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大陆地壳生长和演化研究是了解地球早期发展历史的关键，对认识古老克拉通的形成与地球环境演变具有重要意义（ Zhai Mingguo and Santosh，2011; Nance et al.，2014）。目前，早前寒武纪的陆壳形成、增生时间及机制仍存在争议。一种观点认为现今的地壳形成于地球演化的早期（ >4. 0 Ga），其后新生地壳量等于或小于由于循环进入地幔的消耗地壳量，导致地壳累积增长曲线呈稳态变化或呈下降趋势（Armstrong，1991; Sylvester et al.，1997）。另一种观点认为地壳在整个地质历史时期一直处于增长状态，太古宙早期，地壳增长速度较快，以后渐慢，地壳增长一直以稳定的速度进行（ Taylor and Mclennan，1995）。无论哪种模式，都认为太古宙是地壳增长的重要时期，而新元古代到显生宙，地壳增长量十分有限。
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近年来，古老克拉通大量的同位素年龄数据表明，克拉通 90%的陆壳可能是在早前寒武纪形成，其主要形成期集中在 3.5~3.1 Ga、2.8~2.7 Ga、2.6~2.5 Ga3 个阶段（Hawkesworth and Kemp，2006; Condie and Aster，2010; Zhai Mingguo and Santosh，2011）。其中，新太古代早期（2.8~2.7 Ga）和晚期（2.6~2.5 Ga）被认为是全球克拉通大陆地壳巨量生长最为关键的时期（Khanna et al.，2014; Hayman et al.，2015; Tang Ming et al.，2020），受样品稀少的限制，3.5~3.1 Ga 时期陆壳形成演化的研究相对薄弱。 Shirey 等通过对澳大利亚卡普瓦尔、西伯利亚、加拿大 Slave 克拉通和津巴布韦等五个古老克拉通产出的钻石进行研究发现，钻石中包裹体内的物质在 3.2~3. 0 Ga 期间发生了较大转变，之前为以橄榄岩为主，之后是以榴辉岩为主（ Shirey and Richardson，2011）。另外，TTG 岩石（ tonalite— trondhjemite—granodiorite，即英云闪长岩—奥长花岗岩—花岗闪长岩，构成的岩石组合）的 Rb / Sr、 K2O/ Na2O、Sr/ Y 和（ La / Yb） N 值和玄武岩、科马提岩等基性岩的 Ba / La、Ba / Nb、U/ Nb 和 Pb / Nd 值，在约 3.15 Ga 前后都发生了显著变化（ Shirey and Richardson，2011; 邓晋福等，2015; 张旗等，2024; 张金朋等，2024）。这些变化都说明，3.2~3. 0 Ga 可能是地球地壳形成演化的一个关键转折阶段。甚至，有些学者认为板块构造运动就可能起始于 3.2~3. 0 Ga 期间（Dhuime et al.，2012，2015; 吴鸣谦等，2014; Gamal El Dien et al.，2020; Windley et al.，2021）。
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受古老地壳岩石样品稀少的限制，前人对 3.2~3. 0 Ga 时期岩石的成因及地壳形成演化的研究多集中于地球化学数值模拟（Windley et al.，2021）。对实际地质样品的研究相对较少，仅有的几个克拉通古老岩石的研究也比较独立，缺少全球性的对比。笔者等对全球 3.1 Ga 左右岩石和锆石的地质记录进行系统梳理，总结了其锆石年龄分布、地球化学、 Lu—Hf—O 同位素组成特征，系统对比了全球主要克拉通 3.1 Ga 左右岩石的时空分布、物质组成、地球化学以及同位素特征，探讨中太古代岩石成因为早期地壳生长与演化提供关键信息。
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1 3.1 Ga 左右岩石和锆石的时空分布特征
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统计表明，全球约 10 余个克拉通中保存有 3.1 Ga 左右时期的岩石，22 个克拉通见有 3.1 Ga 左右时期的岩浆锆石和碎屑锆石（附表，纸质印刷本略，见网络版:www. geojournals. cn / georev; 图1），主要特征如下:
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（1）在现今构造格局下，岩石主要分布在北半球地区，南半球仅在东南极地盾区和澳大利亚部分地区有发现，出露范围很小，多以脉体形式穿插于其他岩石之中; 锆石分布广泛，遍布全球，北半球明显多于南半球。在发现的约 3.1 Ga 锆石中，碎屑锆石与岩浆锆石数量相当，但在非洲刚果、津巴布韦克拉通和印度部分地区岩浆锆石数量明显多于碎屑锆石。其在 3.1 Ga 左右时分布特征还需进一步研究（张世红灯，2002; 张拴宏等，2022）。
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图1 全球太古宙克拉通位置分布（图中给出了 3.1 Ga 左右岩石和锆石的空间位置，数据来源见附表）
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Fig.1 Distributions of global Archeancratons (showing spatial distribution of~3.1 Ga rocks and zircons) (modified from Tang Yanjie et al., 2013. See attached table for data details)
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（2）岩石以 TTG 岩石为主，少量闪长岩、辉长岩等岩石，在欧洲一处蛇纹岩中也存在 3.1 Ga 左右岩石。
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（3）并非所有 3.1 Ga 左右 TTG 岩石都伴随有表壳岩存在，仅在华北克拉通、圣弗朗西斯科克拉通、乌克兰地盾、印度库克地块、达尔瓦克拉通、西格陵兰 6 个地区发现有表壳岩，它们具有相似的岩石组合，由变质泥岩、变质砾岩和 BIF 组成。
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（4）岩石普遍遭受后期变质作用改造形成片麻岩，原始岩石几乎不可分辨。
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（5）3.1 Ga 左右的碎屑锆石多发现于太古宙岩石中（3. 0~2.5 Ga），也有少量出现在元古宙和现代河流沉积物中。
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从全球约 3.1 Ga 锆石和岩石年龄统计（图2 和图3），可以看出:①3.1 Ga 左右岩石存在 3 个明显的年龄峰值，分别为 3. 0 Ga、3. 05 Ga 和 3.15 Ga。 ②锆石年龄存在两个明显的年龄峰，分别为 3. 0 Ga 和 3.15 Ga。 ③各克拉通约 3.1 Ga 锆石年龄均存在相似的 3.15 Ga 峰值（南美洲亚马逊和圣弗朗西斯科克拉通除外）。说明约 3.15 Ga 时期的岩浆事件具有全球性，而 3. 0 Ga 和 3. 05 Ga 两次岩浆事件仅在局部发生，不具备全球性。
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1.1 亚洲地区
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华北克拉通是欧亚大陆东部最大的克拉通之一，已在 5 个地区发现 3.1 Ga 岩石，但规模都很小。鞍山—本溪地区，3.1 Ga 岩石以包体或侵入体的形式与更古老岩石一同构成白家坟、东山、深沟寺和锅底山杂岩（万渝生等，2001; 周红英等，2007，2008; Wu Fuyuan et al.，2008; Wan Yusheng et al.，2012; 董春艳等，2013）。冀东，黄柏峪和曹庄，喇叭山岩系变质碎屑沉积岩中存在 3.1 Ga 左右岩石和碎屑锆石。最近，Meng Fanchao 等（2022）在渤海湾盆地钻孔岩芯样品中发现 3.1 Ga 左右岩石，说明渤海湾盆地存在中太古界基底（ 孙会一等，2016; 万渝生等，2021; Meng Fanchao et al.，2022）。鲁西地区，新太古代早期岩石中存在大量 3.1 Ga 左右锆石颗粒，认为该区可能存在一个中太古代陆核（Gao Lei et al.，2019; Yu Yang et al.，2022）。辽北地区，3.1 Ga 左右的岩石主要分布在栾家界地区（ Li Dapeng et al.，2020; Liu Jin et al.，2022）。
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扬子克拉通 3.1 Ga 左右岩石分布于南部的崆岭杂岩和撮科杂岩。最近，在崆岭杂岩中获得片麻岩岩石年龄为约 3. 0 Ga，并获得 3.1 Ga 的两阶段 Hf 模式年龄（Qiu Xiaofei et al.，2018a; Qiu Xiaofei et al.，2018b; 邱啸飞等，2022）撮科杂岩中也发现 3.11~3. 06 Ga 太古宙基底岩石，这些岩石由古太古代至中太古代早期的新生地壳物质改造形成（Zhang Shaobing et al.，2006; Cui Xiaozhuang et al.，2018）。
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图2 （a）全球~3.1 Ga 锆石年龄分布图（数据详情见附表）;（b）全球~3.1 Ga 岩石年龄分布图（数据详情见附表）
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Fig.2 (a) Global~3.1 Ga zircons age distribution (see attached table for data details) ; (b) Global~3.1 Ga rocks age distribution (see attached table for data details)
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图3 全球各地区 3.1 Ga 左右岩石年龄分布直方图
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Fig.3 Histograms of age distribution from~3.1 Ga rocks
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塔里木克拉通边缘地区广泛分布着太古宙露头岩石。塔里木盆地西南缘赫罗斯坦岩群中发现紫苏辉石麻粒岩，其锆石 U-Pb 年龄为 3137±4 Ma，是塔里木克拉通存在中太古代古老陆核和大规模地壳生长的直接证据（Zhang Chuanlin et al.，2013; 郭新成等，2013; Ge Rongfeng et al.，2013，2022）。敦煌东巴兔山干沟地区片麻岩中，从 45 颗锆石中获得约 3. 06 Ga U-Pb 表面年龄，是目前为止敦煌最古老的岩石，对指示敦煌地区的构造归属具有重要意义（赵燕等，2015）。
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印度太古宙克拉通广泛分布于中—南部地区。达瓦克拉通西部以 3.1~3. 0 Ga 岩浆岩为主，εHf（t）值为负值，暗示这些岩石是由古老地壳重熔而来（Maibam et al.，2016; Ao Wenhao et al.，2021）。 Sargur 群代表达瓦克拉通较老绿岩带，由以超镁铁质玄武岩为主的火山序列与层间变质沉积物组成，其锆石表面年龄为 3200~3106Ma（Jayananda et al.，2015; Guitreau et al.，2017; Dasgupta et al.，2019; Ravindran et al.，2023）。 Arsikere，Bellur 和霍纳加纳哈利（Honaganahalli）地区的正片麻岩，二长花岗岩和花岗片麻岩等岩石均获得了 3.1~3. 0 Ga 锆石年龄（Maibam et al.，2011; Jayananda et al.，2019; Ao Wenhao et al.，2021）。辛格布姆克拉通 3.1 Ga 左右岩石分布于辛格布姆花岗杂岩和古铁矿群。其中辛格布姆花岗杂岩的侵位一直持续到中太古代（3120 Ma 和 3050 Ma）（Misra，2006），马尤布汉杰（Mayurbhanj）花岗岩套中获得了一致的锆石结晶年龄（3080±8 Ma，3092±5 Ma（Mishra et al.，1999）; 3084 ± 3 Ma（ Nelson et al.，2014）; 3063 ± 11 Ma（Upadhyay et al.，2019）。古铁矿群中博奈花岗岩套具有较年轻的锆石结晶年龄（3.16 Ga），与辛格布姆花岗杂岩在年龄上相当。另外，在苏金达一瑙萨希地区发现一套锆石 U-Pb 年龄为 3123±7 Ma 和 3119 ± 6 Ma 的层状铁镁质—超铁镁质侵入体（Monda et al.，2006; Khatun et al.，2014）。巴斯塔尔克拉通 3.1 Ga 左右岩石分布于苏克马（ Sukma）群中，其最大沉积年龄为 3128±6 Ma（Nandi et al.，2023）。除此之外，印度南部库尔格（Coorg）地块、阿拉瓦利和本德尔坎德克拉通也发现了 3.1 Ga 左右铁镁质—超铁镁质岩石和 TTG 岩石（3189 ± 5 Ma）（Santosh et al.，2016; Amaldev et al.，2016; Yang Qiongyan et al.，2016; Yu Bing et al.，2021; Yang Chengxue et al.，2023; Kaur et al.，2021，2022）。
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西伯利亚（Siberian）克拉通位于俄罗斯东部，是亚洲最大的前寒武纪克拉通。目前，仅在阿纳巴尔（Anabar）地区发现有 3.12 Ga 左右石榴子石云母片麻岩、约 3.19 Ga 石榴子石麻粒岩和 3.1 Ga 左右碎屑锆石（Rosen et al.，2006; Paquette et al.，2017; Shatsky et al.，2022）。这些证据证实西伯利亚克拉通存在 3.1 Ga 左右时期太古代地壳生长事件。
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1.2 大洋洲
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澳大利亚西部和南部地区太古宙克拉通分布广泛，包括皮尔巴拉（Pilbara）克拉通、高勒（Gawler）克拉通和伊尔冈（Yilgarn）克拉通。皮尔巴拉克拉通古陆核可以分为东、西皮尔巴拉地体两部分。在东皮尔巴拉地体的英云闪长岩和火山沉积岩中获得 3.1 Ga 左右锆石年龄（Kranendonk et al.，2010）。西皮尔巴拉地体相对年轻，已在 3 个地区发现 3.1 Ga 左右岩石，包括邵尔地体火山碎屑岩与花岗片麻岩（3.13~3.11 Ga）（Smithies et al.，2005）、谢拉塔杂岩东部的黑云母英云闪长岩（3. 07 Ga）和克里夫维尔组长英质凝灰岩中的继承锆石（ 3.195 Ga）（Kranendonk et al.，2007）。高勒克拉通新发现了约 3.15 Ga 中太古代岩石，出露范围较广，把克拉通构造演化历史向前推进 500 Ma 左右（Fraser et al.，2010）。伊尔冈克拉通克拉通被划分为 5 个主要部分，已在 4 个地体中获的 3.1 Ga 左右岩石，包括默奇森东部地体（3.17 Ga）、南十字星花岗岩—绿岩带（3. 05 Ga）、纳瑞尔地体石英岩（3.1 Ga）和西南地体石英岩（ 3.177 Ga、 3. 05 Ga）（ Kinny et al.，1990; Bosch et al.，1996; Chen Shefa et al.，2003）。
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1.3 非洲
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非洲太古宙克拉通分布于中部和南部地区。卡普瓦尔（Kaapvaal）克拉通中东部于 3.1 Ga 左右进行第一次克拉通化，该地区 3.1 Ga 左右花岗岩面积超过 20000 km 2（Belcher et al.，2006）。在斯威士兰中部存在大规模沉积记录（3.16 Ga）和麻粒岩相变质记录（3.11~3. 07 Ga），这些记录被解释为增生边缘沉积（Taylor et al.，2012，2019）。斯威士兰西部存在大型花岗岩基岩，从中获得 3.15~3. 08 Ga 锆石 U-Pb 年龄和 3.11 Ga 全岩 Sr—Nd 等时线年龄。（Moser et al.，2001; Westraat et al.，2005; Suhr et al.，2014）。刚果（Congo）克拉通 3.1 Ga 左右岩石分布于克拉通西北部 Ntem 杂岩中，包括沉积变质岩（3.14~3. 07 Ga）、辉石花岗岩套和 TTG 岩套（3.15 Ga），其中 TTG 岩套被解释为在俯冲—增生构造模式下形成（Akame et al.，2020）。在马达加斯加 Antongil 克拉通南部变质沉积物中，获得了 3178 Ma 变质流纹岩和 3187 Ma 黑云母片麻岩，可能当时存在一个中太古代陆核。
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1.4 北美洲
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格陵兰岛南部基亚地体研究历史较长。早期研究认为，基亚地体是由 3076~3068Ma 岩浆弧形成，存在拉斑玄武岩和钙碱性安山岩（ Garde，2007; Szilas et al.，2015，2017）。诺兰特（Nordlandet）杂岩是基亚地体最古老的部分，由约 3.19 Ga 闪长片麻岩组成，受到 3. 05 Ga 英云闪长岩侵入影响。在菲斯克峡湾（ Fiskefjord）杂岩和阿兰瓜杂岩中获得了约 3180 Ma 变质闪长岩和小型捕虏体、3134~3131 Ma 麻粒岩以及大量 3015 Ma 深成侵入岩。具有相似锆石年龄的片麻岩在菲斯克峡湾杂岩内部和周围也普遍存在（Nutman et al.，2004; Kirkland et al.，2018; Kirkland et al.，2020; Steenfelt et al.，2020; Yakymchuk et al.，2020; Waterton et al.，2020; Olierook et al.，2021）。基亚地体北部是未分化的麻粒岩和角闪岩相正片麻岩，它们含有基性上地壳岩石的残余。岩石组合类型与菲斯克峡湾杂岩相似，但年龄相对较小，约 3020Ma（Scherstén et al.，2013; Gardiner et al.，2019）。并发育小型碳酸盐岩侵入体（3007±2Ma）（Bizzarro et al.，2002）。
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苏必利尔（ Superior）克拉通是北美古地核重要组成部分，3.1 Ga 左右岩石分布于克拉通西北部萧提（Solit）湖块体、东盟（Assean）湖块体和皮尔森（Pearson）湖块体，前人研究认为萧提湖块体、东盟湖块体具有相同的 3.16~3.20 Ga 中太古代深成作用事件（Böhm et al.，2003）。其余地区零星分布着~3.1 Ga 太古宙岩石，如北加勒比海地区（3122±13 Ma）、温尼伯河（ Winnipeg）地区（3111 ± 14 Ma）、英（English）河地区（3069±14 Ma、3122±13 Ma）、坦尼斯湖地区（3055±4 Ma、3150 Ma）、明尼苏达河地区（3140 Ma）等，这些地体所记录的中太古代事件与花岗岩—绿岩地体的初始形成有关（Melnyk et al.，2006; Bickford et al.，2006; Lankvelt et al.，2016; Li Dengfeng et al.，2020; Strong et al.，2022）。
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怀俄明克拉通中部的巴洛峡（Barlow Gap）群基底石英岩中含有 3.2~3.1 Ga 碎屑锆石（Grace et al.，2006）。蒙大拿州西南部、北部和萨卡维（Sacawee）地块中，3.1 Ga 左右高铝奥长花岗岩和长英质岩石侵入古太古代麻粒岩中（Gifford et al.，2014）。明尼苏达（Minnesota）州西南部的蒙得维亚（Montevideo）省和莫顿（Morton）地区发现了复杂的 3.1 Ga 左右岩石，岩性为花岗闪长混合岩、花岗片麻岩和花岗闪长岩侵入体（3140±5Ma），锆石外围存在 3.2~3. 0 Ga 生长痕迹，说明该地区 3.1 Ga 左右发生剧烈岩浆活动导致古老岩石变质和新地壳的生长（Schmitz et al.，2006）。
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1.5 南美洲
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圣弗朗西斯科（São Francisco）克拉通由太古宙花岗片麻岩组成。克拉通北部 3.1 Ga 左右岩石主要分布于加维昂（ Gavião）地块和塞里尼亚（Serrinha）地块，包括 TTG 片麻岩（3180~3000 Ma）（Peucat et al.，2002; Oliverira et al.，2020; Barbosa et al.，2020）和混合岩（3. 08~2.98 Ga）（Oliverira et al.，2010）。乌阿（Uauá）地块与塞里尼亚地块接壤，其最古老岩石为 3.15~3.12 Ga 条带状片麻岩。此外，该区还发现了 3.13~3.12 Ga 英云闪长岩和 3.13~3. 07 Ga 长英质火山岩（ Oliverira et al.，2010，2019）。安布罗休（Ambrósio）地块中混合岩包体，其锆石结晶年龄为 3.1 Ga（Mello et al.，2006）。
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拉普拉塔克拉通尼科皮雷斯（Nico PeÂrez）地体中心有两个太古宙单元，La China 杂岩和山雀（Las Tetas）杂岩。前人在此处发现了 3096 Ma 岩石和 3.12~3.16 Ga 的锆石（ Gaucher et al.，2011; Masquelin et al.，2021）。
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在巴西东北部博尔博雷玛（Borborema）省存在南美洲最古老的地壳碎片:São José do Campestre 地块。该地块两侧存在约 3.18 Ga 奥长花岗质片麻岩，并被约 3. 0 Ga 辉长斜长岩侵入（Dantas et al.，2004）。在巴西西部亚马逊（Amazonian）克拉通中发现有两个太古宙陆核（ Juliani et al.，2010; Fernandes et al.，2021）:卡拉加斯（Carajas）是一个典型花岗岩—绿岩地体，包含约 3. 04~2.99 Ga 绿岩带和花岗岩类（Almeida et al.，2011，2013）; 而卡拉吉（Caraj）存在太古宙岩石，包括约 3. 06 Ga TTG 片麻岩和混合岩、约 3. 0 Ga 麻粒岩和约 3. 0 Ga 钙碱性英云闪长岩（ Moreto et al.，2011，2015a，2015b）。
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1.6 欧洲
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萨尔玛提亚（ Sarmatia）克拉通是东欧地台基底南部部分，由沃罗涅日结晶地块和乌克兰地盾组成。在沃罗涅日结晶地块，3.1 Ga 左右岩石包括科马提岩—拉班玄武岩（3.2~3. 0 Ga）（Chernyshov et al.，2014）和谢尔盖耶夫（Sergiev）橄榄杂岩中的蛇纹岩（3136 Ma）（Lobach-Zhuchenko et al.，2017）。在乌克兰地盾，中第聂伯省绿岩带的形成可分为两个阶段:3.19~3.14 Ga 火山系列岩石和 3. 07 Ga 铁镁质熔岩（Sukach et al.，2014）。同时期还形成萨尔蒂科夫卡（ Saltykovka）杂岩（ 3029 Ma 和 3091 Ma）（Lobach-Zhuchenko et al.，2017）和位于亚速省（Azov province）中部、北部和西部的绿岩带（ 3095 Ma 和 3157 Ma）。
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芬诺斯堪迪亚（Fennoscandian）地盾在 3 个地区发现了 3.1 Ga 左右 TTG 片麻岩:①芬兰北部元古代岩石中一个小穹隆的奥长花岗质片麻岩，其锆石 U-Pb 和 Sm-Nd 全岩年龄均为 3.1 Ga（Kröner et al.，1981，1990）; ②芬兰中部卡累利阿克拉通最西端的伊萨尔米（ Lisalmi）杂岩，由花岗闪长岩（ 3095 ± 18 Ma）、石英闪长岩（3173±7 Ma）、混合角闪岩、麻粒岩和火成岩组成（ Mänttäri et al.，2002; Lauri et al.，2011; Mikkola et al.，2011）; ③伏德洛泽罗（Vodlozero）省西北部存在英云闪长岩（ 3.2~3.1 Ga）和混合岩（Sergeev et al.，2007，2008）。
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1.7 南极洲
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3.1 Ga 左右岩石分布于南极洲面向印度洋扇区的 Denman 冰川地区、鲁克（Ruker）杂岩、恩德比地（Enderby Land）的纳皮尔（Napier）杂岩和 Mawson 海岸沿线。另外，3.1 Ga 左右花岗质片麻岩、英云闪长岩、辉长岩等岩石分布于横贯南极山脉的 Nimrod 杂岩中（ Sheraton et al.，1987; Grew et al.，1988; Boger et al.，2006，2008; Mikhalsky et al.，2006，2010）。
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2 3.1 Ga 左右岩石的岩石类型与岩石学特征
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全球超过 10 个克拉通中见有 3.1 Ga 左右岩石。约 50%为花岗岩，其中 30%为 TTG 岩石，以奥长花岗岩和英云闪长岩为主，花岗闪长岩很少出露; 约 15%为未被具体命名的片麻岩，其中格陵兰岛发现最多，其余分布在南极、美洲和非洲的部分克拉通; 约 7% 为变质沉积岩，包括变质泥岩和变质砾岩，主要分布在华北、达瓦、南非、圣弗朗西斯科等克拉通; 约 10%为基性岩、超基性岩，根据前人文献所述，多为地幔物质直接侵入到地壳中; 华北克拉通塔里木、印度库格地块等地发现有高级变质作用形成的麻粒岩，皮尔巴拉、库格地块和萨尔玛提亚等克拉通中发现的流纹岩和凝灰岩等火山喷发物质，是地壳生长最直接的证据。
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3.1 Ga 左右岩石数据点在 An—Ab—Or 图中大多数落于英云闪长岩区与奥长花岗岩、花岗岩交界处（图4a），结合前人报道的岩石岩性类型，说明 3.1 Ga 左右岩石以英云闪长岩和奥长花岗岩为主，数据显示 3.1 Ga 左右岩石岩性和分布十分复杂。华北克拉通鞍山地区和塔里木克拉通主要为奥长花岗岩，扬子克拉通主要为花岗岩; 皮尔巴拉克拉通和西南格陵兰数据点落于英云闪长岩区域; 花岗闪长质岩基本只位于西伯利亚克拉通和萨尔玛提亚克拉通，其他地区几乎没有花岗闪长岩区数据点; 卡普瓦尔克拉通和刚果克拉通数据点主要在奥长花岗岩和花岗岩区，其他岩性区域几乎没有。 3.1 Ga 左右岩石多为过铝质岩石（图4b），只有极少数印度克拉通岩石位于准铝质区域。英云闪长岩和花岗闪长岩具有较高 A/ NK 值。岩石数据点普遍位于流纹岩区和英安岩等酸性岩区（图4c）（邓晋福等，2015）。西南格陵兰、圣弗朗西斯科克拉通、亚马逊克拉通、苏必利尔克拉通、怀俄明克拉通和西伯利亚克拉通岩石属于钙碱性系列，少部分位于拉斑系列（图4d）; 而皮尔巴拉克拉通和华北克拉通一部分岩石位于高钾钙碱性系列（图4d）。
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图4 （a）全球约 3.1 GaTTG 岩石的 An—Ab—Or 图解（数据来源同图2）;（b）全球约 3.1 GaTTG 岩石的 A/ CNK—A/ NK 图解（数据来源同图2）;（c）全球约 3.1 GaTTG 岩石的 ATS 图解（数据来源同图2），（ d）全球约 3.1 GaTTG 岩石的 SiO2— K2O 图解（数据来源同图2）
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Fig.4 (a) An—Ab—Or diagram of global~3.1 Ga old TTG rocks ( source of data same as Fig.2) ; ( b) A/ CNK vs A/ NK diagram of global~3.1 Ga old TTG rocks (source of data same as Fig.2) ; (c) ATS diagram of global~3.1 Ga old TTG rocks (source of data same as Fig.2) , (d) SiO2 vs K2O diagram of global~3.1 Ga old TTG rocks (source of data same as Fig.2)
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图5 全球约 3.1 Ga TTG 岩石锆石年龄-εHf（t）图解（数据来源同图2; 图例同图4）
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Fig.5 εHf (t) vs. Zircon age diagram for rocks from the world (source of data same as Fig.2; figure legend same as Fig.4)
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3 3.1 Ga 左右锆石的 Hf— O 同位素特征
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笔者等收集了全球约 3.1 Ga 岩石主微量元素数据、锆石 Hf—O 同位素数据，选取不谐和度小于 15%的锆石207 Pb / 206 Pb 表面年龄与相应锆石的 Hf 同位素进行分析。全球 3.1 Ga 左右 TTG 岩石的锆石 Hf 同位素具有以下特征:
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（1）不同地区 εHf（t）表现出明显差异，如辛格布姆克拉通、巴斯塔尔克拉通、华北克拉通、扬子克拉通、卡普瓦尔克拉通和皮尔巴拉克拉通、高勒克拉通 εHf（t）值多为正值（-16.18~12.67），但位于亏损地幔线之下，说明这些地区岩石主要为新生地壳，同时伴随有强烈壳内再循环作用; 而圣弗朗西斯科克拉通、拉普拉塔克拉通、亚马逊克拉通、苏必利尔克拉通、怀俄明克拉通、西伯利亚克拉通、萨尔玛提亚克拉通 εHf（t）值多为负值（-12.3~5.96），说明这些地区约 3.1 Ga 岩石主要为壳内再循环产生，但有少量地幔物质添加。
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图6 锆石 δ18O 与 εHf（t）、 207 Pb / 206 Pb 年龄的关系（数据来源同图2; 图例同图4）
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Fig.6 Diagrams of εHf (t) and 207 Pb / 206 Pb versus δ18O (source of data same as Fig.2; figure legend same as Fig.4)
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（2）同一地区不同时代的锆石 Hf 同位素组成也呈现明显差异，如华北克拉通、达瓦克拉通、辛格布姆克拉通，随着年龄减小，εHf（t）呈现下降趋势，同时负值的数据点明显增多，说明 3.1 Ga 左右早期，这些地区主要为新地壳的形成，到 3. 0 Ga 左右时期则变为古老地壳的再循环。总体而言，随着时间的推移，地幔物质的添加减少，壳内再循环作用增加。
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约 3.1 Ga 锆石的氧同位素具有类似该时期地幔的 δ 18O 值，部分 δ 18O 值略有升高（图6）。华北克拉通锆石 δ 18O 范围为+1.47‰~+8.93‰。卡普瓦尔克拉通锆石 δ 18O 范围为+3.9‰~+7.4‰。达尔瓦克拉通锆石 δ 18O 值在+4.14‰~+6.51‰之间，平均为+5.15‰。尽管许多锆石 δ 18O 值与地幔熔体处于平衡状态，但部分锆石 δ 18O 值较高（ δ 18O 为 +8.93‰）（图6），说明存在上地壳物质熔融或混染。部分高 δ 18O 值分布在太古宙岩浆锆石范围以上，表明玄武岩源经历了一定的低温蚀变，或发生地壳混染。大多数锆石具有一致的 Hf 同位素组成。这些观测结果与大规模岩浆活动对高 δ 18O 沉积岩的同化作用不一致，因为同化作用会导致初始 εHf 值发生较大变化。由此可见，华北克拉通和卡普瓦尔克拉通 3.1 Ga 左右岩石中至少有一部分源岩在熔融前经历了低温蚀变而产生 TTG 熔体。特别是 3.1 Ga 左右华北克拉通锆石，δ 18O 值低至 + 1.47 ‰。它们可能记录了 3.1 Ga 左右岩浆混合作用事件的原始同位素特征。综上所述，3.1 Ga 左右岩浆锆石 δ 18O 变化范围较大，成因各不相同，3.1 Ga 左右地壳演化过程可能比之前认为的更为复杂。
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图7 全球典型地区约 3.1 Ga 岩石哈克图解（数据来源同图2; 图例同图4）
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Fig.7 Harker diagrams for selected major elements of the~3.1 Ga rocks (source of data same as Fig.2; figure legend same as Fig.4)
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4 3.1 Ga 左右岩石的地球化学特征
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现有数据表明，主量元素氧化物如 TiO2、Fe2O3、 MnO、MgO、CaO、P2O5 与 SiO2 之间存在明显负相关性（图7）。能够反应压力变化的 Al2O3 与 SiO2 之间存在微弱负相关关系。 Na2O、K2O 与 SiO2 之间存在明显正相关性。值得注意的是，印度地区 3.1 Ga 左右岩石存在 SiO2 含量低、MgO 含量高的英云闪长质岩石，其稀土总量高，轻重稀土没有明显分异，存在较强 Eu 负异常。结合该区其他同时代岩石特征，这些英云闪长岩可能是基性岩浆结晶分异形成。华北克拉通的 TiO2、MgO、Fe2O3 值普遍更高，而 MnO 值与其他地区相似（图7），且明显低于皮尔巴拉克拉通岩石样品，其余主要元素氧化物具有相同的分布趋势。
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稀土元素是反映岩浆源区性质、岩浆起源与演化过程的良好地球化学指标。华北克拉通、皮尔巴拉克拉通、亚马逊克拉通、刚果克拉通和西南格陵兰部分地区的稀土元素配分样式基本相同（图8），呈现出明显右倾趋势，表明轻稀土元素比较富集，而重稀土元素相对亏损，显示出强烈分馏的稀土配分模式。此外，铕存在轻微负异常，说明 TTG 岩浆经历了少量斜长石分离结晶。这些相似特征可能暗示这些地区的岩石可能具有相似的源区、成因模式和构造背景。相比之下，印度和西南格陵兰部分地区样式与其他地区有所不同，轻重稀土分异不明显，具有较为强烈铕正异常。由此可见，3.1 Ga 左右岩石在全球表现出明显差异，TTG 岩石形成过程显示出明显多样性，岩浆作用过程十分复杂，表明该时期陆壳的演化程度相对较高。
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图8 全球典型地区 3.1 Ga 左右岩石稀土元素配分图;（a）全球 3.1 Ga 左右 TTG 岩石稀土元素配分图;（b）中国地区 3.1 Ga 左右 TTG 岩石稀土元素配分图;（c）非洲地区 3.1 Ga 左右 TTG 岩石稀土元素配分图;（ d）澳大利亚地区 3.1 Ga 左右 TTG 岩石稀土元素配分图;（e）西格陵兰地区 3.1 Ga 左右 TTG 岩石稀土元素配分图;（ f）印度地区 3.1 Ga 左右 TTG 岩石稀土元素配分图（球粒陨石数据来自 Sun and McDonough，1989）
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Fig.8 REE distribution patterns of the~3.1 Ga rocks from the word: (a) global REE distribution patterns for~3.1 Ga rocks: (b) REE distribution patterns of the~3.1 Ga rocks in China: (c) REE distribution patterns of the~3.1 Ga rocks in Africa: (d) REE distribution patterns of the~3.1 Ga rocks in Australia: (e) REE distribution patterns of the~3.1 Ga rocks in West Greenland: (f) REE distribution patterns of the~3.1 Ga rocks in India (The chondrite values are from Sun and McDonough, 1989)
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图9 全球典型地区 3.1 Ga 左右 TTG 岩石原始地幔标准化微量元素蛛网图:（a）中国;（b）澳大利亚;（c）非洲地区;（d）西格陵兰地区;（e）南美洲地区地区;（f）北美洲地区;（g）欧洲地区;（h）印度（地幔标准化数据 Sun et al.，1989）
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Fig.9 Primitive mantle normalized trace elements spidergrams for~3.1 Ga TTG rocks from the world: (a) China; (b) Australia; (c) Africa; (d) the west Greenland region; (e) the South American region; (f) the North American region; (g) European region; (h) Indian region (The primitive mantle values are from Sun and McDonough, 1989)
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3.1 Ga 左右 TTG 岩石微量元素原始地幔标准化蛛网图如图所示（图9）。图中数据显示出，中国 3 个主要克拉通、澳大利亚 4 个主要克拉通、非洲 2 个主要克拉通、西南格陵兰大部分地区、南美洲 2 个主要克拉通和西伯利亚克拉通的 3.1 Ga 左右岩石整体呈现出 Th、U、K、Pb 明显富集，Nb、Ta、P、Sm、Ti 相对亏损，显示出明显的岛弧配分样式。北美洲怀俄明克拉通则表现出 Ba、Ce、Ti 相对亏损和 Nb、Ta、Pb 相对富集的特征。印度 4 个主要克拉通则显示出 Ba、Nb、Pb 亏损和 Th、Ta、Hf 等元素富集。这进一步说明该时期 TTG 岩石的形成条件和构造背景呈现出多样性。
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La / Yb 和 Sr/ Y 值被认为是反应 TTG 岩石形成压力的重要参数。在 3.1 Ga 左右岩石样品中，Sr/ Y 的值位于 0~479 之间，Y 的值位于 0~43.9×10-6 之间，呈现出较大变化范围。然而，大多数样品 Sr/ Y 值小于 120 且 Y 值小于 50×10-6，这表明 3.1 Ga 左右 TTG 岩石多形成于中—低压条件下，但也有少数岩石表现出高压的特征。岩石样品的 La / Yb（1~1088）、 Ce / Sr（1~473）值变化范围同样较大。从众多地球化学元素的比值变化可以看出，全球各地区 3.1 Ga 左右岩石的成因与形成环境是由巨大差距的，结合图10c、d，可以说 3.1 Ga 左右 TTG 岩石的形成条件与构造背景十分复杂，并非均处于相同的构造机制之下。
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综上所述，全球 3.1 Ga 左右 TTG 岩石 SiO2 平均含量为 65.5%，MgO 平均含量为 4.4%，同时 MgO、Ni、 Cr 值比较低，Mg #值中等偏高，Sr 值为中等程度等主微量数据，这些特征表明 3.1 Ga 左右 TTG 岩石可能来自玄武质岩石源区，部分源区发生低温蚀变。源区为约 3.3 Ga 时期从轻度亏损的地幔部分熔融形成。
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5 3.1 Ga 左右岩浆事件与地壳生长
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5.1 3.1 Ga 左右岩浆事件
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陆壳大规模生长的主要过程为地幔提取玄武质岩浆，玄武质岩石部分熔融形成 TTG 岩石，TTG 岩石通过壳内再循环形成壳源花岗岩（Moyen et al.，2011）。根据已有资料显示，全球 20 余个太古宙克拉通发现了 3.1 Ga 左右锆石，10 余个克拉通中发现了 3.1 Ga 左右岩石。根据岩石锆石年龄分布图，已发现岩石的年龄在 3000~3200 Ma 间连续分布，有两个明显年龄峰值，分别为 3.15 Ga 和 3. 05 Ga。其中 3.15 Ga 峰在全球范围内都有体现（南美洲除外），这说明 3.15 Ga 岩浆事件是一次全球性质事件。全球 3.1 Ga 左右岩石 Hf 同位素数据显示，多数锆石具有正 εHf（t）值和与锆石结晶年龄接近（年龄差<200 Ma）的模式年龄，这说明 3.1 Ga 左右时期全球确实发生了一次全球性地壳生长。同时，部分锆石 εHf（t）为负值，并且具有与锆石结晶年龄相差较远的模式年龄，说明 3.1 Ga 左右时期不仅是新生地壳生长，同时也发生了古老地壳物质重熔。
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根据现有地壳年龄数据，学者们提出了多种地壳生长曲线。从图11a 中可以看出，在部分学者提出的地壳生长曲线中，3.1 Ga 左右时期地壳生长速率或多或少存在转折趋势，说明地壳生长演化在该时期发生了变化。同时，在大陆曲线相关图（图11b）中，地壳改造速率在该时期呈现下降趋势，地幔温度开始下降，地壳厚度由下降趋势转变为上升趋势，这支持了部分学者的观点，即地壳的形成机制在 3.2~3. 0 Ga 期间发生明显转变，从垂向生长逐渐过渡为水平生长（Dhuime et al.，2015; Hawkesworth et al.，2020; Johnson et al.，2019; Chowdhury et al.，2020）。
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综上所述，约 3.1 Ga 发生了一次较大规模的地壳增生事件。
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5.2 3.1 Ga 左右构造环境
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前人研究表明，3.1 Ga 左右时期的 TTG 岩石可能是在不同构造背景下通过不同过程形成的（Palin et al.，2016），包括交代重力差异沉降、热管构造和滞留盖构造、俯冲洋壳和加厚弧中变质玄武岩（角闪岩）的熔融（Nagel et al.，2012; Polat et al.，2015; 徐楠等，2023）。这些成因可以概括为两种认识:①板片俯冲到地壳之下后，板片熔融形成; ②深部地壳物质部分熔融形成。 Dhuime 等（2015）通过研究 13125 个来源和地质状况未知的火山岩和深成岩样品的组成，提出了新生地壳的 Rb / Sr 值在 3.2~3. 0 Ga 急剧增加的认识（Dhuime et al.，2015）。 Johnson 等（2019）研究表明太古宙 TTG 中 K2O/ Na2O、Sr/ Y 和 LaN / YbN 值在 3.3~3. 0 Ga 过渡时期发生显著变化。这些结果表明 3.3~3. 0 Ga 之间全球构造可能发生了根本的转变，从非板块构造停滞—盖层状态到移动—盖层状态（Dhuime et al.，2015; Hawkesworth et al.，2020; Johnson et al.，2019; Chowdhury et al.，2020）。然而，有学者认为，这种变化也可能是地壳长期冷却而导致相容和不相容元素浓度发生重大变化的结果，而不是地壳主要成分变化或构造样式发生变化的结果（Keller et al.，2020; Windley et al.，2021）。
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图10 （a）YbN—（La / Yb）N 图解（底图据 Wan et al.，2005）;（b）Y—Sr/ Y 图解（底图据 Zheng Jianpeng et al.，2009）;（c）La / Yb—Sr/ Y 图解（底图修改自 Moyen et al.，2011）;（d）Y—Ce / Sr 图解（底图修改自 Moyen et al.，2011）（图例同图4）
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Fig.10 (a) YbN vs. (La / Yb) N diagram (after Wan et al., 2005) ; (b) Y vs. Sr/ Y diagram (after Zheng Jianpeng et al., 2009) , (c) La / Yb vs. Sr/ Y diagram (after Moyen et al., 2011) . (d) Y vs. Ce / Sr diagram (after Moyen et al., 2011) (figure legend same as Fig.4)
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中太古代 Ivisaartoq（西格陵兰）和新太古代 Schreiber—Hemlo 绿岩带（加拿大）太古宙火山岩岩浆期后元素活动性及微量元素研究表明变质过程使微量元素在某些岩性中丢失，同时在其他岩性中得到，具有广泛的互补性（ Ordóñez-Calderón et al.，2008; Polat et al.，2012）。然而，在 3.1 Ga 左右岩石的微量元素数据均只有显示 Pb 正异常，没有 Pb 亏损，这表明 Pb 正异常并不是后期变质作用的结果。结合 Th、U、K 元素明显富集，Nb、Ta、P、Sm、Ti 元素相对亏损特征，3.1 Ga 左右岩石的形成与可能俯冲作用密切相关。 Hildebrand 等人（2018）指出 TTG 自 3.8 Ga 以来主要来自板片熔融而不是加厚的弧岩浆，由此便有了古太古代以来俯冲作用就已经开始的观点（Hidebrand et al.，2018）。
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然而，俯冲作用无法完全解释 3.1 Ga 左右 TTG 岩石和绿岩带的一些特征:
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（1）如果俯冲过程导致新地壳形成，那么在不同区域可能会识别出不同的年龄峰，从而形成一个全球年龄的连续。然而，在 3.1 Ga 左右时期，全球克拉通基底 70%左右为 TTG 侵入体，这些侵入体几乎同时侵入了当时存在的各个古陆核，这是俯冲作用无法解释的。
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Fig.11 The global crustal growthcurves (after Wan Yusheng et al., 2022&) and Crustal growth curves (after Fan Hailong et al., 2023&)
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（2）全球太古宙克拉通典型构造是穹隆构造，主要是由 TTG 岩石底辟形成，与俯冲带形成的大规模逆冲带、线性构造带、韧性剪切带等构造样式有所不同。
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（3）3.1 Ga 左右时期尚未发现确定俯冲带存在的重要标志———双变质带。尽管在地球化学上发现俯冲带存在的一些证据，但野外地质记录却不相符。因此，越来越多的学者认为，地球早期存在的长英质大陆是某种前板块构造体制下的产物（Hamilton et al.，2011，2019; Brown et al.，2020）。
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综合前人研究，3.1 Ga 左右时期全球地壳演化机制存在垂向生长和水平演化两种机制的并行。深部地壳部分熔融是地壳演化的重要过程，其形成机制因不同构造单元和地质背景而异。部分地区花岗岩具有相对平坦的 HREE 模式，以及高 Zr/ Sm、低 Gd / Yb、 Dy / Yb、Nb / Ta 值说明岩石主要由古老地壳部分熔融而来，并且这些 TTG 片麻岩样品具有低 Mg# 值，以及极低的 Cr 和 Ni 浓度，这排除了地幔物质为岩浆来源做出贡献的可能性，并表明 TTG 岩浆可能是由早期存在的地壳岩石部分熔化形成的，而不是俯冲的海洋地壳形成的（Ao Wenhao et al.，2021）。与此类似的地区还有圣弗朗西斯科克拉通 Gavião 地块（Medeiros et al.，2017; Lopes et al.，2021）、西格陵兰岛基亚地体（Gardiner et al.，2019; Kirkland et al.，2020）、萨尔玛西亚克拉通东部花岗—绿岩带（ Lobach-Zhuchenko et al.，2017）等。这些地区 3.1 Ga 左右 TTG 主要通过地幔柱影响地壳下部，下地壳部分熔融产生的。另有如高勒克拉通部分岩石因含放射性元素（如铀、钍）热量释放而熔融，而非因地幔柱的影响而产生的熔融（Fraser et al.，2010）。总体来说，深部地壳的部分熔融机制在不同地质环境下的表现是多样的，其主导因素包括构造背景、地幔热源以及地壳物质的组成。而其余地区具有高 LILE（大离子亲石元素）浓度、富 Nb 和 Ta 浓度（以及 Nb / La 比率）高于典型的岛弧和大陆玄武岩、εHf（t）值具有幔源特征等类似现代大洋岛弧的地球化学特征认为是在早期衍生的洋壳俯冲到早期陆壳下形成，类似的构造环境也在西达瓦克拉通 Nugggihalli 绿岩带（Sameer et al.，2020）、库尔格地块（Yu Bing et al.，2022; Anoop et al.，2021）、圣弗朗西斯科克拉通南部绿岩带（Marimon et al.，2022）、怀俄明克拉通（ Smithies et al.，2003）等地区得到表现，均显示出与岛弧或俯冲背景相关的地球化学特征。另有地区记录了近陆相扇组合—水下三角洲前缘组合—浅海陆架的沉积环境，表明这些地区可能与古代洋壳俯冲及岛弧活动密切相关（De et al.，2020; Sindhuja et al.，2022）。总体而言，以上地区的地质证据表明，俯冲板片部分熔融在这些区域的地壳演化中扮演了关键角色。其岩浆活动与岛弧形成、洋壳俯冲等环境密切相关，表明在地球早期，俯冲板块是推动地壳动态演化的重要因素。
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总体来看，3.1 Ga 左右岩石的成因呈现多样性，包括俯冲作用导致的板块边缘增生和洋底高原加厚下地壳部分熔融。下地壳部分熔融在大部分地区都是存在的，而板块俯冲只在少量地区起作用。这说明至少在 3.1 Ga 左右时，某种形式的板块构造运动已经在地球上开始，但此时起主导作用的构造样式仍然是地幔柱主导的垂向构造。
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6 总结
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（1）全球各个地区 TTG 岩石的资料表明，中太古代（3.15 Ga 和 3. 0 Ga）发生了两次全球性的岩浆活动。 3.1 Ga 左右岩石遍布全球各个大陆，现今主要集中在北半球，南半球数量较少。岩石普遍遭受后期变质作用改造形成片麻岩，原始岩石几乎不可见。 3.1 Ga 左右岩石以英云闪长岩和奥长花岗岩为主，呈现出过铝质的特征。华北克拉通、塔里木、印度库格地块等地发现有高级变质作用形成的麻粒岩，皮尔巴拉、库格地块和萨尔玛提亚等克拉通中发现有流纹岩和凝灰岩等火山岩，具有一定的地区独特性。
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（2）中国、澳大利亚、非洲、西南格陵兰、南美洲和西伯利亚克拉通的 3.1 Ga 左右岩石整体呈现出轻稀土富集，重稀土亏损的右倾模式，铕明显异常; 微量元素整体存在 Th、U、K、Pb 相对富集，Nb、Ta、P、Sm、Ti 相对亏损，北美洲怀俄明克拉通和印度主要克拉通微量元素与其他地区有明显差异。全球 3.1 Ga 左右锆石的 εHf（t）具有明显差异; 同一地区的锆石 Hf 同位素组成也有明显差异。大部分锆石 δ18O 值与地幔熔体处于平衡状态（ + 5.3 ± 0.6‰），但也有部分锆石 δ18O 值较高，达+8.93‰，可能表示上地壳物质的熔融。
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（3）3.2~3. 0 Ga 时期岩石组合、全岩地球化学和锆石 O—Hf 同位素在各个克拉通上存在差异，表明该时期岩浆作用过程十分复杂，地壳生长的机制可能是垂向和水平演化两种方式并行。
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摘要
全球克拉通 90%的陆壳可能是在太古宙形成,集中在 3. 5 ~ 3. 1 Ga、2. 8 ~ 2. 7 Ga、2. 6 ~ 2. 5 Ga 3 个阶段,2. 8~ 2. 7 Ga 和晚期 2. 6~ 2. 5 Ga 时期的岩石保留较多,地壳增生与改造机制研究较多,受样品稀少限制,3. 0 Ga 之前的岩浆事件与陆壳形成演化研究相对薄弱,早前寒武纪岩浆事件与地壳增生方式仍存在争议。本文系统总结了全球中太古代(主要为 3. 2~ 3. 0 Ga 期间)岩石的锆石年龄、岩石类型、全岩地球化学和锆石 Lu—Hf—O 同位素特征。主要认识包括:①3. 2~ 3. 0 Ga 时期岩石在全球各大洲均有分布,现今主要集中在北半球,而南半球的数量相对较少;②岩石的锆石年龄峰值集中在约 3. 05 Ga 和约 3. 15 Ga 两个时期;③岩石的主要岩性为英云闪长岩和奥长花岗岩,具有过铝质的特征,不同地区呈现出不同的岩石组合,展现出一定的地区独特性;④不同地区岩石锆石的 εHf(t)值表现出明显差异,反映了岩石起源和演化历史的差异性。大部分锆石的 δ18O 值与地幔熔体处于平衡状态, 也有部分锆石的 δ18O 值较高,可达+8. 93‰,暗示岩石源区经历了一定的低温蚀变或地壳物质的混染; ⑤岩石呈现轻稀土元素富集、重稀土元素亏损的右倾模式,铕元素异常明显。整体上 Th、U、K、Pb 等元素相对富集,而 Nb、Ta、P、 Sm、Ti 等元素相对亏损。综合研究表明:①3. 1 Ga 左右 TTG 岩石可能由经历低温蚀变的玄武质岩石部分熔融形成。 Hf 同位素特征显示,该时期玄武质岩石多数为 3. 3 Ga 左右时期由轻度亏损的地幔部分熔融形成。 ②中太古代早期 (主要为 3. 2~ 3. 0 Ga 期间)发生了一次全球性质的岩浆活动和地壳增长事件,峰值期在约 3. 05 Ga 和约 3. 15 Ga。 ③类似于现代板块运动的构造体制在中太古代已经启动。
Abstract
Objectives: During the Archean, approximately 90% of the global craton’s crust may have formed, particularly during the 3. 5~3. 1 Ga, 2. 8~2. 7 Ga, and 2. 6~2. 5 Ga. More rocks are preserved from the 2. 8~2. 7 Ga and late 2. 6~2. 5 Ga periods. While the mechanisms of crustal accretion and remodeling are frequently investigated, research is limited by the scarcity of samples, resulting in relatively weak studies on magmatic events and crustal formation prior to 3. 0 Ga. Furthermore, the understanding of earlier Preambrian magmatic events and crustal accretion remains controversial.
Methods: Building upon previous research, this study summarizes and compares zircon ages, rock types, wholerock geochemistry, and zircon Lu—Hf—O isotope signatures of global Mesoproterozoic rocks, primarily from the 3. 2 ~3. 0 Ga period, in order to concluding the global magmatic events and crustal evolution patterns around 3. 1 Ga.
Results: Rocks from the 3. 2~3. 0 Ga period are found across all continents, with a predominant concentration in the Northern Hemisphere, while the Southern Hemisphere exhibits a relatively smaller number in present. The peak zircon ages of these rocks are concentrated around 3. 05 Ga and 3. 15 Ga. The main lithologies include stromatolitic and peraluminous aeolian granite. The primary lithologies of the rocks consist of angstromatolite and aeolian granite with peraluminous characteristics. Different regions exhibit distinct rock assemblages, and the εHf(t) values of zircons from these regions demonstrate significant variations, reflecting differences in the origin and evolutionary history of the rocks. Most zircons have δ18O values in equilibrium with mantle melt; however, some zircons exhibit higher δ18O values, reaching + 8. 93‰, suggesting that the rock source areas underwent lowtemperature alteration or mixing with crustal materials. The rocks display a right-tilted pattern characterized by an enrichment of light rare earth elements and a deficit of heavy rare earth elements, with pronounced europium anomalies. Overall, elements such as Th, U, K, and Pb are relatively enriched, whereas elements like Nb, Ta, P, Sm, and Ti are comparatively deficient.
Conclusions: The ~ 3. 1 Ga rocks likely formed through partial melting of a basaltic source region that experienced low-temperature alteration. This source region originated from partial melting of a mildly deficient mantle around ~3. 3 Ga. A global event of magmatism and crustal growth occurred during the early Mesoarchean (primarily between 3. 2 and 3. 0 Ga), with peaks at approximately 3. 05 Ga and 3. 15 Ga. Furthermore, tectonic regimes akin to modern plate motions began to emerge in certain areas during the Mesoarchean.
Keywords
Mesoarchean ； crustal accretion ； magmatic event ； TTG rocks
