岩SHRIMP锆石U-Pb年龄为308±4.9 Ma（Yang Jingsui et al.，2004），布青山地区得力斯坦蛇绿岩的辉长岩锆石U-Pb年龄为467±0.9 Ma（Bian Qiantao et al.，2004）和516±6.3 Ma（Liu Zhanqing et al.，2011），哈尔郭勒蛇绿岩的辉长岩和辉绿岩锆石 U-Pb年龄分别为333±3.1 Ma（Pei Xianzhi et al.，2018）和303±3 Ma（Yue Yuangang et al.，2022）。洋岛玄武岩主要分布于布青山地区的玛积雪山、哈尔郭勒和哥日卓托地区（Dong Yunpeng et al.，2018a; Yue Yuangang，2022）。哈尔郭勒洋岛玄武岩锆石U-Pb年龄为341±3 Ma（Yang Jie et al.，2014），苦海地区与洋岛玄武岩地球化学特征类似的辉长岩SHRIMP锆石U-Pb年龄为555±9 Ma（Li Wangye et al.，2007）。结合蛇绿岩中硅质岩内早石炭世—二叠纪放射虫化石记录（Chang Chengfa et al.，1986; Jiang Chunfa et al.，1992; Lan Chaoli et al.，2002; Sun and Ma，2002），上述同位素年代学结果限定昆仑洋的扩张过程至少存在于早古生代到二叠纪，具有原特提斯、古特提斯连续演化的性质（图6a、c、e、g、i）。
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3.2 原-古特提斯昆仑洋两阶段俯冲
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昆仑洋经历早古生代—早泥盆世和早石炭世—三叠纪两阶段北向俯冲，一方面形成了阿其克库勒湖-昆中蛇绿混杂岩带和木孜塔格-布青山-阿尼玛卿蛇绿混杂岩带中的SSZ型蛇绿岩和相关火山岩、以及昆中构造带中的大量俯冲型辉长岩-花岗岩体，另一方面导致弧后盆地沿祁漫塔格-香日德缝合带开合（Dong Yunpeng et al.，2018a，2019）。
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沿阿其克库勒湖-昆中蛇绿混杂岩带，SSZ型蛇绿岩残片主要分布于曲什昂、清水泉、塔妥、阿此特、阿其克库勒湖、温泉和乌妥等地（图5），以不同程度发育变橄榄岩、辉长岩、玄武岩、斜长花岗岩和少量放射虫硅质岩为特征（Zhu Yunhai et al.，1999; Dong Yunpeng et al.，2018a; Li Ruibao et al.，2021）。曲什昂蛇绿岩的辉长岩锆石U-Pb年龄为504±5.5 Ma（Wei Bo，2015），塔妥蛇绿岩中的辉长岩和斜长花岗岩锆石U-Pb年龄介于504~490 Ma（Dong Yunpeng et al.，2018a），清水泉蛇绿岩中辉长岩锆石 U-Pb年龄为486±1 Ma（Li Ruibao et al.，2021）。温泉地区辉石岩形成于331±2 Ma（Jia Lihui et al.，2018），乌妥蛇绿岩中的辉长岩锆石 U-Pb 年龄为243±1.4 Ma（Dong Yunpeng et al.，2018a）。结合蛇绿岩中硅质岩夹层的石炭纪—二叠纪放射虫化石记录（Zhu Yunhai et al.，2002），这些同位素年代学资料限定阿其克库勒湖-昆中蛇绿混杂岩带的SSZ型蛇绿岩主要形成于早古生代，少量形成于晚古生代—中三叠世（图6a、c、e、g、i）。
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木孜塔格-布青山-阿尼玛卿蛇绿混杂岩带中的SSZ型蛇绿岩残片和俯冲相关火山岩由蛇纹岩、蛇纹石化橄榄岩、辉石岩、（堆晶）辉长岩、辉绿岩墙、玄武岩、斜长花岗岩及放射虫硅质岩组成，主要分布于木孜塔格地区（Molnar et al.，1987; Pan Yusheng，1989; Lan Chaoli et al.，2002; Wu Jun et al.，2005; Zhang Xiangxin et al.，2009）。在硅质岩夹层中，存在早石炭世（Lan Chaoli et al.，2002）和二叠纪（Sun and Ma，2002; Li Weidong et al.，2003）放射虫化石。此外，在布青山地区俯冲相关的流纹斑岩获得438±3 Ma的锆石U-Pb年龄（Liu Zhanqing et al.，2011）。上述同位素年代学资料限定昆仑洋沿木孜塔格-布青山-阿尼玛卿缝合带存在志留纪到二叠纪的长期俯冲过程（图6a、c、e、g、i）。
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昆仑洋向北的两阶段俯冲消减作用（图6a、c、e、g、i、k）形成了昆中构造带470~400 Ma和270~200 Ma两期俯冲相关的侵入体和火山岩（Dong Yunpeng et al.，2018a）。前者主要以452~438 Ma的清水泉角闪辉长岩（Sang Jizhen et al.，2016）和胡晓钦角闪辉绿岩（Liu Bin et al.，2013），474~420 Ma的哈日扎、沟里、埃坑德勒斯特和五龙沟I型闪长岩、花岗岩（Dong Yunpeng et al.，2018a）为代表; 后者主要包括270~250 Ma与板片俯冲相关的辉长岩、闪长岩和花岗岩，250~240 Ma与板片撕裂相关的具暗色包体的花岗闪长岩，240~220 Ma与底侵作用相关的石英闪长岩、花岗闪长岩、二长花岗岩和正长花岗岩以及鄂拉山玄武质-长英质火山岩，220~200 Ma与弧内伸展相关的石英闪长岩、斜长花岗岩、英云闪长岩、正长花岗岩和基性岩墙（Dong Yunpeng et al.，2018a）。此外，在昆南构造带，两阶段俯冲造山作用还被一系列深成岩体所记录，包括441~408 Ma的俯冲型闪长岩、花岗闪长岩和石英闪长岩，454~402 Ma俯冲板片重熔成因的埃达克质花岗闪长岩、石英闪长岩和花岗岩，448~447 Ma与加厚地壳相关的埃达克质二长花岗岩和黑云母花岗岩，424~421 Ma增生杂岩深熔作用形成的石英闪长岩和花岗闪长岩（Dong Yunpeng et al.，2018a），以及260~257 Ma增生杂岩重熔而成的二云母花岗岩（Ren Xiang et al.，2022）。
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昆仑洋向北的持续俯冲导致弧后盆地沿祁漫塔格-香日德缝合带扩开（图6c），在黑山、鸭子达坂、鸭子泉、十字沟、长沟和乌图美仁地区出露有一系列代表弧后大洋岩石圈残余的E-MOR型蛇绿岩残片（图5），以发育蛇纹岩、橄榄辉石岩、（堆晶）辉石岩、（堆晶）辉长岩、玄武岩和少量放射虫硅质岩为特征（Li and Jun，1998; Chen Junlu et al.，2004; Li Rongshe et al.，2008; Song Taizhong et al.，2010; Meng Fancong et al.，2015; Du Wei et al.，2017; Dong Yunpeng et al.，2019）。黑山蛇绿岩中的辉长岩锆石U-Pb年龄为486±6 Ma（Meng Fancong et al.，2015），鸭子泉蛇绿岩中的辉绿岩锆石U-Pb年龄为421.5±2.2 Ma（Dong Yunpeng et al.，2019），十字沟蛇绿岩中的玄武岩和辉绿岩全岩Sm-Nd年龄介于468~442 Ma（Li Rongshe et al.，2008; Song Taizhong et al.，2010），长沟蛇绿岩中的辉长岩锆石 U-Pb年龄为431±4.1 Ma（Dong Yunpeng et al.，2018a）。这些同位素年代学研究资料限定祁漫塔格弧后盆地洋盆至少存在于486~420 Ma（图6c、e）。祁漫塔格弧后盆地的北向俯冲形成了祁漫塔格-香日德蛇绿混杂岩带以及北祁漫塔格构造带中系列俯冲相关侵入岩和火山岩（Dong Yunpeng et al.，2018a，2019）。祁漫塔格-香日德蛇绿混杂岩带中相关岩石包括鸭子泉闪长岩（480±3 Ma; Cui Meihui et al.，2011）、鸭子泉中基性火山岩（418±3 Ma; Wang Xiangli et al.，2010）和夏日哈木超镁铁质-镁铁质杂岩（439~423 Ma; Wang Guan et al.，2014; Jiang Changyi et al.，2015; Peng Yuan et al.，2016）。北祁漫塔格构造带中则以445~439 Ma的祁漫塔格群火山岩（Li Rongshe et al.，2008）和460~425 Ma的俯冲型闪长岩、二长花岗岩和黑云母花岗岩（Li Wei et al.，2013; Dong Yunpeng et al.，2018a）为代表。北祁漫塔格构造带中425~420 Ma的同碰撞二长花岗岩、正长花岗岩（Li Guochen et al.，2012; Zheng Zhen et al.，2016），420~390 Ma的碰撞后A型花岗闪长岩、黑云母花岗岩和钾长花岗岩（Song Zhongbao et al.，2014; Zhang Jianxin et al.，2015），以及昆中构造带与柴达木地块相似的基底性质（He Dengfeng，2016）、夏日哈木和温泉榴辉岩428~411 Ma的峰期变质年龄（Qi Shengsheng et al.，2014; Meng Fancong et al.，2015）和中泥盆统牦牛山组磨拉石建造（Dong Yunpeng et al.，2018a），共同限定祁漫塔格弧后盆地于425~420 Ma关闭，并在420~390 Ma发生造山后伸展垮塌（图6e、g）。
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3.3 昆南带增生作用与弧前沉积
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昆仑洋持续的北向俯冲在阿其克库勒湖-昆中蛇绿混杂岩带和木孜塔格-布青山-阿尼玛卿蛇绿混杂岩带之间形成了宽广的昆南增生杂岩带，主要由广泛分布的不连续的古生代—三叠纪火山-沉积建造、少量古元古代高级变质基底岩系（苦海群）和新元古代火山-沉积岩系（万宝沟群）组成（Dong Yunpeng et al.，2018a）。
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奥陶纪—志留纪火山-沉积序列以纳赤台群为代表，形成于弧前构造环境（Dong Yunpeng et al.，2018a）。岩石类型主要为变质火山岩和火山碎屑岩、杂砂岩、深水浊积岩和少量碳酸盐岩。变质基性火山岩具有俯冲相关特征，时代为474±7.9 Ma（Chen Youxin et al.，2013），变质酸性火山岩锆石U-Pb年龄则介于468~450 Ma（Feng Chengyou et al.，2005），杂砂岩最大沉积时限为538 Ma（Jin Lijie et al.，2015），侵入杂砂岩中的英安斑岩锆石U-Pb年龄为425.9±2.6 Ma（Zhou Chunjing et al.，2010）。这些年龄信息限定纳赤台群主要形成于奥陶纪，少部分可能延续至早志留世。同时，不连续的志留系赛什塘组、中泥盆统布拉克巴什组、下石炭统哈拉郭勒组、上石炭统—下二叠统浩特洛洼组、下二叠统树维门科组、中-下二叠统马尔争组、上二叠统格曲组、中-下三叠统洪水川组、中三叠统闹仓坚沟组以不整合或断层相互接触（Li Rongshe et al.，2008; Yue Yuangang，2022），属于俯冲过程中弧前盆地中的不连续的沉积-增生杂岩（Dong Yunpeng et al.，2018a）。上三叠统八宝山组磨拉石覆盖于上述地层之上，代表了昆南构造带中强烈的晚三叠世造山运动（Dong Yunpeng et al.，2018a）。
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上述所有的蛇绿岩、俯冲相关侵入岩和火成岩、沉积建造等不同构造单元的资料，标定昆南构造带是古生代—三叠纪长期存在的弧前增生杂岩带，指示昆仑洋早期沿阿其克库勒湖-昆中缝合带向北俯冲、后期俯冲后撤至木孜塔格-布青山-阿尼玛卿缝合带（Dong Yunpeng et al.，2021）。考虑到昆南构造带南侧松潘-甘孜构造带广泛分布的三叠系巴颜喀拉群深水浊积岩，残留的昆仑洋在三叠纪可能仍然不断被碎屑物质充填（Dong Yunpeng et al.，2018a，2021）。
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4 中央造山系南部东段:古特提斯秦岭勉略洋俯冲碰撞造山
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中央造山系南部东昆仑地区昆南缝合带向东延伸至秦岭地区勉略缝合带，以一系列裂谷相关火山岩、被肢解的蛇绿岩残片、俯冲型火山岩和高温高压变质岩为代表，记录了晚古生代至中三叠纪南秦岭和华南之间古特提斯勉略洋的打开和关闭过程（Zhang Guowei et al.，2001，2003，2004; Dong Yunpeng et al.，2011a，2021; Dong and Santosh，2016）。
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4.1 古特提斯勉略洋初始扩张
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南秦岭与扬子北缘具有相同的震旦纪—奥陶纪沉积建造，指示南秦岭原为扬子北缘的组成部分（Dong and Santosh，2016）。勉略洋的初始扩张（图6f）主要以略阳黑沟峡、勉县和大洪山地区志留纪裂谷型双峰式火山岩（包括碱性玄武岩、英安岩及流纹岩）（Li Shuguang et al.，1996; Dong Yunpeng et al.，1999a，b）、以及南秦岭—大巴山地区志留纪伸展相关碱性辉绿岩墙为代表（Zhang Fangyi et al.，2020）。洋盆成熟后形成了一系列MOR型蛇绿岩残片，断续出露于康县、琵琶寺、南坪、庄科、安子山和勉略等地区（图5），具有超基性岩、堆晶辉长岩、辉绿岩墙和玄武岩的岩石组合（Zhang Guowei et al.，1995，2001，2004; Li Shuguang et al.，1996; Xu Jifeng et al.，2000; Lai Shaocong et al.，2002，2004）。蛇绿岩内硅质岩夹层中的放射虫化石时代为泥盆纪—石炭纪（Lai and Yang，1995; Feng Qinglai et al.，1996），表明勉略洋至少在泥盆纪—石炭纪已逐步扩张演变为成熟的大洋（图6h、j）。南秦岭晚古生代—早中生代地层古地磁研究显示，早泥盆世、早石炭世和早三叠世南秦岭的古纬度分别为 9.4°N、1.5°S 和 23.6°N，与华北同时代古地磁数据相仿，而与华南明显不同，表明晚古生代—早三叠世南秦岭、北秦岭及华北已经沿商丹缝合带碰撞拼接，而与华南之间仍以勉略洋相隔（Zhao Jie et al.，2020）。这些证据标定了分隔南秦岭和华南的勉略洋至少在泥盆纪—早三叠世时期存在（图6h、j）（Zhang Guowei et al.，1995，2001，2004; Dong Yunpeng et al.，2011a，2021）。
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4.2 勉略洋俯冲消减
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勉略洋于300~220 Ma向北俯冲，在勉略缝合带和南秦岭构造带分别形成了大量的俯冲相关火山岩、辉绿岩和花岗岩体（图5），包括三岔子高镁安山岩、斜长岩和辉绿岩（Xu Jifeng et al.，2000; Li Shuguang et al.，2004），巴山两河-饶峰-石泉-高川-五里坝弧内裂陷双峰式火山岩和陆缘岛弧安山岩（Lai Shaocong et al.，2000），南秦岭构造带俯冲相关I型花岗岩（Dong Yunpeng et al.，2011a，2021; Dong and Santosh，2016）。三岔子斜长岩锆石U-Pb年龄为300±61 Ma（Li Shuguang et al.，2004），辉绿岩锆石U-Pb年龄为295~264 Ma（Lai and Qin，2010）; 南坪安山岩获得了锆石U-Pb年龄246±3 Ma（Qin Jiangfeng et al.，2008）; 南秦岭俯冲型花岗岩锆石U-Pb年龄为245~220 Ma（Qin Jiangfeng et al.，2007，2009; Dong Yunpeng et al.，2011a，2012; Liu Renyan et al.，2011; Yang Pengtao et al.，2012）。这些火山岩和侵入岩的同位素年代学和地球化学资料共同限定勉略洋的俯冲至少存在于300~220 Ma（图6h、j、l）。
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4.3 勉略洋关闭与秦岭全面造山
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南秦岭构造带220~210 Ma同碰撞花岗闪长岩-英云闪长岩-花岗岩和210~200 Ma后碰撞环斑花岗岩（Qin Jiangfeng et al.，2008; Zhang Chengli et al.，2008; Gong Hujun et al.，2009）指示勉略洋的关闭应该发生于晚三叠世（图6l）。这一推论与勉略缝合带内洋壳型和陆壳型麻粒岩的俯冲折返和变质作用时限相吻合。例如，勉略带官地坪含刚玉片麻岩近峰期变质年龄为227 Ma，长坝麻粒岩峰期变质年龄为236 Ma，长坝、王家沟麻粒岩角闪岩相退变质年龄为208 Ma（Liao Xiaoying et al.，2021）; 安子山的洋壳型高压基性麻粒岩40Ar/39Ar年龄为199~192 Ma，代表碰撞后的隆升年龄（Li Sanzhong et al.，2000; Zhang Zongqing et al.，2002）。在桐柏—大别地区，同时发育一系列高压—超高压榴辉岩，峰期变质年龄为245~220 Ma（Liu Fulai et al.，2004，2006; Zhao Zifu et al.，2006，2008; Cheng Hao et al.，2008），退变质年龄为218~205 Ma（Liu Fulai et al.，2006），也记录了三叠纪南秦岭和华南之间的俯冲-碰撞作用。另外，勉略缝合带南侧前陆冲断褶皱带只卷入中三叠世地层（Zhang Guowei et al.，2004），其上不整合覆盖早—中侏罗世陆相断陷盆地型沉积地层（如紫阳瓦房店、房县青峰等地）（Liu Shaofeng et al.，1999; Zhang Guowei et al.，2004），以及荆州晚三叠世—中侏罗世前陆盆地磨拉石建造等（Dong Yunpeng，1997; Dong Yunpeng et al.，2011a），从构造和沉积方面印证了勉略洋在晚三叠世之前闭合。此后，秦岭造山带全面转入陆内造山过程。
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5 中央造山系晚中生代—新生代陆内造山
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中央造山系西段的祁连造山带在原特提斯洋关闭后迅速转为晚泥盆世伸展塌陷的动力学背景，广泛沉积了大量的石炭系—三叠系砂岩和碳酸盐岩，并被侏罗系河湖相含煤建造所覆盖; 而东昆仑造山带北部保留了原特提斯造山记录，南部则记录了原特提斯和古特提斯连续的增生造山过程，并在晚三叠世后转换为碰撞后伸展塌陷的构造背景（Dong Yunpeng et al.，2022a），以发育少量上三叠统火山-沉积岩，以及大量中—下侏罗统陆相碎屑岩与煤层互层为主要特征。这些地质事实显示，中央造山系西段北部、南部分别在晚志留世—早泥盆世、晚三叠世先后转化为新的陆内构造演化时期（Dong Yunpeng et al.，2022a）。在晚三叠世之后，整个中央造山系西段进入大规模陆内造山阶段，导致巴颜喀拉群等前侏罗纪地层、侏罗纪陆相沉积地层发生强烈的逆冲褶皱变形（Dong Yunpeng et al.，2022a）。同时，南北羌塘地块广泛分布的海相侏罗系火山岩、碎屑岩和碳酸盐岩揭示，海水已经向南退却至羌塘地区（Li Cai et al.，2008）。新生代以来，由于印度-欧亚陆陆碰撞导致青藏高原的隆升和广泛的构造叠加改造，中央造山系西段晚中生代的相关地质作用和精细过程仍有待进一步筛分和思考。
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在中央造山系东段的秦岭造山带，中—晚三叠世沿勉略缝合带的碰撞作用使整个秦岭造山带进入大规模陆内造山阶段，以晚侏罗世—早白垩世巨大的陆内俯冲、陆壳收缩叠置为特征（Zhang Guowei et al.，2001，2004; Dong Yunpeng et al.，2011a，2016）。中—晚三叠世，南秦岭构造带和北秦岭构造带具有差异的演化特征。南秦岭构造带的前中三叠世地层广泛发育与南秦岭、华南主碰撞同期的前陆冲断褶皱变形（Dong Yunpeng et al.，2008，2016），并逆冲推覆叠置于华南北缘晚三叠世前陆盆地磨拉石之上（Dong Yunpeng，1997; He Jiankun et al.，1997）。相比之下，在北秦岭构造带，沿着边界断裂带的断陷盆地中发育上三叠统碎屑岩，指示局部伸展的构造背景（Dong Yunpeng et al.，2016; Dong and Santosh，2016）。在早—中侏罗世，南秦岭与华南印支期碰撞后的持续挤压，使得沿主要边界断裂带发育走滑断裂，形成了一系列拉分盆地，充填陆相红层和砾岩，并以角度不整合覆盖于强烈变形的前中三叠世地层之上（Dong Yunpeng et al.，2008，2016）。在南秦岭构造带南侧的大巴山地区，逆冲前锋不断向南扩展，前陆盆地强烈挠曲沉降（Dong Yunpeng，1997; He Jiankun et al.，1997）。
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在晚侏罗世—早白垩世，秦岭造山带北侧大量地球物理资料（Yuan Xuecheng，1996）和测井数据（Zhang Guowei et al.，2001; Shi Rendeng et al.，2004）显示，华北岩石圈沿秦岭造山带北缘的宝鸡-鲁山-舞阳边界断裂发生向南陆内俯冲作用，形成秦岭北缘广泛发育的150~100 Ma早白垩世火山岩和侵入岩（Mao Jingwen et al.，2005; Ye Huishou et al.，2006; Dong Yunpeng et al.，2011a），以及大量的金、钼等矿床（Du Andao et al.，1994; Li Nuo et al.，2008; Zhu Laimin et al.，2008）。在南秦岭地区，华南岩石圈沿巴山弧形断裂带持续向北部的秦岭造山带之下陆内俯冲，使得前陆不断逆冲扩展（Dong Yunpeng et al.，2016）。由于南、北向的陆内相向俯冲，秦岭造山带在晚侏罗世—早白垩世不断抬升并向外逆冲推覆于华南、华北之上，总体呈现出扇型造山带的几何学特征（Zhang Guowei et al.，2001; Dong Yunpeng et al.，2016）。晚白垩世—古近纪时期，秦岭造山带转化为伸展塌陷的背景，沿主干断裂形成了山阳、漫川关、西峡等多个断陷盆地（Zhang Guowei et al.，2001; Dong Yunpeng et al.，2016）。
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新生代，在太平洋板块向西俯冲、印度板块向北碰撞以及西伯利亚板块向南抵挡的三面围限作用下，中国大陆中部的中央造山系发生了强烈的构造活动，突出地表现为约45~40 Ma至约25 Ma和约10 Ma以来的快速隆升剥露，而秦岭北侧渭河地堑则相应地发生强烈伸展断陷，沉积了＞7 km 的巨厚沉积物。这标志着中央造山系在深部的地质作用及其动力学驱动下，浅表构造地貌发生了多阶段差异隆升，终于造就了现今复杂、多样的中央造山系地貌特征。
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致谢:谨以此文纪念中国地质学会成立100周年暨《地质学报》创刊100周年。
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摘要
中国中央造山系是由亲劳亚的北方陆块群、亲冈瓦纳的南方陆块群及其间大量过渡性微陆块历经复杂拼合而成的复合型造山带,是中国大陆完成主体拼合的构造结合带。中央造山系自西而东包括昆仑造山带、祁连造山带和秦岭-大别造山带,保存了古生代—早中生代时期华北、华南、柴达木、塔里木、羌塘等众多大小陆块造山过程的丰富信息,是研究东特提斯构造域原、古特提斯洋构造演化的重要窗口。本文综述了中央造山系地质、地球化学和高精度年代学等多学科研究成果,得到以下主要认识:① 550 Ma之前,众多大小陆块孤立散布于原特提斯洋;② 541~485 Ma,原特提斯洋各分支开始俯冲;③ 485~444 Ma,原特提斯洋持续俯冲,导致秦岭二郎坪弧后盆地、昆仑祁漫塔格弧后盆地打开;④ 444~420 Ma,原特提斯北祁连洋、南祁连洋和商丹洋闭合,昆仑祁漫塔格弧后盆地关闭;⑤ 420~300 Ma,昆仑地区古特提斯洋继承原特提斯洋,古特提斯勉略洋逐步扩张;⑥ 300~250 Ma,昆仑洋自阿其克库勒湖-昆中缝合带向木孜塔格-布青山-阿尼玛卿缝合带发生俯冲后撤;⑦ 250~200 Ma,原-古特提斯昆仑洋、古特提斯勉略洋关闭;⑧ 200 Ma以来,中央造山系转入陆内造山阶段。
Abstract
The Central China Orogenic Belt is a compound orogenic belt formed by the complex amalgamation of many Laurasia-associated northern blocks, Gondwana-associated southern blocks, and many transitional micro-blocks in-between. It is a tectonic combination zone where the main body of mainland China has been assembled. The Central China Orogenic Belt includes, from west to east, the Kunlun Orogen,Qilian Orogen, and Qinling-Dabie Orogen, and preserves abundant information on the Paleozoic-Early Mesozoic orogenic processes of North China, South China, Qaidam, Tarim, and Qiangtang Blocks. It offers a critical window to study the tectonic evolution from Proto-Tethys to Paleo-Tethys Oceans in the East Tethys tectonic domain. This contribution reviews the geological, geochemical and high-precision geochronology dataset from the Central China Orogenic Belt, and draws the following main conclusions: ① Before 550 Ma, many large-small-sized blocks were isolated and scattered in the Proto-Tethys Ocean; ② During 541~485 Ma, all branches of the Proto-Tethys Ocean began to subduct; ③ During 485~444 Ma, the Proto-Tethys Ocean continued to subduct, resulting in the opening of the Erlangping back-arc basin in the Qinling area and the Qimantagh back-arc basin in the Kunlun area; ④ During 444~420 Ma , the Paleo-Tethys North Qilian, South Qilian, and Shangdan Oceans and Qimantagh back-arc basin were closed; ⑤ At 420~300 Ma, the Paleo-Tethys Ocean inherited the Proto-Tethys Ocean in the Kunlun area, and the Paleo-Tethys Mianlue Ocean gradually spread; ⑥ During 300~250 Ma, the Kunlun Ocean subducted and retreated from the Aqikekulehu-Kunzhong suture to the Muztagh-Buqingshan-Anemaqen suture; ⑦ During 250~200 Ma, the Proto- and Paleo-Tethys Kunlun Ocean and the Paleo-Tethys Mianlue Ocean were closed; ⑧ Since 200 Ma, the Central China Orogenic Belt transitioned into intracontinental orogeny.
