2020, Vol. 36
2. 北京大学地球与空间科学学院, 北京 100871
2. School of Earth and Space Sciences, Peking University, Beijing 100871, China
大多数弧岩浆岩的形成被认为俯冲板片脱水有关，脱水作用所释放的含水富挥发分流体引发上覆地幔楔部分熔融形成玄武质岩浆，并可进一步分异形成中-酸性岩浆岩，构成特征的玄武岩-安山岩-英安岩-流纹岩组合(Gill et al., 1981)。然而，在与大洋俯冲有关的弧背景下，也形成一些特殊的岩石，如Defant and Drummond(1990)提出岛弧环境下存在一类具有高Al2O3、高Sr、低Y和Yb等地球化学特征特殊的火成岩，主要为英安岩及与其成分相当的英云闪长岩、奥长花岗岩等，因最先由Kay(1978)在美国阿留申群岛中的埃达克(Adak)岛发现，而称其为埃达克岩(adakites)，并认为其为年轻的(＜25Ma)，因而是热的洋壳在榴辉岩相条件下部分熔融形成的火成岩。埃达克岩提出之后引起了国内外学者的广泛关注。研究中发现埃达克岩一般不与岛弧玄武岩或玄武安山岩共生，但可以与富Nb或高Nb玄武岩共生(Sajona et al., 1996；Martin，1999；Defant and Kepezhinskas, 2001；王强等, 2001, 2008；Wang et al., 2003, 2008a；Castillo，2012)，很多情况下还可以与高镁安山岩共生，组成埃达克岩-高镁安山岩-富Nb玄武岩的岩石组合，这一典型的岩石组合在世界各地新生代至早前寒武纪的地体中均有分布(Kelemen，1995；Drummond et al., 1996；Martin，1999；Manikyamba et al., 2009；Polat and Kerrich, 2001；Shchipansky et al., 2004；王强等，2006；Peng et al., 2012a, b；Guo et al., 2013；Liu et al., 2014；Shen et al., 2014)，不同于由俯冲流体交代地幔楔熔融产生的玄武岩-安山岩-英安岩-流纹岩构成的弧岩浆岩组合，并通常被认为是岛弧环境下俯冲板片熔融的证据(Drummond et al., 1996；Kepezhinskas et al., 1996；Sajona et al., 1996；Aguillón-Robles et al., 2001；Defant and Kepezhinskas, 2001；Wang et al., 2003, 2007, 2008a；Castillo, 2006, 2012；王强等，2006)，其中富Nb玄武岩是由俯冲板片熔融产生的埃达克质熔体交代的地幔楔橄榄岩熔融的产物(Kepezhinskas et al., 1996；Sajona et al., 1996；Defant and Kepezhinskas, 2001；Wang et al., 2008a)。
柴北缘以发育榴辉岩、石榴橄榄岩、高压麻粒岩及相关片麻岩组成的超高压(UHP)变质带为特征，其主体被普遍认为是早古生代大陆深俯冲的产物，并已得到广泛研究(Yang et al., 1998, 2006；Zhang et al., 2000, 2004, 2008a, 2009a, b，2010；Song et al., 2003, 2005, 2006, 2007；张建新等, 2005, 2008；Mattinson et al., 2006a, 2007；Yang and Powell, 2008；Yu et al., 2013, 2014；于胜尧等，2014)。然而，关于柴北缘是否保存大洋俯冲的物质组成以及大洋俯冲的时代等问题却存在很大争议。在柴北缘地区，与UHP变质带在空间上伴生着一套浅变质的早古生代滩间山群火山-沉积岩系，其中的火山岩组合以变质基性-中性火山岩为主，可见少量酸性火山岩(邬介人等，1987；赖绍聪等，1996；史仁灯等, 2003, 2004；王惠初等，2003；Shi et al., 2006)。一些学者认为其为一套裂谷型建造(邬介人等，1987)，而多数学者认为滩间山群形成于大洋俯冲有关的弧或弧后构造环境，但其具体性质还有不同认识。不同的学者根据其岩石组合及火山岩的地球化学特征等，在滩间山群中厘定有蛇绿混杂岩(赖绍聪等，1996；孙延贵等，2000；王惠初等，2003)、弧后盆地型蛇绿岩(王惠初等，2005；朱小辉等，2014)、埃达克岩(史仁灯等，2003；Shi et al., 2006)、岛弧火山岩(王惠初等，2003；史仁灯等，2004；高晓峰等，2011)等。此外，目前对于滩间山群形成的年代学数据也有所欠缺，因此，滩间山群的形成背景及形成时代值得进一步研究。最近，我们在柴北缘东段都兰查查香卡农场一带的滩间山群中新厘定出了一套埃达克岩-富Nb玄武岩组合。在野外工作基础上，我们对其进行了地球化学、锆石U-Pb定年及Hf同位素分析等工作，来确定其形成时代及形成的构造环境，从而探讨柴北缘大陆深俯冲作用之前大洋俯冲的构造热环境、时限及地壳增生机制。
1 地质背景及样品野外关系 1.1 地质背景柴北缘构造带位于青藏高原的东北部，呈北西-南东向展布，南以柴北缘断裂与柴达木盆地(地块)相接，北以宗务隆构造带与祁连造山带(地块)相隔，向西被阿尔金断裂所切，向东被温泉断裂切割。柴北缘构造带主要由柴北缘高压-超高压变质带、欧龙布鲁克地块以及空间上与超高压变质带伴生的滩间山群浅变质火山-沉积岩系组成(图 1)。
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图 1 柴北缘构造带地质简图 Fig. 1 Schematic geological map of North Qaidam tectonic belt |
柴北缘超高压(UHP)变质带分布在欧龙布鲁克地块和柴达木地块之间，西起鱼卡地区，东至都兰沙柳河地区，呈北西-南东向展布(图 1)。变质带可进一步划分出四个次级变质单元，自西向东依次为：鱼卡-落凤坡榴辉岩-片麻岩单元(YLU)；绿梁山石榴橄榄岩-高压麻粒岩单元(LLU)；锡铁山榴辉岩-片麻岩单元(XTU)和都兰榴辉岩-片麻岩单元(DLU)(张建新等，2005；Zhang et al., 2008b, 2009b)(图 1)。带内的鱼卡榴辉岩、锡铁山榴辉岩、都兰榴辉岩和副片麻岩中均已发现柯石英包裹体；绿梁山石榴橄榄岩锆石中保存有金刚石(Yang et al., 2001；Song et al., 2003, 2005；Zhang et al., 2009a, b，2010；Liu et al., 2012)。这些超高压变质作用证据表明柴北缘大陆地壳曾俯冲到80~120km的地幔深度。
欧龙布鲁克地块(又称全吉地块)位于柴北缘UHP变质带北部，二者以断层为界，北以宗务隆构造带与祁连造山带(地块)相隔(图 1)。它被认为是与塔里木克拉通具有亲缘性的大陆克拉通碎片(Chen et al., 2012, 2013b；Gong et al., 2012)。欧龙布鲁克地块具有典型的二元结构，即由经历中-高级变质作用的古元古代变质基底与覆盖于其上的沉积盖层组成(陆松年，2002；陆松年等, 2002a, b，2006；陈能松等，2007)。它的变质基底主要包括古元古代早期的德令哈杂岩及古元古代中晚期的达肯大坂群及中元古代的万洞沟群，沉积盖层主要为全吉群及滩间山群(陆松年，2002；陆松年等，2002a；Chen et al., 2012, 2013a)。德令哈杂岩主要形成于2.39~2.34Ga(陆松年，2002；陆松年等，2002a；郝国杰等，2004；Gong et al., 2012；巴金等，2012；Wang et al., 2015；Yu et al., 2017；路增龙等，2017；He et al., 2018；Lu et al., 2018)；达肯大坂岩群的形成稍晚于德令哈杂岩(2.32~1.96Ga)，二者共同经历了1.96~1.8Ma的多期区域变质岩浆事件(张建新等，2001；Wang et al., 2008b；Chen et al., 2009b, 2012, 2013a；Gong et al., 2012；Liao et al., 2014；路增龙等，2017；Yu et al., 2017)。地块还存在1.80~1.76Ga的环斑花岗岩侵入体(Xiao et al., 2004；陆松年等，2006；Chen et al., 2013b)及1.71Ga的富Nb辉长岩(Liao et al., 2018)。
近年来，一些学者在欧龙布鲁克地块北部(乌兰北部)原定为达肯大坂群中识别出一些~1.5Ga的正片麻岩(Wang et al., 2016)、1.2~1.1Ga的眼球状花岗岩、少量新元古代早期花岗片麻岩(Wang et al., 2016；Yu et al., 2019a)以及广泛分布的中新元古代(？)变沉积岩，并普遍遭受早古生代(510~450Ma)变质事件(低压/高温变质作用)叠加，并伴随同时代(早古生代)的基性-酸性深成岩浆活动(康珍等，2015；李秀财等, 2015a, b；吴才来等，2016；Lu et al., 2018；马建军等, 2018, 2019；Wang et al., 2018a；Li et al., 2019；Wu et al., 2019)。因此，我们把乌兰北部的“达肯大坂群”及相关岩石从欧龙布鲁克地块解体出来，并认为是形成在弧-弧后背景下的深部变质-岩浆杂岩(图 1)，为大陆深俯冲之前大洋岩石圈向欧龙布鲁克地块之下俯冲的产物(Li et al., 2018, 2019；Lu et al., 2018；Wang et al., 2018a)。
滩间山群火山沉积岩系在柴北缘构造带广泛分布，呈北西-南东向展布，西起赛什腾山的吉绿素，向东经绿梁山(双口山)、锡铁山至都兰地区，绵延约600km，与超高压变质带在空间上伴生，但分布范围更大，且与后者多呈断层接触(高晓峰等，2011)。其岩性以浅变质的中-基性火山岩及少量细碎屑岩和碳酸盐岩为主，夹有少量基性-超基性岩侵入体，局部地区可见酸性火山岩，变质程度为绿片岩相-绿帘角闪岩相。滩间山群形成的构造环境长期存在争议。早期有学者认为锡铁山及托莫尔日特地区滩间山群可能为一套大陆裂谷型建造(邬介人等，1987；孙延贵等，2000)；赖绍聪等(1996)认为滩间山群及相伴生的蛇纹岩和辉长岩具有蛇绿岩性质；近10余年来，多数学者认为滩间山群主体形成于与大洋俯冲有关的弧构造背景，地球化学研究显示在吉绿素、绿梁山及双口山地区出露的滩间山群火山岩具有弧火山岩性质(王惠初等，2003；史仁灯等，2004；Shi et al., 2006；高晓峰等，2011)，在吉绿素滩间山群火山岩中还厘定出了埃达克质英安岩(史仁灯等，2003)；王惠初等(2005)及朱小辉等(2014)认为在绿梁山北部地区的滩间山群变基性火山岩形成于弧后盆地，并与相关的辉长岩和蛇纹岩构成弧后盆地型蛇绿岩；此外滩间山群还可能包含一些具有混杂岩特征的弧前增生杂岩(朱小辉等，2014)。
滩间山群的形成时代同样存在争议。最初因在滩间山群灰岩中采到了奥陶纪化石，将其时代定为奥陶-志留纪(青海省地质矿产局，1991)；近10余年来相继获得滩间山群火山岩及相关侵入体的同位素年龄，如史仁灯等(2004)测得了柴北缘西段吉绿素安山岩514±9Ma的锆石U-Pb年龄；赵风清等(2003)在锡铁山中酸性火山岩中得到了486±13Ma的TIMS锆石U-Pb下交点年龄，而Sun et al. (2019)获得锡铁山中基性火山岩的锆石U-Pb年龄为460~440Ma；王惠初等(2005)在绿梁山地区得到了变质玄武岩的464Ma的TIMS锆石U-Pb年龄；袁桂邦等(2002)和朱小辉等(2010)分别获得柴北缘西段绿梁山与滩间山群基性火山岩相关的辉长岩496±6Ma和521±7Ma的年龄；朱小辉等(2012)获得柴北缘东段旺尕秀与滩间山群相关辉长岩的年龄为468±2Ma。这些数据显示滩间山群的形成年龄可能为早寒武世到晚奥陶世(520~440Ma)，时间跨度约80Myr。
1.2 样品及其位置柴北缘构造带东段以都兰UHP变质单元岩石为特征，其北部为欧龙布鲁克地块的一部分，以花岗岩、辉长岩、滩间山群火山岩及泥盆纪牦牛山群与UHP变质单元分隔。进一步向北为从欧龙布鲁克地块解体出的乌兰北早古生代弧变质-岩浆杂岩带(图 1)。其中的UHP变质单元主要分布在的野马滩-沙柳河一带，被~400Ma的未变形的野马滩花岗岩侵入(吴才来等，2004)。都兰UHP变质单元主要由中元古代晚期-新元古代早期正、副片麻岩及夹在其中的榴辉岩和少量超基性岩所组成。滩间山群在区内分布较广泛，与超高压单元岩石之间为断层接触，并与泥盆纪以来的地层呈不整合或断层接触。
本文样品采自都兰查查香卡农场南部，夏日哈山北坡的滩间山群火山岩中(图 2a)。剖面露头显示此岩石组合南侧逆冲在泥盆系浅紫红色砂岩、含砾砂岩之上，北侧与含高压麻粒岩的片麻岩(属于都兰UHP变质单元)呈断层接触(图 2b)。此岩石系列以酸性的英安岩和基性玄武岩为主(图 3a，b)，夹有少量安山质岩石，各类岩石层状分布，之间无明显构造界限。英安岩的斑晶以自形斜长石为主(图 3c)，个别样品可见少量角闪石斑晶，且多数石英颗粒外围呈现港湾状或锯齿状，基质主要为石英，少量暗色矿物蚀变严重，大部分已绿泥石和帘石化。玄武岩斑晶以斜长石为主，局部含有辉石，基质由于强烈蚀变不易识别矿物(图 3d)。我们在对此剖面进行详细观察和系统采样的基础上，选择其中12件典型样品(玄武质基性火山岩2件，英安质酸性火山岩9件，安山质中性火山岩1件)进行了全岩地球化学测试，并对2件代表性样品进行了锆石U-Pb同位素定年及Hf同位素测试工作，具体采样位置见图 2b。
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图 2 都兰查查香卡地区地质简图 Fig. 2 Schematic geological map of Chachaxiangka, Dulan County |
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图 3 柴北缘东段火山岩野外(a、b)及显微照片(c、d) (a)浅灰绿色英安岩；(b)玄武岩呈灰绿色，具有类似枕状构造；(c)英安岩具斑状结构，斑晶以自形斜长石为主，基质为细粒的石英、斜长石及少量暗色矿物；(d)具有斜长石(Pl)斑晶的玄武岩 Fig. 3 Felid macroscopic (a, b) and thin section (c, d) views of volcanic rocks from eastern North Qaidam Mountains (a) lightly grayish green Dacite; (b) greyish green basalt shows a pillow-like structure; (c) dacite with a porphyritic structure. the porphyroblasts are dominated by euhedral plagioclase, and the matrix consist of fine-grained quartz, plagioclase and small amount of dark minerals; (d) basalt with Plagioclase porphyroblasts (Pl) |
测年样品锆石的分选由河北省区域地质矿产调查研究所完成，用传统的重液和磁选法将锆石从碎石中分离出来。在双目显微镜下进行选择后，灌注在环氧树脂靶中，然后抛光至暴露出颗粒的中心。
全岩化学分析由中国地质科学院国家地质测试分析中心测试，其中全岩主量元素用X荧光光谱仪(XRF)分析，所用仪器为日本理学3080E，误差＜0.5%，FeO采用容量滴定法，K2O采用原子吸收法；微量元素和稀土元素采用等离子质谱仪分析，误差＜5%。
样品AQ16-24-3.1锆石U-Pb定年在北京离子探针中心SHRIMP II上完成。详细分析方法见Williams(1998)。一次流O2-强度为3~5nA，束斑直径为25~30μm。标样M257(U=840×10-6，Nasdala et al., 2008)和TEM(年龄为417Ma，Black et al., 2003)分别用于锆石U含量和年龄校正。每分析3~4个未知样品数据分析1次标准锆石TEM，每个分析点采用5组扫描。数据处理采用SQUID和ISOPLOT程序(Ludwig, 2003)。样品AQ16-24-2.2的U-Pb定年在北京燕都中实测试技术有限公司实验室利用LA-ICPMS分析完成。激光剥蚀系统为New Wave UP213，ICP-MS为德国耶拿M90。激光剥蚀过程中采用氦气作载气、氩气为补偿气以调节灵敏度，二者在进入ICP之前通过一个Y型接头混合。每个时间分辨分析数据包括大约20~30s的空白信号和50s的样品信号。对分析数据的离线处理(包括对样品和空白信号的选择、仪器灵敏度漂移校正、元素含量及U-Th-Pb同位素比值和年龄计算)采用软件ICPMSDataCal(侯可军等，2009；Liu et al., 2010)完成。详细的仪器操作条件和数据处理方法同Liu et al.(2008, 2010)。
锆石Lu-Hf同位素测试在北京科荟测试技术有限公司的LA-MC-ICPMS上进行，激光进样系统为NWR213nm固体激光器，分析系统为多接收等离子体质谱仪(NEPTUNE plus)，以高纯He为载气。激光剥蚀的斑束直径为55μm，能量密度为7~8J/cm2，频率为10Hz。根据锆石CL图像，选择的测试点靠近U-Pb测定点，且为同一CL结构位置。采用179Hf/177Hf=0.7325对同位素比值进行指数归一化质量歧视校正，采用173Yb/172Yb=1.35274对Yb同位素比值进行指数归一化质量歧视校正。εHf(t)计算采用衰变常数λ=1.865×10-11y-1(Scherer et al., 2001)，(176Lu/177Hf)CHUR=0.0332，(176Hf/177Hf)CHUR, 0=0.282772(Blichert-Toft and Albarède，1997)。单阶段模式年龄(tDM1)计算时采用(176Lu/177Hf)DM=0.0384，((176Hf/177Hf)DM=0.28325)，二阶段模式年龄(tDM2)计算时采用的平均地壳176Lu/177Hf值为0.0093(Amelin et al., 1999)。
3 分析结果 3.1 全岩地球化学12个岩石样品全岩地球化学分析测试数据见表 1。
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表 1 柴北缘东段火山岩全岩地球化学数据表(主量元素:wt%；稀土和微量元素:×10-6) Table 1 Whole-rock major (wt%) and trace (×10-6) elements of volcanic rocks from the eastern North Qaidam Mountains |
9个英安岩SiO2含量在64.79%~67.73%之间，Al2O3含量较高(16.02%~18.20%)，MgO含量介于1.07%~1.68%之间，平均为1.33%，Mg#值相对偏高，在49~56之间，平均为53，岩石显示明显的富Na2O贫K2O特征，K2O/Na2O比值较低(0.14~0.43之间)，K2O含量在0.83%~1.95%之间，基本都处于中钾亚碱性系列(图 4)。岩石均富集轻稀土(LREE)，亏损重稀土(HREE)，(La/Yb)N比值介于7.56~22.61之间，平均为14.5，具有弱-中等的正Eu异常(Eu/Eu*在1.13~1.45之间，平均值1.27)，配分曲线呈现中等的右倾特征，且重稀土分布较平坦，中稀土有明显的下凹特征(图 5)。微量元素显示高Sr(751×10-6~1043×10-6)，低Y(3.26×10-6~5.3×10-6)和Yb(0.33×10-6~0.58×10-6)，Sr/Y比值较高(172~282)的特征，岩石还具有较高的Ba含量(675×10-6~1303×10-6，平均值1079×10-6)，在微量元素蛛网图中显示较明显的Sr与Ba的正异常。相对富集Rb、Ba、K、Sr等大离子亲石元素，亏损Nb、Zr、Ti等高场强元素，在Sr/Y-Y及(La/Yb)N-YbN图解中均落在埃达克岩区域(图 6)。
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图 4 岩石类型判别图解 (a) SiO2-K2O图解(Peccerillo and Taylor, 1976)；(b)SiO2-(K2O+Na2O)(TAS)图解(Le Bas et al., 1986) Fig. 4 Rock type discrimination diagrams (a) SiO2 vs. K2O diagram (Peccerillo and Taylor, 1976); (b) total alkali vs. silica diagram (Le Bas et al., 1986) |
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图 5 柴北缘东段火山岩球粒陨石标准化稀土元素配分曲线及原始地幔标准化微量元素蛛网图(标准化值据Sun and McDonough, 1989) Fig. 5 Chondrite-normalized REE patterns and primitive mantle-normalized trace element spider diagrams volcanic rocks from the eastern North Qaidam Mountains (normalization values after Sun and McDonough, 1989) |
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图 6 埃达克岩Y-Sr/Y及YbN-(La/Yb)N判别图解(底图据Defant and Drummond et al., 1990；Martin et al., 2005) Fig. 6 Y vs. Sr/Y and YbN vs. (La/Yb)N discrimination diagrams for adakites (base map after Defant and Drummond et al., 1990; Martin et al., 2005) |
1个安山岩样品SiO2含量57.68%，Al2O3含量16.18%，MgO含量4.04%，Mg#值为52，K2O含量0.91%, Na2O含量3.44%，K2O/Na2O比值0.26，属于中钾亚碱性系列(图 4)，类似于高镁安山岩地球化学特征，只是其MgO含量略低(高镁安山岩一般>5%)。高Sr(614×10-6)，低Y和Yb(Y=14.1×10-6，Yb=1.46×10-6)，Sr/Y比值44，在Sr/Y-Y及(La/Yb)N-YbN图解中均落在埃达克岩与经典岛弧岩浆岩过渡的区域(图 6)。稀土元素含量较高，稀土配分图中显示明显的轻稀土(LREE)富集与重稀土(HREE)亏损，(La/Yb)N比值11.94，无Eu异常。相对富集大离子亲石元素(LILE)，亏损高场强元素(HFSE)(图 5)，相容元素Cr、Ni、Co等含量高于典型的埃达克岩。
2个玄武岩的样品中SiO2含量在50%左右，Al2O3含量14.61%~14.95%，MgO含量5.89%~6.07%，Mg#在47.5~49.0之间，K2O含量大约0.68%，Na2O含量为3.45%~3.70%，K2O/Na2O比值在0.2左右，具有中钾亚碱性与碱性过渡的地球化学特征(图 4)。与典型岛弧玄武岩相比，具有更高的TiO2含量(~2%)及P2O5含量(~0.25%)，且具明显高的Nb含量(16.9×10-6~17.9×10-6)。同时具有高的Nb/Ta比值(介于21.1~22.4之间)及Nb/U比值(介于27.5~29.6之间)，且(Nb/La)N>0.5(平均为0.92左右)，符合Sajona et al.(1993, 1996)所提出的富Nb玄武岩特征，并且在MgO-Nb/La及Nb-Nb/U图解中位于富Nb玄武岩区域(图 7)。稀土配分图中显示弱的轻稀土(LREE)富集与重稀土(HREE)亏损，(La/Yb)N比值3.6左右。相对富集大离子亲石元素(LILE)及高场强元素(HFSE)，在微量元素蛛网图中总体分布较平坦(图 5)。
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图 7 玄武岩MgO-Nb/La (a)和Nb-Nb/U (b)图解 岛弧玄武岩及富Nb玄武岩区域据Kepezhinskas et al.(1996) Fig. 7 MgO vs. Nb/La (a) and Nb vs. Nb/U (b) diagrams for basalts The fields of island arc basalt and Nb-enriched basalt are from Kepezhinskas et al. (1996) |
我们分别选取1个英安质和1个安山质埃达克岩进行了锆石U-Pb定年，具体数据见表 2和表 3。
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表 2 英安质埃达克岩(样品AQ16-24-2.2)锆石LA-ICPMS U-Pb测年结果 Table 2 LA-ICPMS U-Pb analysis results of zircons from dacitic adakite (Sample AQ16-24-2.2) |
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表 3 安山质埃达克岩(样品AQ16-24-3.1)锆石SHRIMP U-Pb测年结果 Table 3 SHRIMP U-Pb analysis results of zircons from andesitic adakite (Sample AQ16-24-3.1) |
英安质埃达克岩AQ16-24-2.2中锆石粒径在100~200μm之间，长宽比1.2~4，在CL图像中为较规则的短-中等长度的棱柱状，具明显的密集振荡环带，Th/U比值为0.16~0.71，显示典型的岩浆锆石特征(图 8)，个别锆石具有继承性锆石核。我们对其锆石进行了LA-ICPMS U-Pb同位素测试，得到了26个有效数据点，其206Pb/238U年龄介于617~445Ma之间，去除4个继承/捕获锆石年龄，剩余22个数据点均位于谐和线上及附近，得到了457±4Ma的加权平均年龄(图 9)，解释为英安质埃达克岩的结晶年龄。
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图 8 柴北缘东段埃达克岩锆石CL图像及代表性年龄 Fig. 8 Zircon CL images and their representative ages of adakites from the eastern North Qaidam Mountains |
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图 9 柴北缘东段埃达克岩锆石U-Pb谐和图 Fig. 9 Zircon U-Pb concordia plots of adakites from the eastern North Qaidam Mountains |
安山质埃达克岩AQ16-24-3.1中锆石粒径在120~250μm，大部分在200μm左右。多为半自形粒状，晶面较平直，很多颗粒形态呈现碎片状，具有补丁或不明显振荡环带特征(图 8)，其总体形态结构与典型中基性岩中的锆石特征相似，结合其Th/U比值(介于0.47~0.80之间)，推断其为岩浆锆石。选取其中20颗锆石进行了SHRIMP U-Pb同位素测试，得到的206Pb/238U年龄数据介于478~436Ma之间。5个锆石数据误差或相对误差较大，且其年龄稍老或年轻，排除这5个数据，剩余15个谐和的数据得到453±4Ma的加权平均年龄(图 9)，解释为锆石的岩浆结晶年龄。
3.3 锆石Lu-Hf同位素我们对2个测年样品中有年龄结果的锆石进行了相应的Lu-Hf同位素测试，详细分析结果见表 4。由于锆石的Lu/Hf值(fLu/Hf=-0.97)显著小于大陆地壳，因此二阶段模式年龄更能真实的反映其源区物质从亏损地幔抽取的时间(第五春荣等，2007)。
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表 4 样品AQ16-24-2.2及AQ16-24-3.1锆石Lu-Hf同位素测试结果 Table 4 Lu-Hf isotope analysis results of zircons from samples AQ16-24-2.2 and AQ16-24-3.1 |
英安质埃达克岩AQ16-24-2.2共得到18个有效数据，锆石的176Hf/177Hf比值处于0.282619与0.282870之间，εHf(t)均为正值，但变化较大，介于4.64~13.23范围内，平均值为8.18，二阶段模式年龄(tDM2)介于1017~566Ma之间，平均值为827Ma(图 10)。安山质埃达克岩AQ16-24-3.1共得到20个有效数据点，样品中锆石的176Hf/177Hf比值介于0.282595与0.282716之间，εHf(t)亦均为正值，数值变化相对AQ16-24-2.2略小，介于3.40~8.03范围内，平均值5.92，相应的二阶段模式年龄(tDM2)在1059~836Ma之间，平均值939Ma(图 10)。
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图 10 柴北缘东段埃达克岩的锆石年龄-εHf(t)图 Fig. 10 εHf(t) vs. Age diagram for zircons of adakites from the eastern North Qaidam Mountains |
柴北缘东段中酸性岩具有高SiO2(64.49%~67.73%，除了安山质埃达克岩为57.78%)，高Al2O3(16.02%~18.20%)，MgO含量主要在1.07%~1.68%之间(安山质埃达克岩的MgO为4.04%)，富Na、贫K特征，K2O/Na2O比值较低(介于0.14~0.43之间)，高Sr(614×10-6~1043×10-6)，低Y (3.26×10-6~14.1×10-6)和低Yb (0.33×10-6~1.46×10-6)，高的Sr/Y比值(44~282)，具有典型的埃达克岩地球化学特征。
埃达克岩最初被定义为年轻的(＜25Ma)而热的洋壳在榴辉岩相条件下部分熔融形成的火山岩或深成岩(Defant and Drummond, 1990)。后来有学者提出埃达克岩根据其地球化学特征可分为O型埃达克岩和C型埃达克岩，并认为O型埃达克岩为经典埃达克岩，与板片部分熔融作用有关；而C型埃达克岩富K(大部分仍为Na质)，与板片熔融无关，可能由加厚陆壳(>50km)底部或拆沉(delamination)的下地壳基性岩部分熔融形成(Atherton and Petford, 1993；张旗等, 2001a, b；Chung et al., 2003；Xiong et al., 2003；Hou et al., 2004；Wang et al., 2005；张旗，2011；Long et al., 2015；张旗和焦守涛，2020)。还有一些学者认为埃达克岩可能是由岛弧环境下复杂成因的幔源基性岩浆高压下分离结晶的产物(Castillo, 2002；Macpherson et al., 2006；Petrone and Ferrari, 2008)。因此，归纳起来，埃达克岩的主要形成方式可总结为三种：(1)俯冲大洋板片的部分熔融；(2)下地壳基性岩的部分熔融；(3)岛弧环境下初始弧岩浆高压下的分离结晶。
在Harker图解中，柴北缘东段埃达克岩多数落在俯冲板片熔融区域与加厚下地壳部分熔融共同区域内及附近，部分落在俯冲洋壳部分熔融区域(图 11)。但其相对富Na、贫K，K2O/Na2O比值较低(K2O/Na2O介于0.14~0.43之间，K2O含量在0.83%~1.95%之间)，MgO含量较低，且具有低的Th含量(1.90×10-6~5.02×10-6)和Th/Ce比值，明显区别于下地壳基性岩部分熔融形成的C型埃达克岩，Cr-Ni相关图解中也显示具有板片熔融特征(图 12)。其εHf(t)均为正值，且分布范围较大，部分数据甚至接近地幔演化线，显示以新生地壳物质为主(图 10)，亦不符合下地壳熔体特征，并且加厚下地壳熔融的熔体无法经过地幔楔，因此不能与之进行相互作用，无法形成埃达克岩-富Nb玄武岩的岩石组合。柴北缘东段埃达克岩的以上特征均表现出鲜明的板片熔融特征，而与下地壳的熔体特征差别较大(Zhou et al., 2006；Wang et al., 2007, 2008a)，因此排除了加厚下地壳部分熔融的可能性。同时柴北缘东段埃达克岩在一定范围内非常一致的稀土元素及微量元素配分模式及强烈的轻重稀土分馏(图 5)均表明其AFC过程并不明显(Liu et al., 2014)，与岛弧钙碱性系列明显不同。Sm-La/Sm及La-(La/Yb)N图解同样显示柴北缘东段埃达克岩具有显著的部分熔融趋势，并无显著的分离结晶过程(图 13)。基于以上认识，我们认为柴北缘东段埃达克岩为典型的O型埃达克岩，为岛弧环境下俯冲大洋板片部分熔融的产物。
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图 11 柴北缘东段埃达克岩Harker图解(底图据王强等，2006及其文献) Fig. 11 Harker diagrams for adakites from the eastern North Qaidam Mountains (base map after Wang et al., 2006 and references therein) |
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图 12 柴北缘东段火山岩Cr-Ni图解(据Tsuchiya et al., 2005) Fig. 12 Cr vs. Ni diagrams for volcanic rocks from the eastern North Qaidam Mountains (after Tsuchiya et al., 2005) |
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图 13 柴北缘东段埃达克岩Sm-La/Sm (a)及La-(La/Yb)N (b)图解(据Long et al., 2015) Fig. 13 Sm vs. La/Sm (a) and La vs. (La/Yb)N (b) diagrams for adakites from the eastern North Qaidam Mountains (after Long et al., 2015) |
实验岩石学证据表明，蚀变的玄武岩部分熔融产生的溶体Mg#值一般 < 50，而地幔橄榄岩的交代作用能使其MgO及Mg#迅速增加(Rapp et al., 1999)，柴北缘东段安山质埃达克岩具有较高的Mg#值，较低的SiO2、较高的MgO且相对富集Cr、Co、Ni等相容元素，符合受地幔橄榄岩交代的特征，具有高Mg安山岩的一些性质。但由于仅1个样品，需要进一步详细工作和更多样品研究来确定安山质埃达克岩的成因，本文不做过多讨论。
4.1.2 富Nb玄武岩(NEBs)不同于经典岛弧玄武岩，柴北缘东段富Nb玄武岩明显高的TiO2、Nb和Zr含量及高的(Nb/La)N，且无明显Nb、Ti、P等的负异常，表明其不太可能形成于流体交代的地幔楔部分熔融。有观点认为富Nb玄武岩可能由富集地幔或洋岛玄武岩(OIB)与亏损地幔混合的产物(Castillo et al., 2002)，但多数学者认为其来源于受埃达克质熔体交代的地幔楔部分熔融(Defant and Drummond, 1993；Sajona et al., 1993, 1996；Kepezhinskas et al., 1996；Aguillón-Robles et al., 2001；Defant and Kepezhinskas, 2001)。柴北缘东段富Nb玄武岩Nb/U比值远低于洋岛玄武岩(OIB)(47±10)，且其Ce/Pb比值(7.6~9.6)也较低，故而排除其来源于OIB、E-MORB及N-MORB型地幔的可能性。其不相容元素显示具有明显熔体交代相关的富集特征(图 14)，相容元素Cr-Ni相关图解显示其位于板片熔体-地幔混合的演化线上，具有板片熔体交代的特征(图 12)。因此推断柴北缘东段富Nb玄武岩为受埃达克质岩浆交代的地幔楔部分熔融形成。
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图 14 柴北缘东段玄武岩Th/Zr-Nb/Zr (a)和Nb/Y-Rb/Y (b)判别图解(据Kepezhinskas et al., 1997) Fig. 14 Th/Zr vs. Nb/Zr (a) and Nb/Y vs. Rb/Y (b) diagrams for basalts from the eastern North Qaidam Mountains (after Kepezhinskas et al., 1997) |
柴北缘东段富Nb玄武岩具有典型富Nb玄武岩的一般特征，但其相容元素含量(如Cr=47.3×10-6~50.8×10-6，Ni=28.4×10-6~36.5×10-6)明显低于显生宙，尤其是新生代以来的典型富Nb玄武岩(Cr=135×10-6~250×10-6、Ni=70×10-6~190×10-6)，同时其重稀土元素含量(如Yb=3.39×10-6~3.77×10-6)明显高于显生宙，尤其是新生代富Nb玄武岩(Yb=1.32×10-6~1.88×10-6)，而更类似太古宙富Nb玄武岩(Yb=2.01×10-6~5.01×10-6，Cr=1×10-6~217×10-6，Ni=1×10-6~146×10-6)(Wang et al., 2003, 2007及其文献)。太古宙时期相较于显生宙时期具有异常高的地热梯度，板片熔体交代的地幔楔橄榄岩在较浅部的斜长石稳定域便可发生熔融(Martin，1999)，并因此导致其具有较高的重稀土元素含量，柴北缘东段富Nb玄武岩可能形成于此种高地温梯度的环境下，从而导致其具有类似太古宙富Nb玄武岩的地球化学特征。
4.1.3 埃达克岩-富Nb玄武岩成因动力学模式正常的洋壳俯冲状态下，俯冲的大洋板片会在100~200km左右的深度发生脱水作用，产生的流体上升并导致上覆地幔楔部分熔融形成岛弧高钾钙碱性系列岩浆岩(Gill，1981；Defant and Drummond, 1990)，而埃达克岩的形成需要一个高热的状态，从而使俯冲的大洋板片在达到弧下深度之前就已发生部分熔融，生成埃达克质岩浆(Defant and Drummond, 1990，1993；Peacock et al., 1994；Drummond et al., 1996；Martin, 1999)。由此不同学者相继提出多种可能的动力学模式，主要观点主要有：1)平坦俯冲的板片被加热而发生熔融(Gutscher et al., 2000)；2)俯冲的年轻而热洋壳部分熔融(Defant and Drummond, 1990， Kepezhinskas et al., 1996；Sajona et al., 1996；Defant and Kepezhinskas, 2001；Wang et al., 2007, 2008a)；3)板片撕裂或洋脊俯冲导致的板片窗(slab window)加热板片发生熔融(Thorkelson，1996；Aguillón-Robles et al., 2001；Yogodzinski et al., 2001；Benoit et al., 2002；Thorkelson and Breitsprecher, 2005；Pallares et al., 2007；Geng et al., 2009；Ling et al., 2009；Wallace et al., 2009；Sun et al., 2010；Li et al., 2012；Shen et al., 2014；Wang et al., 2018b)。由于在平板俯冲(flat subduction)过程中会产生一个较宽(可能超过200km)的埃达克质的弧(adakitic arc)，并且其位置会较正常的火山弧距海沟更远(Gutscher et al., 2000)，而反观柴北缘东段埃达克岩其与超高压变质带在空间上伴生，更可能是形成于弧前的位置。因此柴北缘东段埃达克岩-富Nb玄武岩可能的形成模式有两种：1)俯冲年轻洋壳的部分熔融；2)板片撕裂或洋脊俯冲形成的板片窗构造。
目前柴北缘地区报道的早古生代岛弧相关的岩浆活动时代基本介于520~450Ma期间(史仁灯等, 2003, 2004；吴才来等, 2004, 2008；Shi et al., 2006；朱小辉等, 2010, 2012；Wu et al., 2019)，从早古生代岛弧相关的岩浆活动从520Ma左右开始，至柴北缘东段埃达克岩形成时(~455Ma)已至少经历~65Myr的时间。随着俯冲的进行，有可能会发生扩张洋脊的俯冲，大洋板片会在扩张脊处发生分离，形成板片窗，俯冲的岩石圈地幔或软流圈会沿板片窗上涌，形成一个高热流环境，在板片窗边缘的洋壳发生部分熔融形成埃达克岩，埃达克岩浆上升交代地幔楔并部分熔融形成富Nb玄武岩。另外, 即使在未发生洋脊俯冲的情况下，在洋壳俯冲晚期，由于洋盆的不断萎缩，大洋地壳从其在洋中脊形成到其运动至海沟发生俯冲左右所经历的时间和距离均较短，同样可以具有较高的俯冲板片温度，从而具备形成埃达克岩的温压条件(边千韬等，2007)。
4.2 构造意义自二十世纪九十年代在该区发现榴辉岩以来(杨建军等，1994；Yang et al., 1998)，柴北缘的HP-UHP变质岩就引起了地质学家的广泛关注。已有的研究表明柴北缘UHP变质带主要形成于大陆深俯冲作用，对于其构造演化模式，不同学者也进行了详细的探讨(Yin et al., 2000, 2007；Yang et al., 2002；Song et al., 2006, 2014；Mattinson et al., 2007；张贵宾等，2012；张建新等，2015；Lu et al., 2018)。此外，一些大陆深俯冲之前的大洋俯冲作用的证据也逐渐被揭示，除了弧岩浆活动(吴才来等, 2004, 2008；Wu et al., 2019)和少量洋壳俯冲形成的榴辉岩证据外(Zhang et al., 2008a)，在柴北缘北部的乌兰地区，近年还报道有与大洋俯冲的弧构造背景下的低压/高温(LP/HT)变质带(李秀财等，2015b；Lu et al., 2018；Wang et al., 2018a；Li et al., 2019)，也表明柴达木地块及其相连的南祁连洋壳向北部的欧龙布鲁克地块之下俯冲。
对于南祁连洋的俯冲和闭合的具体时限还存在一定的争议(Song et al., 2006, 2014, 2019；Xiong et al., 2011；张贵宾等，2012；Zhang et al., 2017；周桂生等，2017；Lu et al., 2018；Wang et al., 2018a；Li et al., 2019；Wu et al., 2019；Yu et al., 2019b)。早期的很多年龄为单颗粒锆石TIMS或Sm-Nd等方法获得，年龄分布范围较大，由于锆石多期次生长的存在，其可信度可能有待商榷。近年来已有大量锆石LA-ICPMS或SHRIMP年代数据的报道，数据显示柴北缘UHP变质带及北部的欧龙布鲁克地块内与弧相关的岩浆作用时代主要介于520~450Ma之间(史仁灯等，2004；朱小辉等，2010；2012，2014；Li et al., 2018；Wang et al., 2018a；Wu et al., 2019；Yu et al., 2019b)；乌兰北早古生代弧变质-岩浆杂岩带内与弧相关的LP/HT变质作用的时代主要集中于500~460Ma，峰期集中于~475Ma左右(康珍等，2015；李秀财等，2015b；Lu et al., 2018；Wang et al., 2018a)，可能为弧-弧后环境下的产物。柴北缘UHP变质带内与洋壳俯冲有关的榴辉岩变质时代介于460~445Ma之间(Zhang et al., 2008a；Xiong et al., 2011)，陆壳性质的榴辉岩变质年龄在450~423Ma之间(Song et al., 2005, 2006, 2014；Mattinson et al., 2006a, b，2009；Chen et al., 2009a；Zhang et al., 2009a, c，2010，2017；Xiong et al., 2011, 2012；宋述光等，2011；Yu et al., 2013；Ren et al., 2017；周桂生等，2017)，显示大陆初始俯冲约在450Ma左右。依前文所述，柴北缘东段埃达克质岩石-富Nb玄武岩的组合为大洋俯冲过程中的岛弧(弧前)环境下的产物，其结晶年龄为457~453Ma。因此综合以上数据我们推断：在~455Ma左右，柴北缘地区正处于大洋俯冲的晚期阶段，此时南祁连洋并未完全闭合。
在柴北缘东部都兰地区，已报道有与大陆碰撞有关的埃达克质岩石形成，时代为435~420Ma，且其与同时代的镁铁质高压麻粒岩密切共生，其形成机制被解释为大陆碰撞过程中加厚的镁铁质下地壳岩石在高压麻粒岩相变质作用下部分熔融的产物(Yu et al., 2012, 2014)。在柴北缘西段, 吉绿素的滩间山群火山岩中还厘定出了埃达克质英安岩(史仁灯等，2003)，相关安山岩形成时代为514Ma(史仁灯等，2004)，推测可能与柴北缘地区大洋的初始俯冲有关，但缺乏进一步的研究。因此，在柴北缘早古生代从大洋俯冲到大陆碰撞过程的不同演化阶段，可能产生不同成因和时代的埃达克岩(或埃达克质岩石)。另外，正如前面所述，大洋俯冲环境下埃达克岩的形成要求热(暖)的俯冲条件，即洋壳俯冲在高温榴辉岩和石榴麻粒岩(角闪岩)相条件下的部分熔融。然而，到目前为止，柴北缘地区已报道的与洋壳俯冲相关榴辉岩形成的温压条件处在相对冷的俯冲环境(Zhang et al., 2008a, 2009a)，没有部分熔融证据。因此，在柴北缘是否存在洋壳热(暖)俯冲背景下的榴辉岩仍需要进一步详细的工作来澄清。
柴北缘东段埃达克岩-富Nb玄武岩的存在均表明柴北缘地区早古生代大洋俯冲过程中，存在板片熔体来源的新生陆壳物质。埃达克岩与地壳生长的关系已得到广泛关注，许多学者认为热的俯冲洋壳的部分熔融可能是地球早期地壳生长的重要方式(Martin，1999)。因此，在柴北缘地区，地壳的增生作用除俯冲带上盘流体交代的地幔楔部分熔融外，大洋板片熔体的贡献同样不能忽视，柴北缘东段埃达克岩-富Nb玄武岩的形成对研究俯冲-碰撞造山带的洋陆转换过程及显生宙陆壳增生机制均具有重要的意义。
5 结论(1) 柴北缘UHP变质带柴北缘东段中酸性火山岩为典型的埃达克岩，具有O型埃达克岩特征，形成于俯冲大洋板片熔融过程；基性火山岩具有富Nb玄武岩地球化学特征，显示板片熔体交代特征，可能为受埃达克质熔体交代的地幔橄榄岩部分熔融的产物。
(2) 锆石U-Pb定年结果表明柴北缘东段埃达克岩形成年龄为~455Ma，表明当时柴北缘地区大洋俯冲尚未结束。
(3) 柴北缘东段埃达克岩-富Nb玄武岩组合可能源于大洋俯冲晚期俯冲年轻洋壳的部分熔融或洋脊俯冲作用过程；俯冲大洋板片的部分熔融可能是柴北缘早古生代地壳增生的一种重要方式。
致谢 本文在实验测试中得到了北京离子探针中心、北京燕都中实测试技术有限公司、北京科荟测试技术有限公司及国家地质实验测试中心工作人员的帮助；在文章修改过程中得到了何碧竹研究员的帮助；两位评审专家张泽明研究员和孟繁聪研究员提出了建设性的修改意见；在此一并致以诚挚的谢意。
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