岩石学报  2017, Vol. 33 Issue (1): 16-30   PDF    
引用本文
李甘雨, 李永军, 王冉, 杨高学, 向坤鹏, 刘佳, 佟丽莉. 2017.西准噶尔哈拉阿拉特山一带晚石炭世赞岐岩的发现及其地质意义. 岩石学报, 33(1): 16-30  
Li GY, Li YJ, Wang R, Yang GX, Xiang KP, Liu J and Tong LL. 2017. The discovery and significance of Late Carboniferous sanukitoids in Hala'alate Mountain, West Junggar. Acta Petrologica Sinica, 33(1): 16-30(in Chinese with English abstract)   
西准噶尔哈拉阿拉特山一带晚石炭世赞岐岩的发现及其地质意义
李甘雨1, 李永军1,2, 王冉1,2, 杨高学1,2, 向坤鹏1,3, 刘佳1,4, 佟丽莉1,2     
1. 长安大学地球科学与资源学院, 西安 710054;
2. 国土资源部岩浆作用成矿与找矿重点实验室, 西安 710054;
3. 贵州省地质矿产开发局贵州省地质调查院, 贵阳 550005;
4. 陕西省地矿局综合地质大队, 渭南 714099
2016-06-19 收稿; 2016-10-09 改回.
基金项目: 本文受中国地质调查局地质矿产调查评价专项（1212011220619）、国家自然科学基金项目（41273033、41303027）、中央高校基本科研业务费专项资金（310827165016、310827153506、310827153407）和陕西省科技新星（2016KJXX-71）联合资助
第一作者简介: 李甘雨, 男, 1990年生, 博士生, 地球化学专业, E-mail:liganyuchd@163.com
通讯作者: 李永军, 男, 1961年生, 教授, 博士生导师, 主要从事区域地质学及地球化学调查研究, E-mail:yongjunl@chd.edu.cn
摘要: 西准噶尔哈拉阿拉特山一带广泛分布晚石炭世玄武安山岩、辉石安山岩，属钙碱性系列，岩石具有较高的SiO2（52.88%~56.89%）、MgO（3.47%~6.88%，Mg#为48.5~63.7）、Sr（442×10-6~970×10-6）、Ba（199×10-6~796×10-6）含量，K/Na为0.22~0.70，P2O5变化范围较大（0.18%~0.52%），富集大离子亲石元素和轻稀土元素（（La/Yb）N为1.88~15.9），亏损Nb、Ta、Hf等高场强元素和重稀土元素，弱负Eu异常（δEu=0.77~0.94），（87Sr/86Sr）i=0.70366~0.70409，（143Nd/144Nd）i=0.51247~0.512564，εNd（t）=4.41~6.19，206Pb/204Pb=18.220~18.405，207Pb/204Pb=15.482~15.522，208Pb/204Pb=37.991~38.296，与典型赞岐岩地球化学特征一致。该赞岐岩的厘定，为研究西准噶尔构造演化提供了新的思路，约束了本区残余洋盆的闭合时限并非前人确立的早石炭世，而应延迟至晚石炭世末期。
关键词: 赞岐岩     板片熔体交代     岛弧构造环境     晚石炭世     西准噶尔     新疆    
The discovery and significance of Late Carboniferous sanukitoids in Hala'alate Mountain, West Junggar
LI GanYu1, LI YongJun1,2, WANG Ran1,2, YANG GaoXue1,2, XIANG KunPeng1,3, LIU Jia1,4, TONG LiLi1,2     
1. Earth Science & Resources College, Chang'an University, Xi'an 710054, China;
2. Key Laboratory for the Study of Focused Magmatism and Giant Ore Deposits, MLR, Xi'an 710054, China;
3. Guizhou Geological Survey, Bureau of Geology and Mineral Exploration and Development of Guizhou Province, Guiyang 550005, China;
4. Geological Brigade of Shaanxi Exploration and Development Corporation of Geology and Mineral Resources, Weinan 714099, China
Abstract: The Late Carboniferous volcanic rocks consist of basaltic andesite and pyroxene andesite which are widespread in Hala'alate Mountain, West Junggar. The volcanic rocks belong to calc-alkaline series and show a remarkable geochemical affinity with Cenozoic sanukitoids of the Setouchi Volcanic Belt of SW Japan with high SiO2 (52.88%~56.89%), MgO (3.47%~6.88%, Mg# ranging from 48.5 to 63.7), Sr (442×10-6~970×10-6), Ba (199×10-6~796×10-6), K/Na ranging from 0.22 to 0.70, P2O5 changing with a wide range (0.18%~0.52%). Moreover, all samples are enriched in large-ion lithophile elements and light rare earth elements ((La/Yb)N=1.88~15.9), but strongly depleted in some high field strength elements (e.g. Nb, Ta and Hf) and heavy rare earth elements with slight negative Eu anomalies (δEu=0.77~0.94). Additionally, the volcanic rocks have the same characteristics of Sr-Nd-Pb isotopes as typical sanukitoids ((87Sr/86Sr)i=0.70366~0.70409, (143Nd/144Nd)i=0.51247~0.512564, εNd(t)=4.41~6.19, 206Pb/204Pb=18.220~18.405, 207Pb/204Pb=15.482~15.522, 208Pb/204Pb=37.991~38.296). The confirmation of sanukitoids in Hala'alate Mountain proofs that it provides a new idea for studying the evolution of West Junggar, and provides important constraints on the remnant ocean basin closed time of West Junggar, meanwhile it indicate that the closed time should be postponed to the end of Late Carboniferous instead of the Early Carboniferous.
Key words: Sanukite     Metasomatism of slab melts     Island arc tectonic setting     Late Carboniferous     West Junggar     Xinjiang    

Sanukite (赞岐岩)最早由Weinschenk (1891)发现于日本中新世(11~14Ma) Setouchi火山岩带，最初按其矿物成分定名为“古铜辉石安山岩”，后又依其发现地Sanuki取名Sanukite (译“赞岐岩”)，主要由玻璃、斜方辉石、磁铁矿和斜长石组成，可含少量橄榄石、斜方辉石或单斜辉石斑晶。岩石化学成分以富SiO2(>52%)、MgO (通常>5%，Mg#为45~75)和高的Cr (>100×10-6)、Ni (>100×10-6)及K/Na (0.33~0.52)为特征，富集LILE和LREE，亏损高场强元素，通常具弱的负Eu异常，主要产于与俯冲作用有关的岛弧环境(Tatsumi, 1981, 1982; 张旗等, 2004, 2005)。

赞岐岩是一种极为独特和少见的新岩石类型，受到国内外众多地球化学家们的广泛关注。国外很早就开始对赞岐岩进行研究(Tatsumi, 1981, 1982, 2008; Tatsumi and Ishizaka, 1981, 1982; Shirey and Hanson, 1984; Stern et al., 1989; Tatsumi et al., 2003; Kamei et al., 2004; Martin et al., 2005)，而国内相关报道少而滞后。张旗等(2004, 2005)首先对赞岐岩概念及其在地壳早期演化中的意义进行阐述，随后在内蒙古固阳晚太古代英云闪长岩(简平等, 2005)、吉林珲春三叠纪高镁闪长岩(付长亮等, 2010)和大兴安岭富西里新元古代侵入岩(边红业等, 2014)中有赞岐岩的发现。近期报导的赞岐岩时代均为晚古生代，产地也全在新疆境内。北天山一处，为早石炭世火山岩，分布于果子沟-阿希一线(王强等, 2006; Wang et al., 2007)；西准噶尔有三处, 分别是：1)谢米斯台山中志留世火山岩(孙勇等, 2015)；2)哈图早二叠世基性岩墙群(尹继元等, 2012; Yin et al., 2015)；3)克拉玛依后山晚石炭世基性岩墙群(Yin et al., 2010; Ma et al., 2012)。

赞岐岩一名目前被广泛冠名于具有相似特征的火山岩和侵入岩(Tatsumi and Ishizaka, 1982)，而在西准噶尔地区前人报道的晚石炭世-早二叠世赞岐岩均为中基性岩墙(Yin et al., 2010, 2015; 尹继元等, 2012; Ma et al., 2012)，未见赞岐岩类火山岩的报道。笔者等在西准噶尔哈拉阿拉特山一带进行1：5万区域地质调查时，首次发现区内晚石炭世火山岩同样具有与日本Setouchi火山岩带中赞岐岩类似的特征。这一重要发现，为研究西准噶尔甚至是中亚造山带晚古生代的构造演化历史提供了新的思路，丰富了我国赞岐岩的产地与层位，同时也为研究该特殊岩类的地球化学特征提供了更多信息。

1 地质概况与岩石学特征

西准噶尔包古图-哈拉阿拉特山一带石炭纪地层极为发育，早石炭世地层主要出露于包古图-哈图一带，以包古图组和希贝库拉斯组为代表，形成于弧后盆地，研究程度较高(王瑞和朱永峰, 2007; 安芳和朱永峰, 2009; 佟丽莉等, 2009, 2014; 李永军等, 2010; 郭丽爽等, 2010; Geng et al., 2011; 孙羽等, 2014a, b)；晚石炭世主要出露于乌尔禾北哈拉阿拉特山一带，地层单位有成吉思汗山组、哈拉阿拉特组及阿腊德依克赛组(图 1)，对其形成构造环境研究较少。在哈拉阿拉特山一带，早二叠世佳木河组陆相磨拉石建造角度不整合于哈拉阿拉特组及阿腊德依克赛组之上，因此，长期以来，区内主流观点认为晚石炭世已完成了洋盆的关闭并进入陆内造山阶段(沈远超, 1993; 金成伟和张秀棋, 1993; 何国琦等, 2001; 韩宝福等, 2006; 王京彬和徐新, 2006; 苏玉平等, 2006; 徐新等, 2010; 高睿等, 2013)。

图 1 西准噶尔地区大地构造示意图(a, 据Chen et al., 2010; Xu et al., 2012; 王金荣等, 2013)及西准噶尔包古图-哈拉阿拉特山一带地质简图(b, 据孙羽等, 2014b修改) 1-二叠系；2-阿腊德依克赛组；3-哈拉阿拉特组；4-成吉思汗山组；5-希贝库拉斯组；6-包古图组；7-泥盆系；8-奥陶系-志留系；9-花岗岩基；10-蛇绿构造混杂岩带；11-基性岩脉；12-辉绿岩；13-断层；14-角度不整合 Fig. 1 Schematic tectonic map showing main tectonic units of the West Junggar (a, after Chen et al., 2010; Xu et al., 2012; Wang et al., 2013) and geological map of Baogutu-Hala'alate Mountain area (b, after Sun et al., 2014b) 1-Permian; 2-Aladeyikesai Fm.; 3-Hala'alate Fm.; 4-Chengjisihanshan Fm.; 5-Xibeikulasi Fm.; 6-Baogutu Fm.; 7-Devonian; 8-Ordovician-Silurian; 9-granite; 10-ophiolite tectonic melange belt; 11-mafic dikes; 12-diabase; 13-fault; 14-unconformity

本文报道火山岩见于哈拉阿拉特山晚石炭世哈拉阿拉特组与阿腊德依克赛组中(图 2)，哈拉阿拉特组为一套滨-浅海相火山-沉积岩建造，岩性以深灰色安山岩、灰黑色玄武岩、深灰色辉石安山岩、灰褐色火山角砾岩、灰色杏仁状安山岩为主，夹薄层状中粗砂岩、细砾岩，可见少量流纹岩，总体显示为一套浅海相钙碱性火山岩组合，火山岩中获得的锆石U-Pb年龄为304.5~306.9Ma (李甘雨等, 2015)，与前人在本组中发现的化石所示地质时代吻合；而阿腊德依克赛组以陆源碎屑岩为主，火山岩呈夹层状，岩性以玄武岩、玄武安山岩、安山岩以及火山碎屑岩为主，本组灰岩夹层中产珊瑚类Bradyphyllum sp.和Zaphrentites sp.、腕足类Balakhonia cf.silimica，Brachythyrina pingusiformis等化石(卡西莫夫期)，玄武岩LA-ICP-MS锆石U-Pb年龄为303.8±2.4Ma (向坤鹏等, 2015)。

图 2 西准噶尔哈拉阿拉特山一带区域地质图 Fig. 2 Geological map of Hala'alate Mountain area, West Junggar

用于本研究的样品采自哈拉阿拉特组与阿腊德依克赛组基岩露头，采样位置见图 2。采集时尽量避开接触带、蚀变带和断裂破碎带等，以保证样品新鲜且具有代表性。用于地球化学分析的样品岩性主要为辉石安山岩和玄武安山岩：辉石安山岩具斑状结构，块状构造(图 3a)，岩石由斑晶(10%~15%)和基质(85%~90%)组成，斑晶主要为斜长石(8%~10%)和普通辉石(2%~5%)，斜长石呈半自形板状，粒径0.5×0.15~1.7×0.8mm，聚片双晶发育，普通辉石呈柱状、粒状，粒径0.3~1.2mm，淡绿色，具辉石式解理，基质具交织结构，斜长石之间分布玻璃质和暗色矿物，可见少量磁铁矿(图 3b)；玄武安山岩具斑状结构，块状构造(图 3c)，斑晶主要为半自形板状斜长石(10%~15%)、粒状橄榄石(3%~5%)及少量普通辉石，基质由斜长石(55%~60%)、玻璃质(10%~12%)、暗色矿物(5%~10%)及少量磁铁矿组成，其中斜长石长径0.03~0.1mm，可见聚片双晶(图 3d)。

图 3 哈拉阿拉特山地区晚石炭世火山岩宏观露头及镜下照片 Cpx-单斜辉石；Pl-斜长石 Fig. 3 Macroscopic and microscopic photos of the volcanic rocks of Late Carboniferous in Hala'alate Mountain area Cpx-clinopyroxene; Pl-plagioclase
2 地球化学特征及构造环境

火山岩样品主量与微量元素由长安大学教育部重点实验分别用XRF和ICP-MS方法进行测定，元素含量及有关参数见表 1。SiO2含量为52.88%~56.89%，平均为55.5%；TiO2含量为0.96%~1.33%，变化范围较大，平均为1.05%，明显低于MORB平均值1.5%；具有较高的MgO (3.47%~6.88%，Mg#为48.5~63.7)、Al2O3(16.25%~18.97%)和P2O5(0.18%~0.52%)。在TAS硅碱图中所有样品均落入亚碱性岩区(图 4a)，考虑到由于该地区火山岩经历了蚀变作用和构造变形，易发生K、Na等活动性元素的迁移，因而，进一步利用不活泼元素SiO2-Zr/TiO2×0.0001图解，样品均落入安山岩区域(图 4b)，与TAS图基本一致。样品的全碱含量(K2O+Na2O=4.51%~7.39%)较高，相对富钠(Na2O的含量为3.42%~4.96%，平均值为4.13%)，K2O含量为0.79%~2.84%，平均为1.47%，属钙碱性系列(图 5)。

表 1 哈拉阿拉特山一带晚石炭世火山岩主量元素(wt%)和微量元素(×10-6)及有关参数 Table 1 The concentration of major elements (wt%) and trace elements (×10-6) and their parameters for volcanic rocks from Late Carboniferous in Hala'alate Mountain area

图 4 西准噶尔哈拉阿拉特山地区晚石炭世火山岩TAS图(a, 据Le Bas et al., 1986)及SiO2-Zr/TiO2×0.0001图解(b, 据Winchester and Floyd, 1977) Fig. 4 TAS (a, after Le Bas et al., 1986) and SiO2 vs. Zr/TiO2×0.0001 (b, after Winchester and Floyd, 1977) diagrams of the volcanic rocks of Late Carboniferous in Hala'alate Mountain area, West Junggar

图 5 西准噶尔哈拉阿拉特山一带晚石炭世火山岩AFM图(a, 据Irvine and Baragar, 1971)及SiO2-K2O图解(b, 据Miller et al., 1999) Fig. 5 AFM (a, after Irvine and Baragar, 1971) and SiO2 vs. K2O (b, after Miller et al., 1999) diagrams of the volcanic rocks of Late Carboniferous in Hala'alate Mountain area, West Junggar

在球粒陨石标准化稀土元素(REE)配分曲线图上火山岩均表现出轻稀土元素富集而重稀土相对亏损的右倾型特征，其中哈拉阿拉特组火山岩轻稀土元素富集尤为显著(图 6a, c、表 1)。样品具有较高的稀土总量(∑REE=48.02×10-6~127.5×10-6)，且轻重稀土元素分异明显((La/Yb)N=1.88~15.9)，与岛弧钙碱性火山岩的(La/Yb)N值相似。(La/Sm)N值均大于1(1.12~2.68)，反映轻稀土之间分馏程度较好，而未发生明显的重稀土分馏((Gd/Yb)N=1.48~3.72)，具有弱的Eu负异常(δEu=0.77~0.94)，无明显Ce异常(δCe=0.99~1.16)，表明原始岩浆演化过程中可能经历了斜长石的分离结晶作用。

图 6 哈拉阿拉特山地区晚石炭世火山岩球粒陨石标准化稀土元素配分图(a、c, 标准化值据Boynton, 1984)及原始地幔标准化多元素蛛网图(b、d, 标准化值据Sun and McDonough, 1989) 图中西准噶尔哈图地区赞岐岩数据尹继元等(2012)，Yin et al. (2015)；西准噶尔克拉玛依后山地区赞岐岩数据引自Yin et al. (2010)，Ma et al. (2012) Fig. 6 Chondrite-normalized REE patterns (a, c, normalization values after Boynton, 1984) and primitive mantle-normalized trace element spider diagram (b, d, normalization values after Sun and McDonough, 1989) for volcanic rocks of Late Carboniferous in Hala'alate Mountain area The data of the Hatu area from Yin et al.(2012, 2015); Data of the northwestern Karamay from Yin et al. (2010), Ma et al. (2012)

样品均表现出亏损Nb (1.09×10-6~7.32×10-6)、Ta (0.08×10-6~0.35×10-6)、Th (0.79× 10-6~2.09×10-6)、Hf (1.70×10-6~2.48×10-6)、等高场强元素(HFSE)和相对富集Ba (199×10-6~796×10-6)、Rb (7.54×10-6~21.0×10-6)、Sr (442×10-6~970×10-6)等大离子亲石元素(LILE)的地球化学性质，而本区Cr (12.11×10-6~206.9×10-6)、Ni (10.38×10-6~115.8×10-6)含量则相对略低，所有样品在图中有较明显的Nb-Ta槽，具有岛弧火山岩的地球化学特征(图 6b, d)。样品中Nb/Ta比值均集中在12.1~20.9，Zr/Hf比值为37.6~49.4，略高于原始地幔值(Nb/Ta=17, Zr/Hf=37, Sun and McDonough, 1989)。哈拉阿拉特山晚石炭世火山岩样品具有相似的元素分布模式，表明两者可能来自相似源区以及成岩过程。

哈拉阿拉特组与阿腊德依克赛组火山岩具有相似的Sr-Nd-Pb同位素组成(表 2)。测试获得87Sr/86Sr为0.703832~0.70447，143Nd/144Nd为0.512699~0.512900，计算(87Sr/86Sr)i变化范围为0.70366~0.70409，具有正的εNd(t)(4.41~6.19)，将其与岛弧玄武岩(IAB)作对比，表明其可能来源于亏损地幔。在Sr、Nd图上的投点较集中，与西准噶尔哈图地区赞岐岩分布范围相吻合，均落入西准噶尔早石炭世岛弧火山岩区域(图 7a)。206Pb/204Pb为18.220~18.405，207Pb/204Pb为15.482~15.522，208Pb/204Pb为37.991~38.296，计算得(206Pb/204Pb)i变化范围为17.7558~17.8977，(207Pb/204Pb)i为15.4549~15.5038，(208Pb/204Pb)i为37.6086~37.7536，与日本Setouchi火山岩带新生代赞岐岩类一致(Tatsumi et al., 2003)，均落入地球等时线右侧(图 7b, c)。6件样品的Sr、Nd、Pb初始比值变化范围较小，暗示其指示同一岩浆源区。

表 2 哈拉阿拉特山地区晚石炭世火山岩的Sr-Nd-Pb同位素组成 Table 2 Sr-Nd-Pb isotopic compositions for volcanic rocks of Late Carboniferous in Hala'alate Mountain area

图 7 哈拉阿拉特山地区晚石炭世火山岩εNd(t)-(87Sr/86Sr)i图解(a)及206Pb/204Pb与207Pb/204Pb (b, 据Zindler and Hart, 1986)、208Pb/204Pb相关图(c, 据Allègre et al., 1988) 西准噶尔早石炭世岛弧火山岩数据引自Geng et al. (2011)；西准噶尔哈图地区赞岐岩数据尹继元等(2012)，Yin et al. (2015)；西准噶尔克拉玛依后山地区赞岐岩数据引自Yin et al. (2010)，Ma et al. (2012)；日本Setouchi火山岩带新生代赞岐岩数据引自Tatsumi et al. (2003) Fig. 7 εNd(t) vs. (87Sr/86Sr)i diagram (a) and correlogram of 206Pb/204Pb vs. 207Pb/204Pb (b, Zindler and Hart, 1986), 206Pb/204Pb vs. 208Pb/204Pb (c, after Allègre et al., 1988) for volcanic rocks of Late Carboniferous in Hala'alate Mountain area Early Carboniferous volcanic rocks value from West Junggar after Geng et al. (2011); data of the Hatu area from Yin et al.(2012, 2015); data of the northwestern Karamay from Yin et al. (2010), Ma et al. (2012); Sanukitoid data of Setouchi volcanic belt are from Tatsumi et al. (2003)

哈拉阿拉特山一带晚石炭世火山岩样品具有较高的MgO含量(3.47%~6.88%，Mg#=48.5~63.7)，且K/Na值为0.22~0.70，富集大离子亲石元素(LILE)和轻稀土元素(LREE)，亏损高场强元素(HFSE)，弱负铕异常，正的εNd(t)(4.41~6.19)与较低(87Sr/86Sr)i值(0.70366~0.70409)，206Pb/204Pb=18.220~18.405，207Pb/204Pb=15.482~15.522，208Pb/204Pb=37.991~38.296，与赞岐质高Mg安山岩地球化学特征类似(表 3)。然而值得说明的是，哈拉阿拉特组火山岩具有高Sr (634×10-6~970×10-6)，Ba (269×10-6~796×10-6)及Sr/Y (61.3~84.3)比值等特征，极易与埃达克岩混淆，而典型的埃达克岩SiO2≥56%，MgO一般 < 3%(很少超过6%)，通常表现出正铕异常，与该套火山岩特征不符，综合对比后认为其与克拉玛依后山地区赞岐岩类极为相似(图 8, Yin et al., 2010; Ma et al., 2012)；而阿腊德依克赛组火山岩则表现为较低的Sr (442×10-6~509×10-6)，Ba (199×10-6~485×10-6)及Sr/Y (25.0~30.3)比值，与日本Setouchi火山岩带和哈图地区(尹继元等, 2012; Yin et al., 2015)赞岐岩地球化学特征基本一致(图 8)。

表 3 哈拉阿拉特山地区火山岩与典型赞岐岩及区内前人报道赞岐岩对比表 Table 3 The comparison among volcanic rocks in Hala'alate Mountain area, typical Sanukitoid and Sanukitoid reported by predecessor in this area

图 8 哈拉阿拉特山晚石炭世火山岩的SiO2-MgO图解(a, 底图据Mccarron and Smellie, 1998)、(La/Yb)N-YbN图解(b, 底图据Kamei et al., 2004)及TiO2-MgO/(MgO+FeOT)图解(c, 底图据Kamei et al., 2004) 克拉玛依后山地区赞岐岩数据引自Yin et al. (2010)，Ma et al. (2012)；哈图地区赞岐岩数据据尹继元等(2012)；Yin et al. (2015) Fig. 8 SiO2 vs. MgO (a, after Mccarron and Smellie, 1998), (La/Yb)N vs. YbN (b, after Kamei et al., 2004) and TiO2 vs. MgO/(MgO+FeOT) (c, after Kamei et al., 2004) diagrams for volcanic rocks of Late Carboniferous in Hala'alate Mountain area Data of the northwestern Karamay from Yin et al. (2010), Ma et al. (2012); data of the Hatu area from Yin et al.(2012, 2015)

哈拉阿拉特组与阿腊德伊克赛组由陆源细碎屑岩和火山岩组成，含有较多生物碎屑灰岩条带，产大量腕足、珊瑚、双壳等化石，整体为滨海相沉积。火山岩主要由玄武岩、玄武安山岩和安山岩组成，代表了区内海相沉积相关最晚火山活动的产物。同时，较高的Mg#值(48.5~63.7)、Al2O3含量(16.25%~18.97%)，Nb、Ta呈现明显的亏损，正的εNd(t)值(4.41~6.19)等特征表明，其源区可能与俯冲相关。其中，哈拉阿拉特组赞岐岩具有与埃达克岩类似的地球化学特征，且与克拉玛依后山地区赞岐岩类极为相似，通常被认为是形成于受埃达克质板片熔体交代的地幔楔的部分熔融(图 9, Ma et al., 2012; Tang et al., 2012a; Yin et al., 2013)；而阿腊德依克赛组赞岐岩以高的Th/La和Th/Yb值为特征类似于日本Setouchi火山岩带和哈图地区赞岐岩，被认为是形成于富集俯冲大洋沉积物的地幔橄榄岩的部分熔融(Tatsumi, 2001, 2008; Yin et al., 2015)。总之，区内晚石炭世火山岩均表现出与俯冲环境相关的特征。

图 9 哈拉阿拉特山晚石炭世赞岐岩Th/Yb-Ba/La (a)及Th/La-Sr/Y (b)图解 西准噶尔哈图地区赞岐岩数据尹继元等(2012)，Yin et al. (2015)；西准噶尔克拉玛依后山地区赞岐岩数据引自Yin et al. (2010)，Ma et al. (2012)；日本Setouchi火山岩带新生代赞岐岩数据引自Tatsumi et al. (2003) Fig. 9 Th/Yb vs. Ba/La diagram (a) and Th/La vs. Sr/Y diagram (b) for volcanic rocks of Late Carboniferous in Hala'alate Mountain area Data of Hatu area are from Yin et al.(2012, 2015a). Data of northwestern Karamay area are from Yin et al. (2010) and Ma et al. (2012). Data of Setouchi Volcanic Belt are from Tatsumi et al. (2003)
3 地质意义

西准噶尔在古生代表现为洋内弧的俯冲体系(Xiao et al., 2010)，到了晚石炭世其构造环境却存在较大争议：一是形成于岛弧环境(肖文交等, 2006, 2008; Xiao et al., 2008; 唐功建等, 2009)，一是形成于后碰撞环境(Chen and Arakawa, 2005; 苏玉平等, 2006; 韩宝福等, 2006)。最新研究结果显示，西准噶尔地区存在石炭纪的埃达克岩-高镁安山岩-富Nb玄武质岩组合：西准噶尔西部巴尔努克山一带早石炭世黑山头组中的玄武质岩具有富Nb岛弧玄武岩的地球化学特征(李永军等, 2014)；埃达克岩则分布于西准噶尔中部达尔布特断裂以南的包古图地区，主要为中酸性小斑岩体，与铜金矿化关系密切(张连昌等, 2006; 唐功建等, 2009)；此外，在西准噶尔东部可见高镁安山岩分布，样品地球化学特征类似于日本Setouchi火山岩带中的赞岐岩类。这一特殊岩石组合特征指示，西准噶尔地区在整个石炭纪可能为岛弧环境(图 10)。

图 10 哈拉阿拉特山晚石炭世赞岐岩构造环境判别图 (a) TiO2×10-Al2O3-K2O×10图解(赵崇贺, 1989)；(b) Rb/10-Hf-Ta×3(Pearce, 1982)；(c) Hf/3-Th-Ta图解(Wood, 1980) Fig. 10 Tectonic discrimination diagrams of Late Carboniferous Sanukitoids in in Hala'alate Mountain area (a) TiO2×10-Al2O3-K2O×10 diagram (Zhao, 1989); (b) Rb/10-Hf-Ta×3 diagram (Pearce, 1982); (c) Hf/3-Th-Ta diagram (Wood, 1980)

前人报道西准噶尔石炭纪的俯冲作用多位于西准噶尔西部，时代均为早石炭世(赵振华等, 2006; Shen et al., 2008; 田陟贤等, 2013; 李永军等, 2014)。有学者认为，准噶尔洋在385Ma之前向博什库尔-成吉思岩浆弧及准噶尔板块之下形成双向俯冲，而在358~342Ma哈萨克斯坦板块和准噶尔板块可能发生碰撞，最终导致准噶尔洋的完全闭合(陈博和朱永峰, 2011; Zhu et al., 2013, 2015)。然而，越来越多的学者通过对西准噶尔蛇绿构造混杂岩、埃达克岩及A型花岗岩的研究，认为西准噶尔乃至整个中亚造山带从泥盆纪到晚石炭世存在一个俯冲的过程(Geng et al., 2009; Tang et al., 2012a, b, c)，与本文所述晚石炭世赞岐岩形成于岛弧环境这一结论相一致。更为重要的是，近年来多位学者在西准噶尔包古图-哈图地区的中基性岩墙群和深成小岩体中发现和报道了赞岐岩的存在，均分布于达尔布特断裂两侧，时代多集中于晚石炭世-早二叠世(Yin et al., 2010, 2015; Ma et al., 2012; 尹继元等, 2012)，与本文报道的赞岐岩类火山岩在产出位置与形成时间上一致，显示二者之间存在着密切的成因联系。最有可能的解释是西准早石炭世与晚石炭世-早二叠世地质体是两次由南向北的俯冲增生体，当早石炭世完成俯冲增生拼贴后，已进入陆内后碰撞造山，而其南的晚石炭世仍处在岛弧环境，持续进行沉积和俯冲过程，形成赞岐质岛弧火山岩，同时，向北部地区在已进入陆内后碰撞造山的早石炭世地层内，在形成后造山花岗质岩浆的过程中，与赞岐质岛弧火山岩同源的赞岐质侵入岩沿达尔布特大断裂上侵，一部分形成独立的小侵入体，另一部分与同期的壳源后碰撞花岗质岩浆相遇，形成岩浆混合花岗岩或是成为浆混岩中的幔源包体及基性岩墙群。

西准噶尔位于中亚造山带西南缘，具有复杂造山演化历史(Kwon et al., 1989; Yang et al., 2012a, b, c, 2013, 2015; Chen et al., 2014; Zhu et al., 2015)。然而，该区大陆地壳增生机制仍存在较大争议(Şengör et al., 1993; Windley et al., 2007; Xiao et al., 2010, 2015; Wilhem et al., 2012; Kröner et al., 2014; Xiao and Santosh, 2014)。研究认为，岛弧环境不仅可以产生本文所述赞岐岩，同时也能生成大量的年轻的大陆地壳。因此，综合前人研究成果表明，多期次的俯冲增生作用在西准噶尔乃至中亚造山带的构造演化及地壳增长过程中可能发挥着至关重要的作用。

4 结论

(1)晚石炭世哈拉阿拉特组与阿腊德依克赛组火山岩岩石地球化学特征、Sr-Nd-Pb同位素组成与经典赞岐岩总体有较好的可比性，可以判定其为赞岐岩类。

(2)哈拉阿拉特组赞岐岩形成于受埃达克质板片熔体交代的地幔楔的部分熔融，而阿腊德依克赛组赞岐岩则形成于富集俯冲大洋沉积物的地幔橄榄岩的部分熔融。

(3)哈拉阿拉特山地区晚石炭世赞岐质火山岩的发现和报道在区内尚属首次，这为确认西准噶尔石炭纪存在赞岐质火山岩提供了详实的地质资料，为研究西准噶尔俯冲增生机制提供了重要的地球化学信息。

致谢 主量元素和稀土微量元素分析得到长安大学王柱命和何克老师的支持和帮助; 三位审稿专家对本文进行认真修改并提出建设性意见; 在此一并表示感谢。
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