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特提斯（Tethys），又名特提斯洋（Tethys Ocean），或特提斯海（Tethys Sea），是一个较为古老的地质概念。它由奥地利地质学家Eduard Suess于1893年提出，指存在于三叠纪—侏罗纪期间，北方安加拉大陆（Angara）与南方冈瓦纳大陆（Gondwana）之间的残留海（Suess，1893）。后来，随着研究的深入，特提斯构造域演化阶段划分也相应发生变化。Stöcklin（1974）、Sengör（1979）将最初Suess命名的特提斯“两分”，晚三叠世—中侏罗世以前的特提斯称作古特提斯洋（Paleo-Tethys），以后的特提斯称作新特提斯洋（Neo-Tethys）。目前，一般定义古特提斯为晚古生代形成的大洋，这样，学者们就把特提斯范围内存在的更古老大洋称之为原特提斯或始特提斯（Proto-Tethys）（潘裕生，1989；刘增乾等，1993；潘桂棠，1994；李兴振等，1995；李三忠等，2016a），并进一步综合厘定出特提斯演化三阶段划分方案（潘桂棠等，1997；潘裕生等，1998），即原特提斯阶段（Proto-Tethys，震旦纪—志留纪）、古特提斯阶段（Paleo-Tethys，泥盆纪—中三叠世）和新特提斯阶段（Neo-Tethys，晚三叠世—始新世）。
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作为特提斯构造运动的起始，原特提斯洋是研究特提斯地球动力学的重要切入点。李三忠等（2016a，2016b）界定原特提斯洋为“起始于新元古代，闭合于早古生代末期，位于塔里木-华北陆块以南，滇缅马苏/保山微陆块以北，与Rodinia超大陆的裂解密切相关的一个古洋盆”，内有众多陆块/微陆块弥散分布（如华夏、扬子、柴达木、欧龙布鲁克及中祁连等）。多数学者认同原特提斯洋的闭合发生在约440~410 Ma（Song Shuguang et al.，2014; Yu Shengyao et al.，2015; Li Sanzhong et al.，2018; Dong Yunpeng et al.，2021; Yu Shengyao et al.，2021; Dong Yunpeng et al.，2022），但是对原特提斯是小洋盆还是大洋，是Rodinia超大陆解体以来就存在还是早古生代才发生、发展的，以及内部多个陆块/微陆块之间新元古代—早古生代亲缘性和拼合问题仍存在争议（李兴振等，1995；葛肖虹等，2000；陆松年等，2002；Stampfli et al.，2002；李三忠等，2016a，2016b；Zhao Guochun et al.，2018），这直接限制了对原特提斯洋整体形成演化历史这一关键科学问题的研究。
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目前，关于原特提斯洋的起源认识仍分歧较大，主要有4种不同的解释：① 新元古代Rodinia超大陆解体至早古生代发育原特提斯洋（潘桂棠等，2012；李三忠等，2016a；Li Sanzhong et al.，2018；Zhao Guochun et al.，2018；Dong Yunpeng et al.，2021；王立全等，2021）；② 吴福元等（2020）基于蛇绿岩的研究认为，原特提斯可能由多个小洋盆组成，整个洋存在的时间约为100 Ma，它在520~480 Ma形成后很快就进入消亡期；③ 原特提斯洋的打开是穿时的，有一部分前寒武纪块体可能在Rodinia解体时从冈瓦纳大陆分离，而一些块体泛非造山期以后（530 Ma）才从冈瓦纳大陆分开（Teng Xia et al.，2020；张建新等，2021）；④ 原特提斯构造域内昆仑-祁连-秦岭的小洋盆-微陆块体系并不是从新元古代延续到早古生代，而是古中国地台解体后才产生的早古生代海底裂谷系（任纪舜，2004）。由此可见，原特提斯构造域内众多陆块/微陆块所保存的新元古代—早古生代地质事件的性质亟需进一步研究。成冰纪—埃迪卡拉纪的冰期沉积普遍发育于扬子、塔里木克拉通及其周边地区，尤其埃迪卡拉纪冰期记录则广泛见于青藏高原东北缘、华北克拉通和塔里木克拉通等地区。本文以华北克拉通、祁连构造带和欧龙布鲁克微陆块上发育的埃迪卡拉纪冰期地层为研究对象，并综合扬子及塔里木的埃迪卡拉纪冰期资料和区域上蛇绿岩的发育，探讨原特提斯洋开启时间，为原特提斯洋整体形成演化历史研究提供基础资料。
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1 研究背景
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华北和塔里木克拉通位于原特提斯域北部，往南弥散分布着大量陆块/微陆块，如中祁连、欧龙布鲁克、柴达木及羌塘等（图1），这些陆块/微陆块之间的独立性或亲缘性研究直接关系到早古生代洋-陆格局的重建（李三忠等，2016b）。
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图1 中国及邻区主要克拉通和陆块/微陆块分布图（据Ren Jishun et al.，1999修改）
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Fig.1 Distribution map of the major cratons and continental/micro-continental blocks in China and adjacent regions (modified from Ren Jishun et al., 1999)
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埃迪卡拉纪处于Rodinia超大陆裂解到Gondwana超大陆聚合的阶段，发生了影响比较显著的寒冷气候事件，但与成冰纪的全球性冰期相比，埃迪卡拉纪冰期的影响范围相对较小（周传明等，2019；孙郎等，2024）。经过数十年中、外地质学家对埃迪卡拉纪的不断深入研究，现已查明在华北克拉通南缘和西缘、欧龙布鲁克微陆块、祁连山以及塔里木克拉通库鲁克塔格地区（图1研究区），紧挨着寒武纪早期地层之下都发育一套冰期沉积地层，可以作为区域地层对比的标志（Wang Xin et al.，2021；柳永清等，2023；孙郎等，2024），并为探讨不同陆块间的古地理格局和原特提斯洋演化历史提供重要依据。
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原特提斯洋-陆格局的争论还表现在洋盆的持续时限。许多学者支持原特提斯洋形成于Rodinia超大陆的解体，可能在~700 Ma已开始形成，促使一些微陆块的分离（Zhao Guochun et al.，2018），但是大陆裂谷环境岩浆活动的产生，并不代表原特提斯洋的打开。吴福元等（2020）认为，如果将早古生代蛇绿岩作为原特提斯洋存在的证据，那么目前厘定的中国大陆境内的原特提斯主要分布在秦岭、祁连-东昆仑、阿尔金及西昆仑地区（即秦祁昆，又称中央造山带）（图1研究区），在龙木错-双湖-昌宁-孟连带也有少量发育。因此，厘定秦祁昆造山带蛇绿岩的性质和时代对原特提斯洋形成演化研究尤为重要。
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2 埃迪卡拉纪冰期沉积记录
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2.1 华北克拉通南缘
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华北克拉通南缘埃迪卡拉纪地层由罗圈组和东坡组组成，罗圈组之下与中元古代不同地层呈角度不整合接触，其上与东坡组整合接触，或直接被寒武系第二阶辛集组含磷地层平行不整合覆盖（吴瑞堂等，1988；汪明洲等，1996；张良等，2008；旷红伟等，2023）（图2）。罗圈组自上而下沉积类型可分为以下4种，即：① 底部冰溜面之上的混杂砾岩，呈块状构造或弱层状构造，砾石成分主要来自下伏地层；② 砂质、泥质砾岩，含大小不等漂砾，呈弱层状或块状；③ 粉砂岩、细砂岩或两者韵律，可含漂砾；④ 泥页岩、粉砂岩或韵律，夹块状砾岩、坠石，从垂向上构成了冰下—冰前—海相冰碛物的沉积序列，为大陆冰川沉积样式（张碧云，2019；Chen Xiaoshuai et al.，2023；柳永清等，2023）。东坡组为无冰川沉积的粉砂岩、页岩组合，具海绿石胶结，底部为透镜状钙质石英砂岩，含砾页岩和砂砾岩互层（邢裕盛等，1989；张良等，2008）。
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尽管国内、外埃迪卡拉纪地层年代学研究不断取得进展，但有关冰碛岩直接精确的年龄数据却还十分少见，目前较多的仍然是间接的年龄限定。罗圈组冰碛岩及其相当于罗圈组的贺兰山正目观组、西安礼泉唐王陵昭陵组和安徽凤台组冰碛岩最年轻碎屑锆石年龄约为1100~820 Ma，揭示罗圈组及其相当层位的沉积时代不早于820 Ma（胡波等，2015；张文龙等，2016；Dong Xiaopeng et al.，2017；李振生等，2018）。Xu Bei et al.（2009）获得塔里木库鲁克塔格汉戈尔乔克（罗圈组相当层位）冰碛杂岩下部地层火山岩年龄为615 Ma。北祁连白杨沟群底部亦发育一套冰碛杂砾岩，相当于罗圈组的杂砾岩，Xu Xin et al.（2015）获得白杨沟群下部朱龙关群碳酸盐岩和细碎屑岩系中发育的玄武质火山熔岩年龄为583 Ma，据此可以粗略地限制罗圈组及其相当层位冰碛岩的时代下限应晚于583 Ma（旷红伟等，2023；柳永清等，2023）。此外，埃迪卡拉纪中晚期还发生了全球性遗迹地质历史时期幅度最大和等时性的碳同位素负漂移事件（Shuram），汗格尔乔克组冰碛岩（冰期）记录恰好发生在Shuram事件之后（Wang Ruimin et al.，2023a，2023b），基于铼锇定年和天文年代学方法获得了Shuram负漂移年代为570.2~562.5 Ma（Gong Zheng et al.，2020）。综上，罗圈冰期的起始时间又被进一步限定为晚于562.5 Ma（柳永清等，2023）。整合覆盖于罗圈组上部的东坡组，以粉砂岩或粉砂质板岩为主，产出埃迪卡拉纪晚期标志性化石Shaanxilithes sp.（Wang Xin et al.，2021），对比扬子克拉通也产出Shaanxilithes在灯影组中上部。扬子峡东地区灯影组的底界为551 Ma（Zhang Shihong，2004；Condon et al.，2005），此年龄可作为罗圈冰碛岩的顶界年龄。因此，罗圈冰碛岩的年龄大致为562.5~551 Ma。
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罗圈组冰碛岩上部虽然无盖帽白云岩覆盖，但在河南汝州、鲁山一带，东坡组中发育白云岩透镜体及白云质粉砂岩、砂岩。张良等（2008）获得白云岩透镜体的δ13C为-6.18‰~-4.19‰，白云质粉砂岩的δ13C为-4‰~-2‰，表明具有明显的碳同位素负漂移。
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2.2 欧龙布鲁克微陆块
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在欧龙布鲁克微陆块，埃迪卡拉纪地层由全吉群、红铁沟组和皱节山组组成。全吉群以角度不整合上覆于古元古界达肯大坂群变质岩系之上，为一套以碎屑岩为主夹镁质碳酸盐岩及冰碛砾岩的地层，自下向上包括麻黄沟组、枯柏木组、石英梁组、红藻山组、黑土坡组、红铁沟组和皱节山组（王云山等，1980）。这套地层过去曾被认为全部属于震旦系和下寒武统（王云山等，1980），然而红藻山组凝灰岩年龄为1640 Ma（张海军等，2016），麻黄沟组、枯柏木组、石英梁组及红藻山组最年轻碎屑锆石年龄约1800~1730 Ma（张璐等，2012；张海军等，2016；Sun Jiaopeng et al.，2019），表明全吉群下部4个组的时代可能为中元古代。据王超等（2015），红藻山组与上覆地层之间存在古风化壳，揭示两者之间存在一个区域性不整合界面（图2）。不整合面之上黑土坡组，由碳质板岩及泥质粉砂岩组成，吴承羲等（2024）在黑土坡组仅获得光面球藻Leiosphaeridia疑源类，而没有埃迪卡拉纪早中期典型的大型具刺疑源类；碎屑锆石年龄显示黑土坡组最大沉积年龄为750 Ma，可能为拉伸纪晚期地层（Sun Yunpeng et al.，2022）。因此，黑土坡组与下伏红藻山组之间存在着800~900 Ma的沉积间断。
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图2 华北克拉通南缘、欧龙布鲁克微陆块及祁连山埃迪卡拉纪冰碛岩地层对比图
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Fig.2 Stratigraphic columns of the Ediacaran tillites in the southern margin of the North China Craton, Olongbuluke Terrane and Qilian mountains
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黑土坡组上部发育红铁沟组冰碛岩，自下而上沉积类型分为以下3种（Wang Ruimin et al.，2023b），即：① 混杂砾岩，砾石成分主要为硅质岩和白云岩，分选、磨圆较差，为冰下泥石流沉积；② 弱层状混杂砾岩，砾石含量小于50%，可能形成于冰缘环境；③ 含坠石层状粉砂岩、泥岩，砾石含量小于10%，形成于冰前海相环境。皱节山组整合覆盖在红铁沟组之上，底部为含砾白云岩（盖帽白云岩），砾石含量由底往上逐渐减少至完全消失，白云岩之上发育细碎屑岩，产Shaanxilithes ningqiangensis和Charnia sp.等化石（Shen Bing et al.，2007；Pang Ke et al.，2021）。皱节山组被寒武系欧龙布鲁克群含砾砂岩不整合覆盖。综上，红铁沟组应为埃迪卡拉纪晚期冰碛岩，大致相当于罗圈组冰碛岩，皱节山组相当于豫西的东坡组。皱节山组盖帽碳酸盐δ13C为0‰~2‰（Shen Bing et al.，2010；Wang Ruimin et al.，2023b），碳同位素显示弱的正漂移。
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2.3 祁连山地区
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2.3.1 北祁连构造带
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在北祁连构造带，埃迪卡拉纪地层多指白杨沟群冰碛岩系（余以生，1994）。北祁连出露的前寒武纪地层自下而上被划分为北大河群、镜铁山群、朱龙关群、大柳沟群和白杨沟群（图2）。北大河群由各类片岩、片麻岩、斜长角闪岩及大理岩组成，变质变形较强，为古元古代—中元古代基底岩系（张招崇等，1998；李怀坤等，2007；Liu Yixin et al.，2021）。镜铁山群是以陆源碎屑为主夹有白云质大理岩及铁矿层的浅海相沉积岩系，时代为中元古代（Yang Xiuqing et al.，2016；Zhou Zilong et al.，2024）。朱龙关群下部为火山碎屑岩、中基性火山熔岩夹碳酸盐岩，上部为浅变质砂泥质碎屑岩夹铁矿层。大柳沟群下部为灰岩、白云岩，上部为粉砂质板岩、粉砂岩及白云岩。白杨沟群下部为冰碛杂砾岩，砾石大小混杂，呈次圆状，上部为粉砂质板岩（余以生，1994）。白杨沟群被寒武纪黑茨沟组砂岩及火山碎屑岩不整合覆盖。
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朱龙关群之前被认为是中元古代地层（徐晓春等，1996；Mao Jingwen et al.，1998；张招崇等，2001），最近对朱龙关群内火山岩、火山碎屑岩及侵入其中的辉绿岩脉的年代学研究显示其时代约为602~583 Ma（Xu Xin et al.，2015；Yang Xiuqing et al.，2022，2023），属埃迪卡拉纪。因此，朱龙关群之上的大柳沟群和白杨沟群也属于埃迪卡拉纪。目前，多数学者认为白杨沟群与欧龙布鲁克地区的红铁沟组冰碛岩层位相当，属于埃迪卡拉纪末的同一期冰期沉积记录（周传明等，2021；旷红伟等，2023；孙郎等，2024）。
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2.3.2 中祁连微陆块
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在中祁连微陆块，埃迪卡拉纪地层多指多若诺尔群（余以生，1994；张立涛等，2021；孙郎等，2022）。在中祁连西段，前寒武系自下而上由托赖群、托来南山群、龚岔群和多若诺尔群组成（图2）。托赖群以片岩、片麻岩及大理岩为主，局部夹石英岩，为古元古代—中元古代基底岩系（董进生等，2015；刘建栋等，2015；杨昕，2015）。拖来南山群下部南白水河组为滨浅海相碎屑岩，上部花儿地组为稳定型碳酸盐岩沉积。龚岔群不整合于拉伸系托来南山群之上（Gehrels et al.，2003），自下而上被划分为其他大坂组、五个山组、哈什哈尔组及窑洞沟组，其他大坂组主要为粗碎屑岩，五个山组为灰岩，哈什哈尔组为砂质板岩，窑洞沟组主要为灰岩和角砾状灰岩（甘肃省地质矿产局，1997；青海省地质矿产局，1997）。多若诺尔群自下向上为扁麻沟组、石板墩组及查干布尔嘎斯组，扁麻沟组角度不整合于龚岔群窑洞沟组之上，为粗碎屑砾岩、砂砾岩、砂岩及粉砂质板岩等，砾石成分复杂，分选及磨圆较差，多呈次棱角状，具有冰碛岩特点（余以生，1994）；石板墩组主要为火山碎屑岩、中基性火山岩夹硅质岩、碎屑岩，张立涛等（2021）在德勒诺尔一带石板墩组中新发现一套含砾（冰坠石）钙泥质粉砂岩组合，与海相基性火山岩共同产出；查干布尔嘎斯组主要为硅质板岩、灰岩及千枚岩。多若诺尔群之上被寒武系毛家沟组碳酸盐岩不整合覆盖。
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最近，孙郎等（2022）在肃北龚岔群哈什哈尔组粉砂质板岩中获得了569±2 Ma的最大沉积年龄，表明龚岔群可能整体属于埃迪卡拉系，之上的多若诺尔群冰碛岩沉积时代应晚于569±2 Ma，属于埃迪卡拉纪末期冰期记录，与华北罗圈组、欧龙布鲁克红铁沟组及北祁连白杨沟群冰碛岩可以对比。
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3 原特提斯洋内蛇绿岩的形成时代
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原特提斯构造域内蛇绿岩主要分布在秦祁昆造山带（表1），龙木错-双湖-昌宁-孟连带发育较少，本文暂不做讨论。秦祁昆造山带东段北秦岭商丹缝合带含有大量蛇绿混杂岩，包括具有成熟洋中脊性质的关子镇、小王涧、丹凤资峪N-MORB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-MORB型蛇绿岩，时代为534~471 Ma（李王晔等，2007；裴先治等，2007；陈隽璐等，2008；Dong Yunpeng et al.，2011a，2011b；李源等，2012；Yang Liming et al.，2018）。
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秦祁昆造山带西段的北祁连构造带出露有大量代表北祁连洋岩石圈残片的 E-MORB 或N-MORB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 Chienyuan et al.，2007；Xia Xiaohong et al.，2012；Song Shuguang et al.，2013；Yu Shengyao et al.，2021），分布在北部香毛山—九个泉—大岔大坂—老虎山和南部的熬油沟—玉石沟—东草河一带，北部蛇绿岩带时代集中在510~450 Ma（宋忠宝等，2007；孟繁聪等，2010；Xia Xiaohong et al.，2012；Song Shuguang et al.，2013；宋述光等，2019）；南带年龄为520~470 Ma（相振群等，2007；武鹏等，2012；Xia Xiaohong et al.，2012；吴少锋等，2018）。南祁连蛇绿混杂岩主要出露于党河南山、大道尔吉、木里和拉脊山，具E-MORB或N-MORB性质的蛇绿岩主要分布于拉脊山和清水地区，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），时代集中于535~490 Ma（Dong Yunpeng et al.，2011b；付长垒等，2017；Zhang Yuqi et al.，2017；宋述光等，2019；Yan Zhen et al.，2019；李智佩等，2020）。
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表1 秦祁昆造山带内原特提斯缝合带及块体划分（据吴福元等，2020修改）
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Table1 Proto-Tethys sutures and blocks in the Qinling-Qilian-Kunlun Orogenic Belt (modified from Wu Fuyuan et al., 2020)
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柴北缘蛇绿混杂岩带西起阿尔金断裂南侧，向东经赛什腾山、绿梁山、锡铁山和阿木尼克山，止于哇洪山一带，其中具N-MORB性质的蛇绿岩主要分布在锡铁山、绿梁山和沙柳河一带，年龄集中在535~485 Ma（袁桂邦等，2002；Zhang Guibin et al.，2008；朱小辉等，2012；李建兵等，2018）。东昆仑阿其克库勒湖-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，代表了过渡洋中脊的E-MORB型蛇绿岩残片（边千韬等，2002；李怀坤等，2006；魏博，2015；祁晓鹏等，2016），同位素年龄集中在537~450 Ma（Yang Jingsui et al.，1996；李怀坤等，2006；冯建赟等，2010；Li Ruibao et al.，2013；魏博，2015；王国良等，2019）。东昆仑木孜塔格-阿尼玛卿蛇绿混杂岩带西起阿尔金断裂，向东经木孜塔格、昆仑山口、布青山到阿尼玛卿山，时代以晚古生代为主，但在得力斯坦沟及布青山等地有N-MORB型蛇绿岩组分，为洋脊蛇绿岩套组合，同位素年龄为516~467 Ma（边千韬等，1999；刘战庆等，2011；李智佩等，2020）。
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北阿尔金红柳沟-拉配泉蛇绿混杂岩带西起若羌县红柳沟，向东经恰什坎萨依、拉配泉和石棉矿，最终到肃北半鄂博一带。蛇绿岩内发育MORB型基性火山岩、席状岩墙群及OIB型玄武岩，同位素年龄集中在514~479 Ma（吴峻等，2002；杨经绥等，2002；2008；高晓峰等，2012；王军等，2018）。南阿尔金阿帕-茫崖蛇绿混杂岩带沿阿尔金断裂分布在阿中地块南缘，对于蛇绿岩及其岩石组合类型，多数研究者认为具有E-MORB和OIB 特征，属洋脊型蛇绿岩（王焰等，1999；李向民等，2009；康磊等，2016），同位素年龄为510~467 Ma（李向民等，2009；马中平等，2011；郭金城等，2014）。
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西昆仑库地-其曼于特蛇绿混杂带西起库地，向东经尼沙、其曼于特，沿喀什塔什山北侧延伸，止于阿尔金走滑断裂。该蛇绿岩中枕状玄武岩间的放射虫硅质岩时代为早古生代（方爱民等，2000），锆石U-Pb同位素年龄集中在525~450 Ma（肖序常等，2003；张传林等，2004；尹得功等，2013；李天福等，2014；白春东等，2018；郭远新等，2019）。西昆仑南部康西瓦-苏巴什蛇绿混杂岩带一直被认为是古特提斯发育的地区，1∶25万康西瓦幅区域地质调查项目，在康西瓦北侧首次发现了蒙古包-普守早古生代蛇绿混杂岩带，该带向西延伸到赛图拉被康西瓦-苏巴什蛇绿构造混杂岩带截切，向东延伸到图边与库地-其曼于特早古生代蛇绿构造混杂岩带合并，内部发育大量蛇纹石化纯橄岩、云母二辉岩、辉长岩、蚀变辉绿岩、玄武岩夹硅质岩、中基性熔岩及英云闪长岩等岩石组合，该蛇绿岩带北侧发育与其对应的510~400 Ma的闪长-花岗质岩石（崔建堂等，2006；2007；吴福元等，2020）。
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4 讨论
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4.1 埃迪卡拉纪冰碛岩综合对比
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中国新元古代冰碛岩系，以塔里木克拉通的库鲁克塔格发育最全，有四套冰碛岩层，即贝义西组、阿勒通沟组、特瑞艾肯组和汉格尔乔克组，其中贝义西组底部及顶部火山灰经SHRIMP定年分别为740±7 Ma和725±10 Ma（Xu Bei et al.，2009），时代相当于拉伸纪晚期Kaigas冰期，阿勒通沟组和特瑞艾肯组时代相当于成冰纪的Sturtion和Marinoan冰期，最后一组冰碛岩为汉格尔乔克组，时代为埃迪卡拉纪晚期（高林志等，2013）。如前文所述，华北克拉通南缘罗圈组和欧龙布鲁克红铁沟组冰碛岩均不整合于中元古代不同层位之上，冰碛岩上覆地层中均产出埃迪卡拉纪晚期标志性化石Shaanxilithes。目前，虽然北祁连白杨沟群和中祁连多若诺尔群冰碛岩上部地层中没有Shaanxilithes化石产出的报道，但下伏地层的时代被限定为埃迪卡拉纪。上述冰碛岩系应相当于塔里木汉格尔乔克冰期，时代为约562~551 Ma的埃迪卡拉纪晚期（柳永清等，2023），略晚于~580 Ma全球性Gaskiers冰期（Pu et al.，2016）。此外，与罗圈冰碛岩系同时代的冰碛岩，在朝鲜半岛（飞浪洞组）（Hu Bo et al.，2012；胡波等，2015；金明哲等，2016）、淮南（凤台组）（岳亮等，2020）和贺兰山（正目观组）（Yang Jie et al.，2019；Wang Xin et al.，2021）等地也有分布。
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华北克拉通南缘、欧龙布鲁克微陆块及北祁连、中祁连4个地区的冰碛岩岩石类型，主要为块状/弱层状冰碛杂砾岩，含砾砂岩、砂岩/粉砂岩韵律和发育漂砾或含坠石的泥质粉砂岩。砾石成分多为近源或冰碛岩直接下伏的基底岩石，砾石规模参差不齐（柳永清等，2023）。在沉积特征上，总体可分为下部的冰川沉积和上部的冰水沉积，其中冰川沉积多为块状结构，层理不明显；冰水沉积特征为层理逐渐明显，砾石含量逐渐减少，可见冰坠石经典沉积构造，并逐渐过渡为上部的海相细粒碎屑岩段。
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在碳同位素组成变化上（图3），罗圈冰碛岩上部东坡组虽然无盖帽碳酸盐发育，但白云岩透镜体及白云质粉砂岩的δ13C约为-6‰~-2‰；欧龙布鲁克皱节山组底部盖帽白云岩厚4~5 m，δ13C约为-1‰~2‰；在祁连山，白杨沟群和多若诺尔群冰碛岩上部未发育盖帽白云岩；华北克拉通西缘正目观组冰碛岩之上盖帽白云岩，厚1.6 m，δ13C为-5‰~-2‰（Yang Jie et al.，2019）；汉格尔乔克冰碛岩上部泥质/粉砂质白云岩厚1~5 m，δ13C为-16‰~-2‰，同位素组成变化较大（Shen Bing et al.，2011；Wang Ruimin et al.，2023b）。综上，埃迪卡拉纪盖帽白云岩主要显示碳同位素负漂移，仅皱节山组盖帽白云岩表现为既有负漂移，也发育较低正漂移的特点。
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4.2 华南埃迪卡拉纪综合地层对比
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华南的成冰纪（南华纪）自下而上为古城组、大塘坡组和南沱组。埃迪卡拉纪（震旦纪）以三峡剖面研究最好，分为陡山沱组和灯影组。陡山沱组整合覆于南沱冰碛岩（相当于Marinoan冰期）之上，自下而上依次为盖帽白云岩、黑色粉砂质页岩夹碳酸盐岩、灰色中厚层白云岩、黑色页岩和炭质页岩等，含微体生物化石及宏体化石（Xiao Shuhai et al.，2002；Liu Pengju et al.，2014，2019; Xiao Shuhai et al.，2021）。灯影组自下而上依次为灰白色厚层白云岩、黑色厚层灰岩和灰白色厚层白云岩。灯影组中已发现大量埃迪卡拉纪晚期化石Cloudina、Shaanxilithes和Sinotubulites等（An Zhihui et al.，2020；Xiao Shuhai et al.，2021；Yang Ben et al.，2022）。通过岩层中的火山灰锆石U-Pb定年，已确定陡山沱组底界年龄为635 Ma，灯影组底界为551 Ma（Condon et al.，2005），灯影组与上部寒武系纽芬兰统连续沉积，之后被寒武系纽芬兰统上部或寒武系第二统平行不整合覆盖。
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华南埃迪卡拉纪地层中没有发现冰川事件的直接沉积记录，但在湖北宜昌樟村坪陡山沱组中，Wang Zhou et al.（2017）发现了硅化的钙芒硝状方解石，认为它们是同沉积期形成的六水方解石假晶，代表了接近冰点的寒冷气候环境的沉积，表明华南在埃迪卡拉纪可能存在区域性冰期事件。
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华南埃迪卡拉纪记录了3次全球性碳同位素负漂移事件，EN1/CANCE，EN3/DOUNCE和EN4（Xiao Shuhai et al.，2016；周传明等，2019）（图3），其中EN3/DOUNCE可与Shuram事件对比，为历史上最大的负漂移事件（Wang Yuanzheng et al.，2022）。Zhou Chuanming et al.（2017）发现，在EN3之后还存在1次碳同位素的正漂移（DPE）和随后的一次负漂移（MNE）。新疆库鲁克塔格汉格尔乔克组冰碛岩下伏水泉组也记录了完好的Shuram信息（Xiao Shuhai et al.，2004；Wang Ruimin et al.，2023a，2023b），可对比华南EN3/DOUNCE负漂移事件；而汉格尔乔克组上覆盖帽白云岩的负漂移则与MNE对应。因此，华北克拉通罗圈组及正目观组冰碛岩上覆地层的碳同位素负漂移均可与华南的MNE进行对比。欧龙布鲁克皱节山组底部盖帽白云岩较弱的正漂移特征，与华南MNE事件后期弱的正漂移也存在对应关系。
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图3 埃迪卡拉纪冰期盖帽白云岩碳同位素对比（据周传明等，2019修改）
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Fig.3 Carbon isotope value comparison of Ediacaran glacial cap dolomites (modified from Zhou Chuanming et al., 2019)
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综上，地层的沉积序列及所含化石、碳同位素组成变化和同位素地质年代学研究共同显示，华北、塔里木、扬子克拉通及其间的陆块/微陆块（祁连、欧龙布鲁克等）在埃迪卡拉纪具有极强的相似性，表明它们当时可能连为一体，共同沉积了古中国地台最初的盖层（黄汲清等，1977；Ren Jishun et al.，1987；任纪舜，2004），各陆块/微陆块之间并不存在相互分割的洋盆，原特提斯洋此时并未形成。
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4.3 秦祁昆造山带蛇绿岩时代限定
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秦祁昆造山带内发育的蛇绿岩在空间上基本可以相互对比，自北向南有北阿尔金-北祁连缝合带、南阿尔金-柴北缘-商丹缝合带、库地-昆中缝合带和康西瓦-阿尼玛卿-布青山缝合带（吴福元等，2020）。如前文所述，前三条带中蛇绿岩的时代主要集中在535~450 Ma，而后一条缝合带中，除大量发育的晚古生代蛇绿岩外，同时发育约520~470 Ma的早古生代蛇绿岩。因此，中国大陆境内原特提斯的时代大约为535~450 Ma的寒武纪—奥陶纪。结合前述不同陆块/微陆块间埃迪卡拉纪地层的相似性，中国境内的原特提斯洋可能并不是多数学者认为的从元古宙延续到早古生代，而是古中国地台解体后才产生的早古生代小洋盆-微陆块体系（任纪舜，2004）。
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5 结论
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（1）华北、扬子、塔里木克拉通及其间的陆块/微陆块在埃迪卡拉纪可能连为一体，共同沉积了古中国地台最初的盖层，它们之间并不存在相互分割的洋盆，原特提斯洋此时并未形成。
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（2）秦祁昆造山带内早古生代蛇绿岩的时代主要集中在535~450 Ma，表明中国大陆境内原特提斯洋的形成时代应该为寒武纪—奥陶纪。
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（3）原特提斯洋可能并不是多数学者认为的从元古宙延续到早古生代的大洋，而是古中国地台解体后才产生的早古生代小洋盆-微陆块体系。
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致谢：谨以此文祝贺恩师任纪舜院士九十华诞，感谢老师多年来对我们的悉心教导，敬祝任先生生日快乐、福寿双全！诚挚感谢审稿专家对本文提出的宝贵修改意见和建议。
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摘要
原特提斯洋是研究特提斯地球动力学的重要切入点，目前对原特提斯洋的起源，以及内部多个陆块/微陆块之间的亲缘性研究仍存在争议，这直接限制了对原特提斯洋形成演化历史这一关键科学问题的研究。埃迪卡拉纪，原特提斯构造域内很多陆块/微陆块都发育一套冰期沉积地层。本文通过对华北克拉通南缘、欧龙布鲁克微陆块以及祁连山等地埃迪卡拉纪冰碛岩地层的综合对比分析，结合扬子及塔里木的冰期资料和区域上蛇绿岩的发育，认为华北、扬子、塔里木克拉通及其间的陆块/微陆块在埃迪卡拉纪可能连为一体，共同沉积了古中国地台最初的盖层，原特提斯洋可能并不是从元古宙延续到早古生代的大洋，而是古中国地台解体后产生的早古生代小洋盆-微陆块体系。
Abstract
The Proto-Tethys Ocean is an important aspect for understanding Tethyan geodynamics. However, the origin of this ocean and the affinity of multiple continental/micro-continental blocks within it are still controversial, hindering the research into its formation and evolutionary history. During the Ediacaran, a suite of glacial sedimentary strata developed on many continental/micro-continental blocks in the Proto-Tethys domain. This study presents a comprehensive analysis of Ediacaran tillites from the southern margin of the North China Craton, the Olongbuluke Terrane, and the Qilian Mountains. Integrating these findings with previous glacial literatures of the Yangtze and Tarim Cratons, as well as regional ophiolite studies, we propose that the North China, Yangtze, and Tarim Cratons, along with the intervening continental/micro-continental blocks, may have been connected and deposited the initial cover of the ancient Chinese Platform during the Ediacaran. Our findings suggest that the Proto-Tethys Ocean was not a direct successor of the Proterozoic Ocean but rather a small ocean basin-microcontinent system that developed after the breakup of the ancient Chinese Platform in the early Paleozoic.
Keywords
Proto-Tethys Ocean ； Ediacaran ； micro-continent ； tillite ； ophiolite
