2013, Vol. 29
2. 中国科学院大学，北京 100039
2. University of Chinese Academy of Sciences, Beijing 100039, China
大火成岩省主要由分布广泛(>105km2)和巨量(>105km3)的基性岩浆岩，以及少量相伴生的碱性长英质和硅不饱和岩浆岩组成，其持续时间最长可达50Myr，主体在较短(1~5Myr)的时间内形成 (Bryan and Ernst, 2008)。其形成通常和地幔柱活动相关 (Campbell, 2005; Campbell and Griffiths, 1990; Courtillot et al., 2003; Griffiths and Campbell, 1990; Hill et al., 1992; Richards et al., 1989; Wolfe et al., 2009; Xu et al., 2004)。
早二叠世塔里木大火成岩省岩浆岩覆盖面积超过250000km2 (Tian et al., 2010; Yang et al., 2007)，主要由分布在在盆地内部的溢流玄武岩和分布在盆地边缘的超基性-基性-长英质侵入体、长英质火山岩和基性岩墙组成(陈汉林等, 1997; 姜常义等, 2004; 厉子龙等, 2008; 杨树峰等, 2006; Tian et al., 2010; Yang et al., 2007; Yu et al., 2011b; Zhang et al., 2008, 2010a, b ; 张洪安等, 2009)。在空间分布上不同的这两类岩浆在时间上也存在明显的差异：以柯坪玄武岩为代表的喷出岩形成较早(~290Ma)，以巴楚超基性-基性-长英质侵入岩和岩墙为代表的侵入岩形成较晚(~280Ma) (位荀和徐义刚, 2011; 徐义刚等, 2013; Li et al., 2011)。而且两期岩浆具有明显不同的地球化学特征：玄武岩具有Nb-Ta负异常和富集的Nd同位素组成，而侵入岩和岩墙具有Nb-Ta正异常和相对亏损的Nd同位素组成(Zhang et al., 2010a; Zhou et al., 2009)。尽管很多学者提出地幔柱模式来解释塔里木大火成岩省的形成(厉子龙等, 2008; Zhang et al., 2010a; Zhou et al., 2009)，但现有模型并未很好地解释两期岩浆的时间、空间分布特征以及它们之间地球化学差异。
岩石圈-地幔柱的相互作用，在大火成岩省的形成过程中扮演了非常重要的角色(Gibson et al., 1995, 1999, 2006; Molzahn et al., 1996; Pik et al., 1999)。柯坪玄武岩可能来自于富集的岩石圈地幔(Zhang et al., 2010a)，而巴楚辉绿岩墙源自富集的软流圈地幔(Zhou et al., 2009)；随着时间的演化，软流圈组分在塔里木岩浆岩中越来越明显，因此两期岩浆的形成可能与岩石圈-地幔柱的相互作用密切相关。巴楚岩墙具有较大的εNd变化范围(-2.6~+5.1)，可能是地壳同化混染也可能是岩石圈地幔物质不断加入所致，对这种现象的解释对理解塔里木大火成岩省形成过程中地幔柱和岩石圈的相对贡献以及相互作用具有重要的意义。
因此，本文对巴楚岩墙进行了锆石年代学和主量、微量元素分析，讨论其岩石成因及岩石圈和地幔柱在塔里木大火成岩省形成过程中的相对贡献；结合文献资料，提出地幔柱侧向流动模型解释两期岩浆的时间、空间分布特征，以及它们之间的地球化学差异。
2 区域地质背景和样品特征塔里木盆地位于中国的西北部，覆盖面积超过600000km2，被北部的天山造山带、南部的昆仑山和阿尔金造山带所围绕(图 1b)。塔里木地块主要由前寒武纪的基底和上覆的古生代沉积地层组成(新疆维吾尔自治区地质矿产局, 1993)。前寒武纪基底主要形成于太古代、古元古代、中元古代和新元古代，主要出露在盆地边缘的库鲁克塔格、阿克苏-乌什、铁克里克等地区(新疆维吾尔自治区地质矿产局, 1993; 张师本, 2003)。塔里木盆地的岩浆期次主要有太古代、元古代和早二叠世(新疆维吾尔自治区地质矿产局, 1993; Hu et al., 2000; Long et al., 2010)。其中早二叠世的岩浆活动最为广泛，形成了大规模的溢流玄武岩、超基性-基性侵入岩、基性岩墙群和A-型花岗岩类等(新疆维吾尔自治区地质矿产局, 1993; 杨树峰等, 2006; 厉子龙等, 2008; Zhang et al., 2008, 2010a)，覆盖面积约2.5×105~3.0×105km2 (Tian et al., 2010; Yang et al., 2007)。玄武岩主要分布于盆地内部，分为底部的库普库兹曼组和上覆的开派兹雷克组，主要出露于柯坪和塔西南地区；超基性-基性侵入岩、基性岩墙群和A-型花岗岩类主要出露于盆地边缘的巴楚、皮羌等地区。
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图 1 塔里木盆地(b)和巴楚小海子地区(a)地质简图(据Yang et al., 2007;陈咪咪等, 2010修改) Fig. 1 Simplified geological map of the Tarim basin (b) and Bachu Xiaohaizi area (a) (modified after Yang et al., 2007; Chen et al., 2010) |
研究区麻扎尔塔格地区(也称为小海子地区)，位于塔里木盆地西北缘(图 1a)。该区地层大部分被第四系覆盖，在小海子水库附近有零星出露，主要有志留系、泥盆系、石炭系以及早二叠统(新疆维吾尔自治区地质矿产局, 1993; 张师本, 2003)。该区出露早二叠世超基性-基性-长英质侵入岩组合、辉绿岩墙和石英正长斑岩脉。研究程度较高的小海子正长岩体，侵入到石炭系-早二叠统，呈近等轴圆形。年代学研究表明，正长岩形成于~280Ma (杨树峰等, 1996, 2006; 位荀和徐义刚, 2011)。正长岩体的边部有少数橄榄辉长岩堆晶岩。辉绿岩墙和石英正长斑岩脉不仅侵入到围岩地层中，也侵入到小海子正长岩体中，并且辉绿岩墙和正长岩局部有岩浆混合的现象(陈咪咪等, 2010; 张自力等, 2008)，暗示辉绿岩墙可能和正长岩近同时侵位。
所采辉绿岩墙样品具有辉绿结构。斑晶主要为斜长石(＜5%)，基质主要由单斜辉石、斜长石和磁铁矿组成。样品均发生不同程度的蚀变：斜长石蚀变成绢云母，单斜辉石蚀变成不透明矿物。
3 分析方法用于U-Pb年龄测定的样品XHZ-10用常规的重选和磁选技术分选出锆石。将锆石样品颗粒和锆石标样 Plésovice (Sláma et al., 2008)和Qinghu (Li et al., 2009) 粘贴在环氧树脂靶上，然后抛光使其曝露一半晶面。对锆石进行透射光和反射光显微照相以及阴极发光图象分析，以检查锆石的内部结构、帮助选择适宜的测试点位。阴极发光图像在中国科学院地质与地球物理研究所LEO 1450 VP扫描电镜上完成，分析电压为15kV，电流为1.1nA。
U、Th、Pb的测定在中国科学院地质与地球物理研究所CAMECA IMS-1280二次离子质谱仪上进行，详细分析方法见Li et al. (2009) 。锆石标样与锆石样品以1：3比例交替测定。U-Th-Pb同位素比值用标准锆石Plésovice (Sláma et al., 2008) 校正获得，U含量采用标准锆石91500 (Wiedenbeck et al., 1995) 校正获得，以长期监测标准样品获得的标准偏差(1SD=1.5%, Li et al., 2010)和单点测试内部精度共同传递得到样品单点误差，以标准样品Qinghu (Li et al., 2009) 作为未知样监测数据的精确度。普通Pb校正采用实测204Pb值。由于测得的普通Pb含量非常低，假定普通Pb主要来源于制样过程中带入的表面Pb污染，以现代地壳的平均Pb同位素组成(Stacey and Kramers, 1975) 作为普通Pb组成进行校正。同位素比值及年龄误差均为1σ。数据结果处理采用ISOPLOT软件(Ludwig, 2003)。
主量和微量元素分析均在中国科学院广州地球化学研究所同位素地球化学国家重点实验室完成。主量元素在Rigaku ZSX100e仪器上完成，详细的分析方法见Li et al. (2006) 。大多数主量元素的分析精度在1%~5%。微量元素测定在PE Elan 6000型电感耦合等离子体质谱仪(ICP-MS)上完成，分析方法见Xu (2002) 。微量元素分析精度通常优于5%。
4 分析结果 4.1 锆石SIMS U-Pb年代学样品(XHZ-10)中的锆石，大部分为碎片；少数晶型完整的锆石呈长柱状，粒径＜100μm。阴极发光(CL)图像(图 2a中插图) 上具有典型的岩浆震荡环带和扇形环带，暗示它们为岩浆成因锆石。这些锆石的U、Th变化范围分别为88×10-6~1024×10-6，47×10-6~446×10-6，Th/U比值为0.13~1.56(表 1)，符合岩浆锆石的特征。17个分析点给出的协和年龄具有较大的变化范围(2480~717Ma；表 1、图 2)。
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图 2 XHZ-10样品锆石U-Pb协和图(a)和年龄分布直方图(b) Fig. 2 U-Pb concordia diagram (a) and histogram (b) for zircons from XHZ-10 |
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表 1 巴楚岩墙XHZ-10 SIMS锆石U-Pb年龄分析结果 Table 1 SIMS zircon U-Pb results of the Bachu dyke XHZ-10 |
巴楚岩墙的SiO2含量范围为47%~51%，全碱(Na2O+K2O)变化范围较大(3.8%~7.0%)(除样品XHZ-10外)(表 2)。在抗蚀变元素判别图解(Zr/TiO2×0.0001-Nb/Y)(图 3；Winchester and Floyd, 1977)上，这些样品位于碱性玄武岩区域。
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表 2 巴楚岩墙主量元素(wt%)XRF和微量元素(×10-6)ICP-MS分析结果 Table 2 Major (wt%) and trace elements (×10-6) analysis results of the Bachu dykes |
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图 3 巴楚岩墙的Nb/Y-Zr/TiO2×10-4图解(文献数据据Yang et al., 2007; Zhang et al., 2010a; Zhou et al., 2009) Fig. 3 Plot of Nb/Y vs. Zr/TiO2×10-4 for the Bachu dykes (Reference data after Yang et al., 2007; Zhang et al., 2010a; Zhou et al., 2009) |
这些样品(除样品XHZ-10外)具有较高的TiO2含量(3.1%~3.8%)和Ti/Y比值(553~756)，和峨眉山大火成岩省的高钛玄武岩相似 (Xu et al., 2001)。MgO含量相对较低(3.5%~4.8%)，Mg# [(100Mg/(Mg+Fe2+)]为38~39，暗示它们经历了较为明显的分离结晶。在Harker图解(图 4)上，TiO2、Fe2O3T和CaO与MgO呈正相关，而Al2O3与MgO呈负相关。这些样品具有较低的Sc(14.3×10-6~21.5×10-6)、Cr(4.72×10-6~54.6×10-6)和Ni(20.5×10-6~56.5×10-6)含量。
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图 4 巴楚岩墙的Harker图解 灰色实线为MELTS模拟分离结晶趋势线.图例和文献数据同图 3 Fig. 4 Harker diagrams of the Bachu dykes The grey lines represent the results of the MELTS calculations of fractional crystallization. Symbols and reference data sources same as Fig. 3 |
在稀土元素球粒陨石标准化图解 (图 5a) 上，巴楚岩墙具有右倾的REE分布模式：富集轻稀土(LREE)、亏损重稀土(HREE)，其(La/Yb)N比值为17.8~18.2。除XHZ-10外，没有明显的Eu异常。在原始地幔标准化图解(图 5b)中，大离子亲石元素(LILE；如Rb、Ba、Th、U)和高场强元素(HFSE；如Zr、Hf、Ti)富集，具有Nb和Ta的正异常，和洋岛玄武岩(OIB)具有非常相似的地球化学特征(Sun and McDonough, 1989)。与其它几个样品不同，XHZ-10具有明显的Eu负异常和Nb-Ta负异常。
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图 5 巴楚岩墙的稀土元素球粒陨石标准化图解(a)和微量元素原始地幔标准化蛛网图(b)(标准化值据McDonough and Sun, 1995) 文献数据同图 3;OIB数据引自Sun and McDonough (1989) Fig. 5 Chondrite-normalized REE patterns (a) and primitive mantle-normalized multi-element variation diagrams (b) for the Bachu dykes (normalizing values after McDonough and Sun, 1995) Reference data sources same as Fig. 3. Also shown is a typical ocean island basalt (OIB) (dashed line) from Sun and McDonough (1989) |
锆石SIMS U-Pb年龄给出比较老的年龄(2480~717Ma)，在年龄分布直方图上显示有两个明显的峰，分别为800Ma和1850Ma(图 2b)。巴楚岩墙侵入到石炭系-早二叠统，这些锆石年龄明显早于地层的形成时代，因此不能代表岩墙的结晶年龄。可能是岩墙在侵位过程中，捕虏周围围岩中的锆石，反映基底的信息。
5.2 蚀变影响巴楚岩墙中一些样品具有相对高的LOI(1.61%~4.20%)，并且Rb和Ba等活动性元素和在蚀变过程中被认为最为稳定的元素Zr没有明显的相关性(图 6a和b)，暗示这些元素受到了蚀变的影响。而Nb(图 6c)、U(图 6d)和REE(未显示)等元素具有很好的正相关关系，暗示这些元素并未明显受到蚀变的影响，那么这些元素可以用来探讨它们的源区特征。
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图 6 巴楚岩墙的Rb-Zr (a)、Ba-Zr (b)、Nb-Zr (c)和U-Zr (d)图解 图例和文献数据同图 3 Fig. 6 Plots of Rb-Zr (a), Ba-Zr (b), Nb-Zr (c) and U-Zr (d) of the Bachu dykes Symbols and reference data sources same as Fig. 3 |
巴楚岩墙具有比较低的MgO含量和Mg#，表明它们经历了比较明显的镁铁质矿物(如橄榄石、辉石)的分离结晶。在Harker图解(图 4)上，巴楚岩墙的TiO2和Fe2O3T与MgO呈正相关，暗示有Ti-Fe氧化物的分离结晶；随着MgO的降低，CaO降低，表明有单斜辉石的分离结晶；Al2O3和MgO呈负相关，表明斜长石的分离结晶并不明显，与REE球粒陨石标准化图解上无明显的Eu负异常和微量元素蛛网图上Sr轻微的负异常一致。XHZ-10具有明显的Eu负异常，可能经历了明显的斜长石分离结晶。
我们选取08KT18-9(具有相对高的MgO=6.1%，Fe2O3T=17.2，TiO2=5.2%；Zhang et al., 2010a)为初始成分，在FMQ(石英-铁橄榄石-磁铁矿)氧逸度和1kbar压力条件下，用MELTS程序(Ghiorso and Sack, 1995)模拟其分离结晶过程。模拟结果(图 4)显示，Ti-Fe氧化物(14.3%)、橄榄石(2.3%)和单斜辉石(13.4%)的分离结晶，可以解释巴楚岩墙的成分变化范围。
5.4 同化混染样品XHZ-10中含有大量的新元古代锆石，并且具有低的Nb/U(10.6)和Nb/Zr(0.08)比值，以及高的Th/Nb(0.54)和La/Nb(2.37)比值，暗示其侵位过程中同化混染了新元古代的基底物质。塔里木新元古代基底具有低的Nd同位素比值(-13.3~-23.7，校正至280Ma)(Cao et al., 2011; Hu et al., 2000; Xu et al., 2005; Zhang et al., 2007)，幔源岩浆在侵位过程中受到这些物质的同化混染，其Nd同位素和微量元素比值会向地壳的方向演化。
大洋玄武岩Nb/U平均比值为52±15 (Hofmann, 2003; Hofmann et al., 1986)，明显高于地壳的比值(6.2, Rudnick and Gao, 2003)，因此低的Nb/U比值可以反映地壳的同化混染。巴楚岩墙Nb/U比值变化范围较大(9.6~50.7)，暗示Nb/U比值低的样品可能受到地壳物质的同化混染。巴楚岩墙εNd(t)具有较大的变化范围(-2.6~+5.1) (Zhang et al., 2010a; Zhou et al., 2009)。εNd(t)值高的样品(+4.5~+5.1)，同时具有低的Th/Nb(0.06~0.12)和La/Nb(0.79~0.96)，和高的Nb/Zr(0.15~0.17)比值，暗示εNd(t)值高的样品并未受到地壳同化混染的影响，可以反映源区组成。总体来说，εNd(t)随着SiO2和La/Nb比值的升高而降低(图 7)，和分离结晶与同化混染所预测的趋势一致 (Depaolo, 1981)，表明εNd(t)值低的样品，是地壳的同化混染所致。简单二单元混合模拟(图 7b和图 8)结果表明，同化混染~30%的新元古代基底物质可以解释巴楚辉绿岩墙的微量元素和同位素变化范围。需要指出的是，模拟计算中选择的初始样品(08KT18-9，Zhang et al., 2010a)具有比较演化的成分，如果选择更为原始的成分，那么同化混染的量会远小于30%。
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图 7 巴楚岩墙的εNd(t)-SiO2(a)和εNd(t)-La/Nb(b)图解 图 7a中虚线范围内的样品具有高的εNd(t)(+4.5~+5.1)，为未受到同化混染的样品(详细讨论见5.4).图 7b中曲线显示简单二单元混合模拟计算结果，端元组成分别为08KT18-9 (Nb=39.8×10-6, La=33.0×10-6, Nd=42.1×10-6, εNd(280) =5；Zhang et al., 2010a)和新元古代基底 (Nb=6.7×10-6, La=42.0×10-6, Nd=26.0×10-6, εNd(280) =-23.6；Cao et al., 2011; Zhang et al., 2007).新元古代基底数据引自Cao et al., 2011; Long et al., 2011; Zhang et al., 2007; Zhu et al., 2011.图例和文献数据同图 3 Fig. 7 Plots of εNd(t)-SiO2 (a) and εNd(t)-La/Nb (b) of the Bachu dykes Results are shown in (b) for assimilation of an uncontaminated sample from the Bahcu dykes (08KT18-9, Zhang et al., 2010a) with Neoproterozoic igneous rocks (Cao et al., 2011; Zhang et al., 2007) as an end-member. Dashed curves with tick marks at 10% indicate the amount of assimilated material relative to 08KT18-9. 08KT18-9 and Neoproterozoic igneous rocks are modeled with 39.8×10-6 Nb, 33.0×10-6 La, 42.1×10-6 Nd, εNd(280) of 5, and 6.7×10-6 Nb, 42.0×10-6 La, 26.0×10-6 Nd, εNd(280) of -23.6 respectively. Neoproterozoic basements from: Cao et al., 2011; Long et al., 2011; Zhang et al., 2007; Zhu et al., 2011. Symbols and reference data sources same as Fig. 3 |
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图 8 巴楚岩墙的La/Nb-Th/Nb(a)和Nb/Zr-Th/Nb(b)图解 图中曲线显示简单二单元混合模拟计算结果.端元组成分别为08KT18-9 (Th=3.64×10-6, Nb=39.8×10-6, La=33.0×10-6, Zr=251×10-6；Zhang et al., 2010a)和新元古代基底(Th=9.21×10-6, Nb = 6.7×10-6, La = 42.0×10-6, Zr = 169×10-6；Cao et al., 2011; Zhang et al., 2007).数据来源：EMI OIB(包括Wavis Ridge, Gough and Tristan)引自Salters and Sachi-Kocher (2010) , Willbold and Stracke (2006) 和Class and le Roex (2008) ; Hawaiian OIB引自http://georoc.mpch-mainz.gwdg.de/georoc/；MORB引自Jenner and O’Neill (2012) ；峨嵋山高钛玄武岩引自Qi and Zhou (2008) , Xiao et al. (2004) , Xu et al. (2001) 和Zhang et al. (2006) .新元古代基底数据引自：Cao et al., 2011; Long et al., 2011; Zhang et al., 2007; Zhu et al., 2011.图例和文献数据同图 3 Fig. 8 Plots of La/Nb-Th/Nb (a) and Nb/Zr-Th/Nb of the Bachu dykes Results are shown for assimilation of an uncontaminated sample from the Bahcu dykes (08KT18-9, Zhang et al., 2010a) with Neoproterozoic igneous rocks (Cao et al., 2011; Zhang et al., 2007) as an end-member. Dashed curves with tick marks at 10% indicate the amount of assimilated material relative to 08KT18-9. 08KT18-9 and Neoproterozoic igneous rocks are modeled with 3.64×10-6 Th, 39.8×10-6 Nb, 33.0×10-6 La, 251×10-6 Zr and 9.21×10-6 Th, 6.7×10-6 Nb, 42.0×10-6 La, 169×10-6 Zr respectively. Data sources: EMI OIB (including Wavis Ridge, Gough and Tristan) from Salters and Sachi-Kocher (2010) , Willbold and Stracke (2006) and Class and le Roex (2008) ; Hawaiian OIB from http://georoc.mpch-mainz.gwdg.de/georoc/; MORB from Jenner and O’Neill (2012) ; Emeishan least contaminated high-Ti basalts from Qi et al. (2008) , Xiao et al. (2004) , Xu et al. (2001) and Zhang et al. (2006) . Neoproterozoic basements from: Cao et al., 2011; Long et al., 2011; Zhang et al., 2007 and Zhu et al., 2011. Symbols and reference data sources same as Fig. 3 |
多数巴楚辉绿岩墙与OIB (Sun and McDonough, 1989) 具有非常相似的配分模式(图 5)。而且受同化混染影响较小样品的微量元素比值(如Th/Nb，La/Nb和Nb/Zr)，落在OIB和峨眉山高钛玄武岩范围内，但是与MORB完全不同(图 8)。这些样品的微量元素比值(如Nb/La=1.2~1.4)和Nd同位素组成(εNd=~+5)，与形成峨眉山高钛玄武岩推测的地幔柱成分(Nb/La=1.0~1.1，εNd=+4.6~+4.8；Xu et al., 2001) 相似。这些特征暗示巴楚辉绿岩墙可能来自对流地幔源区。
在塔里木盆地西缘的巴楚和皮羌地区，辉绿岩墙在时间和空间上通常与超基性-基性侵入体、正长岩和A-型花岗岩伴生。根据同位素组成的相似性，这些A-型花岗岩类被认为和辉绿岩墙以及超基性-基性侵入体具有相似的源区 (位荀和徐义刚, 2011; Zhang et al., 2008, 2010a; Zhang and Zou, 2013)。这些A-型花岗岩类具有非常高的锆石饱和温度(890~1010℃, Zhang et al., 2010a)，是地幔柱相关的侵入体具有的典型特征 (钟玉婷和徐义刚, 2009; Shellnutt and Jahn, 2010; Shellnutt and Zhou, 2007; Zhong et al., 2007, 2011)。
5.6 地幔柱-岩石圈相互作用年龄统计(图 9)表明，塔里木大火成岩省存在明显的两期岩浆活动：玄武岩形成于~290Ma，分布于盆地内部，覆盖面积超过250000km2；岩墙、超基性-基性侵入岩、长英质侵入岩和火山岩形成较晚(~280Ma)，体积小，零散分布于靠近造山带的盆地边缘。并且两期岩浆具有明显不同的地球化学特征和源区组成：~290Ma玄武岩具有Nb-Ta负异常和富集的Nd同位素组成(εNd=-1.8~-3.9)(姜常义等, 2004; Li et al., 2012; Yu et al., 2011b; Zhang et al., 2010a)，可能来自于富集的岩石圈地幔源区；辉绿岩墙具有Nb-Ta的正异常和亏损的Nd同位素组成(εNd=~+5)(Yang et al., 2007; Zhang et al., 2010a; Zhou et al., 2009)，来自于对流地幔。形成如此大规模的玄武岩需要一个巨大的热源提供足够的热使得岩石圈部分熔融。热力学模拟结果表明冷、干的岩石圈地幔不可能发生大规模的熔融形成大陆溢流玄武岩 (Arndt and Christensen, 1992)，但是如果岩石圈地幔先前被挥发分和熔体交代富集，那么在地幔柱的传导加热下在理论上可以发生大程度部分熔融 (Gallagher and Hawkesworth, 1992; Turner et al., 1996)。岩石圈-地幔柱相互作用在塔里木大火成岩省的形成中扮演了很重要的角色：早期的岩浆来自于岩石圈地幔，地幔柱主要提供热源；晚期的岩浆来自于对流地幔，地幔柱提供物源。
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图 9 塔里木大火成岩省岩浆岩年龄分布图 数据来源：杨树峰等, 1996, 2006; 李勇等, 2007; 张洪安等, 2009; 余星, 2009; 上官时迈等, 2011; 位荀和徐义刚, 2011; 于峻川等, 2011; Tian et al., 2010; Yu et al., 2011b; Zhang et al., 2008, 2010a, 2012 Fig. 9 Compilation of representative ages of magmatic rocks from the TLIP Data sources: Li et al., 2007; Shangguan et al., 2011; Tian et al., 2010; Wei and Xu, 2011; Yang et al., 1996, 2006; Yu et al., 2009, 2011a, b ; Zhang et al., 2008, 2009, 2010a, 2012 |
任何地球动力学模式，都需要解释塔里木大火成岩省的两期岩浆时间、空间分布特征及它们之间存在的地球化学差异。在塔里木大火成岩省形成过程中，岩石圈-地幔柱的相互作用可能扮演了很重要的角色。现今的塔里木克拉通具有厚、冷的岩石圈地幔(>140km)(安美建和石耀霖, 2006; Liu et al., 2004; Priestley et al., 2006)。二叠纪以后塔里木没有明显的岩浆活动记录(新疆维吾尔自治区地质矿产局, 1993)，暗示二叠纪后塔里木岩石圈并未发生明显的减薄。如果假设二叠纪时塔里木也具有比较厚的岩石圈地幔(>140km)，当地幔柱上升至岩石圈底部时，巨厚的岩石圈地幔会阻止其继续上升，从而阻碍其减压熔融 (Davies, 1994; Foley, 2008; Jourdan et al., 2007; Sleep et al., 2002)(图 10a)；但不断积累在岩石圈底部的地幔柱物质会向岩石圈厚度比较薄的边缘地区侧向流动 (Sleep et al., 2002)，并提供足够的热，促使早期交代富集的岩石圈地幔发生部分熔融，形成~290Ma的溢流玄武岩(图 10b)。
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图 10 塔里木大火成岩省形成的动力学示意图(据徐义刚等, 2013修改) Fig. 10 A cartoon illustrating the formation of the TLIP (modified after Xu et al., 2013) |
巴楚岩墙具有和OIB相似的地球化学特征，暗示它们来自对流软流圈地幔源区。Lebedev et al. (2006) 认为克拉通下的软流圈地幔物质流动和其导致的克拉通边缘减压熔融，可以解释小体积、分散并且具有OIB特征玄武岩的成因。塔里木盆地~280Ma的岩浆活动以体积小和分布分散为特征，主要分布在盆地的边缘，如塔里木盆地西缘的巴楚和皮羌等地(Zhang et al., 2008, 2010a; Zhang and Zou, 2013)。这些特征和地幔柱物质侧向流动至岩石圈薄的盆地边缘并发生减压熔融模型预测的非常吻合。另外，形成的玄武质岩浆还可以侵位到地壳中，诱发地壳的熔融，形成具有地壳特征的长英质火山岩(图 10c)(于峻川等, 2011)。
6 结论(1) 野外地质关系指示巴楚辉绿岩墙属于塔里木大火成岩省的第二期岩浆活动 (~280Ma)。巴楚岩墙具有较大的εNd值范围(-2.6~+5.1)，其中样品XHZ-10含有年龄为717~2480Ma的继承锆石，暗示这些岩墙在侵位过程中同化混染了元古代的基底物质。受混染程度最小的样品具有与OIB十分相似的微量元素特征及亏损的Nd同位素组成(εNd=~+5)，暗示其来源于富集的软流圈地幔源区，与主要来自富集岩石圈地幔的早期(~290Ma)玄武岩形成鲜明对比。
(2) 岩石圈-地幔柱相互作用在塔里木大火成岩省的形成中扮演了很重要的角色：早期(~280Ma)的岩浆来自于岩石圈地幔，地幔柱主要提供热源；晚期的岩浆来自于软流圈地幔，地幔柱提供物源。地幔柱侧向流动模型可以合理地解释塔里木大火成岩省两期岩浆的时间、空间展布特征以及地球化学差异。
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