新疆可可托海近3号脉花岗岩成岩时代及地球化学特征研究**

2014-03-14 06:47刘锋曹峰张志欣李强LIUFengCAOFengZHANGZhiXinandLIQiang
岩石学报 2014年1期
关键词:阿尔泰造山黑云母

刘锋 曹峰 张志欣 李强LIU Feng, CAO Feng, ZHANG ZhiXin and LI Qiang

1. 国土资源部成矿作用与资源评价重点实验室,中国地质科学院矿产资源研究所,北京 1000372. 新疆地矿局地球物理化学探矿大队,昌吉 8311003. 中国科学院新疆生态与地理研究所,新疆矿产资源研究中心,乌鲁木齐 830011 1. MRL Key Laboratory of Metallogeny and Mineral Assessment, Institute of Mineral Resources, Chinese Academy of Geological Sciences, Beijing 100037, China2. Geophysical and Geochemical Party, Xinjiang Bureau of Geology and Mineral Resource Exploration and Development, Changji 831100, China3. Xinjiang Research Center for Mineral Resources, Xinjiang Institute of Ecology and Geography, Chinese Academy of Sciences, Urumqi 830011, China2013-08-25 收稿, 2013-12-08 改回.

1 引言

阿尔泰造山带是中亚造山带(CAOB)的一部分。在中国新疆境内阿尔泰,大面积出露侵入岩尤其是花岗岩类是其显著特征之一。这些花岗岩类岩石类型众多,具有多时代、多类型、多成因、形成于多种构造环境的特征(王广耀和许培春,1983;芮行健和吴玉金,1984;邹天人等, 1988;刘伟,1990;岳永君等,1990;赵振华等,1993;王中刚等,1998;袁峰等,2001;王登红等,2002;Wangetal., 2006; Zhuetal., 2006;张招崇等,2006;Yuanetal., 2007;周刚等,2007;杨富全等,2008;刘锋等,2009,2010,2012a;柴凤梅等,2010;张超等,2013)。从目前较可靠的同位素资料来看,新疆阿尔泰花岗岩类形成的主要时期在中奥陶世-早中泥盆世,为同造山花岗岩。最老的花岗岩侵入于460Ma左右(Wangetal., 2006; 刘锋等,2008;柴凤梅等,2010)。岩石成因类型为“I”型和“S”型,并伴随有基性岩浆侵入活动(Wangetal., 2006;陈汉林等,2006;童英等,2007),反映了阿尔泰同造山作用早期陆弧环境下的岩浆活动特征(Wangetal., 2006)。二叠纪花岗岩一般岩体规模较小,多为小岩株、岩脉,岩石成因类型有“I”型、“S”型及“I-A”型(王涛等,2005;童英等,2006;周刚等,2007)。三叠纪以来的岩浆侵入活动相对报道较少。

可可托海矿区内侵入岩非常发育,尤其是花岗岩类,出露面积超过50%。前人针对区内岩浆活动的研究主要集中在伟晶岩脉及其稀有金属矿化,如对3号伟晶岩脉形成时限的研究已有大量结果发表,同时也产生不同认识。邹天人等(1986)利用K-Ar、Rb-S法获得16件3号伟晶岩脉不同矿物组合结构带的时代由120~332Ma变化,认为3号伟晶岩脉的结晶始于早石炭世,一直持续到了燕山期。陈富文等(1999)、王登红等(2002)根据3个结构带的40Ar-39Ar年龄(178Ma、169Ma、148Ma)认为3号伟晶岩脉形成于燕山期。朱永峰和曾贻善(2002)获得Ⅰ带全岩和白云母238Ma的Rb-Sr等时线年龄。Zhuetal.(2006)获得3号脉边缘带中全岩、白云母和磷灰石样品218Ma的Rb-Sr等时线年龄,认为3号脉于218Ma开始结晶,一直持续到148Ma左右。Wangetal. (2007) 则利用SHRIMP锆石U-Pb法获得Ⅰ带、Ⅴ带、Ⅶ带(220±9Ma、198±7Ma、213±6Ma)的年龄。由于早期测年方法的局限性、本区岩石变形变质特点以及伟晶岩中锆石蚀变特征,造成了利用上述方法获得的有关年龄结果变化太大、无规律、精度也较差,因此很难准确界定3号伟晶岩脉的形成时限(刘锋等,2012b)。最近获得的3号脉边缘带中辉钼矿精确的Re-Os年龄基本解决了3号伟晶岩的形成下限问题(刘锋等,2012b)。

相对而言,区内其它多数侵入岩的成岩时代、岩浆形成构造环境和演化等方面的研究较为欠缺,仅少量辉长岩体、花岗岩(邹天人等, 1988; Liuetal., 1997; Wangetal., 2006; Zhuetal., 2006)等的相关研究见诸报端,如SHRIMP U-Pb年龄为409Ma 的3号脉围岩变质辉长岩体(Wangetal., 2006);还如阿拉尔黑云母花岗岩等的年龄多为K-Ar、Rb-Sr等方法获得(刘伟,1993;Liuetal., 1997; Zhuetal., 2006),精度相对较差。我们对区内出露的主要花岗岩体开展工作,目的是确定区内岩浆演化时限、构造环境以及寻找3号伟晶岩脉的花岗质母岩体。野外调查过程中,在3号伟晶岩脉矿坑东侧附近发现有中粗粒似斑状花岗岩小露头,与东部泥盆纪大花岗岩基并不相连,岩性和岩相特征却与矿区东北部的阿拉尔黑云母花岗岩非常相似。它是否和阿拉尔花岗岩为同期岩体?是否为3号伟晶岩脉的花岗质母岩?本期岩浆侵入和阿尔泰造山带区域岩浆活动关系如何?诸如此类问题需要我们利用精确的定年方法、岩石地球化学分析和同位素示踪以及区域对比进行研究、解决,探讨岩浆物源、构造环境以及形成过程,为区内伟晶岩的花岗母岩的寻找、岩浆活动演化特征乃至阿尔泰造山带演化规律的总结提供约束资料。

图1 阿尔泰造山带区域构造图(a)、阿尔泰造山带构造划分(b,据何国琦等,2004)和可可托海区域地质简图(c,据邹天人和李庆昌,2006)Fig.1 Geographic position of Altay orogen in China (a), tectonic subdivisions of the Altay orogen (b, after He et al., 2004) and simplified geological map of Keketuohai area (c, after Zou and Li, 2006)

2 区域地质

中亚造山带(CAOB)是一个经过长期连续的俯冲-增生过程而形成的造山带(Rotarashetal., 1982; Coleman 1989; Mossakovskyetal., 1993;Zhuetal., 2006;Wangetal., 2006; Windleyetal., 2007; Maoetal., 2008, 2013; Xiaoetal., 2010)。阿尔泰造山带是其重要组成部分(Sengöretal., 1993; Yakubchuketal., 2003)(图1a),经历了新元古代晚期到早古生代早期的稳定大陆边缘阶段(何国琦等, 1990),以及古生代时期的地壳双向增生:早古生代为洋壳俯冲阶段,奥陶世(460Ma)开始转变为活动陆缘(Wangetal., 2006; 袁超等, 2007),逐渐发育成典型的沟-弧-盆体系,晚泥盆世以后发生弧-陆碰撞作用,在早石炭世基本形成阿尔泰造山带的构造格架(何国琦等, 1994; Windleyetal., 2002; Lietal., 2003; Xiaoetal., 2004; 王涛等, 2005)。

图2 黑云母二长花岗岩野外特征(a)和镜下特征(b)Q-石英;Pl-斜长石;Mc-微斜长石;Bt-黑云母;Ms-白云母Fig.2 Field photograph (a) and photomicrograph in polarized light (b) of the biotite monzongranite

阿尔泰造山带位于西伯利亚板块和哈萨克斯坦-准噶尔板块之间(图1b)。其南以额尔齐斯大断裂为界与哈萨克-准噶尔板块相接,以北为西伯利亚板块。由北向南,中国境内阿尔泰造山带划分为北阿尔泰晚古生代陆缘活动带的诺尔特泥盆纪-石炭纪上叠火山-沉积盆地、喀纳斯-可可托海古生代岩浆弧,南阿尔泰晚古生代活动陆缘的克兰泥盆纪-石炭纪弧后盆地、卡尔巴-纳雷姆石炭纪-二叠纪岩浆弧、西卡尔巴石炭纪弧前盆地以及额尔齐斯-布尔根碰撞混杂带(何国琦等,2004)。

北阿尔泰北部的诺尔特一带主要由中晚泥盆世-早石炭世火山-沉积岩组成,以“S”型为主的花岗岩侵入时代主要为志留纪、泥盆纪(袁峰等,2001)。中部喀纳斯-可可托海一带出露地层主要为早古生代深变质岩系;花岗岩类广泛分布,时代以早泥盆世为主,主要为片麻状黑云母二长花岗岩、片麻状黑云母花岗岩、黑云母花岗岩、二云母花岗岩等(邹天人和李庆昌,2006)。南阿尔泰主要由泥盆纪火山-沉积岩系组成。花岗岩类以早泥盆世为主;其次是晚石炭世、二叠纪;少数岩体形成于奥陶纪(如切木切克岩体,462Ma,Wangetal., 2006;阿巴宫岩体,462.5Ma,刘锋等,2008)。

可可托海矿区处于西伯利亚板块阿尔泰陆缘活动带北阿尔泰中部的喀纳斯-可可托海古生代岩浆弧内。区内地层变质较深,主要为震旦纪-早古生代的片麻岩、片岩等。花岗岩、伟晶岩脉分布广泛,还分布有少量早泥盆世的变质基性岩体。伟晶岩脉主要产在变质辉长岩、震旦系-下古生界的片麻岩及片岩和泥盆纪花岗岩中 (图1c)。

3 花岗岩岩相特征

本次研究的花岗岩靠近可可托海3号伟晶岩脉矿坑,位于偏东侧约100m左右。野外露头及标本上可见少量斜长石斑晶粒度达几厘米,似斑状结构,斑晶为长石,含量5%左右;岩石具弱片麻状构造,岩相特征与矿区北部的阿拉尔似斑状黑云母花岗岩相似。(图2a)。岩性为变质中粒斑状黑云母二长花岗岩,变余似斑状结构。基质矿物粒度一般2~5mm,主要由斜长石(35%)、微斜长石(25%)、石英(30%)和黑云母(10%)组成,少量白云母(1%)(图2b)。斜长石呈半自形板状,杂乱分布,发育聚片双晶,局部高岭土化、白云母化,与微斜长石接触部位见净边、蠕虫等交代结构。微斜长石呈他形粒状,部分近半自形板状,杂乱分布,轻微高岭土化,格子双晶发育,交代斜长石,内含斜长石包体。石英呈它形粒状,填隙状分布,粒内波状消光。黑云母呈片状,断续条纹状定向分布,构成似片麻状构造,少量被白云母、绿泥石、绿帘石交代。

4 样品与测试分析

4.1 样品特征

花岗岩测年以及地球化学样品采自3号脉矿坑东侧的岩体边部一带(图1c),地理坐标为N47°12′35″、E89°49′18″。岩性为似斑状黑云母二长花岗岩。采集测年样品1件,选择5件无风化蚀变的新鲜样品用于岩石地球化学和Rb、Sr、Sm、Nd同位素的测试研究。

从测年样品中挑选出的锆石颗粒在透反射光下大多为浅黄褐色,透明度较好。多数晶形完好,部分颗粒破碎;大小在150~200μm,长宽比一般从2:1到3:1;自形程度好,呈板状和柱状。多数锆石表面光滑,少数表面粗糙、有裂纹。阴极发光图像显示(图3),部分锆石晶体具后期作用形成的变质增生和蜕晶化现象。样品中的锆石晶体内部均发育较好的振荡环带结构,是典型的岩浆成因锆石。

图3 锆石阴极发光图像及测年分析点Fig.3 CL images of zircon from granite and analytical spots

4.2 分析方法

锆石U-Pb测年由中国地质科学院矿产资源研究所LA-MC-ICP-MS实验室完成。5件花岗岩样品的主量、微量和稀土元素分析由国家地质实验测试中心完成,Rb-Sr、Sm-Nd同位素分析由中国地质科学院地质研究所同位素实验室完成。

锆石U-Pb测年所用仪器为Finnigan Neptune型MC-ICP-MS及与之配套的Newwave UP 213激光剥蚀系统。锆石定年激光剥蚀所用斑束直径为25μm,频率为10Hz,能量密度约为2.5J/cm2,以He为载气。均匀锆石颗粒207Pb/206Pb、206Pb/238Pb、207Pb/235U的测试精度(2σ)均为2%左右,对锆石标准的定年精度和准确度在1%(2σ)左右。LA-MC-ICP-MS激光剥蚀采样采用单点剥蚀的方式。锆石U-Pb定年以锆石GJ-1为外标,U、Th含量以锆石M127(U=923×10-6、Th=439×10-6、Th/U=0.475)(Nasdalaetal., 2008)为外标进行校正。样品的同位素比值和元素含量计算采用ICP-MS DataCal程序处理(Nasdalaetal., 2008),对204Pb含量异常高的分析点在计算时剔除,锆石年龄谐和图用Isoplot 3.0程序(Ludwig, 2003)获得,表达式中单个数据点的误差均为1σ,加权平均年龄具95%置信度,年龄值选用206Pb/238U年龄。详细测试过程可参见侯可军等(2009)。

主量元素测试采用X射线荧光法 (XRF) (国家标准GB/T 14506.28—1993监控)在X荧光光谱仪(2100)上完成。其中FeO采用容量滴定法(国家标准GB/T 14506.14—1993监控),CO2用电导法(国家标准GB 9835—1988监控),H2O+和烧失量(LOI)用重量法(国家标准GB/T 14506.2—1993和LY/T 1253—1999标准监控)分析。微量和稀土元素测试在等离子光谱仪(IRIS)(JY/T 015—1996标准监控)和等离子质谱仪(X-series)上完成(DZ/T 0223—2001标准监控)。Rb-Sr、Sm-Nd 分析采用同位素稀释法。其中,Rb-Sr、Sm-Nd含量和Sr同位素分析利用MAT262固体同位素质谱计完成,同位素质量分馏采用88Sr/86Sr=8.37521校正;Nd同位素分析所用仪器为Nu Plasam HR MC-ICP-MS、DSN-100膜去溶,同位素质量分馏采用146Nd/144Nd=0.7219校正。

4.3 分析结果

通过锆石的透射光、反射光和阴极发光图像研究,选择表面光滑、无裂纹、无包体、环带发育的锆石颗粒用于测试。对20颗锆石进行了20次分析(图4),年龄分析结果列于表1。本次锆石测年实验过程中测得Plesovice标样的结果为339.63±0.71Ma(n=8,2σ),其年龄推荐值为337.13±0.37Ma(2σ)(Slamaetal., 2008)。误差小于1%,说明本次测年分析是准确、可信的。锆石样品中U含量变化在11.2×10-6~279.7×10-6,总体含量偏低,大多数低于100×10-6或在其附近;Th含量变化在16.3×10-6~464.8×10-6,与U含量相关性较好,集中在100×10-6~200×10-6。Th/U比值变化在0.17~1.02,均大于0.1,表明锆石为岩浆成因(Claessonetal., 2000;Belousovaetal., 2002)。1个点(3号点)年龄数据谐和度偏低,低于95%,因此不参加年龄计算。其余19个测点集中成群分布于谐和线上及附近,206Pb/238U年龄集中于399.6~409.0Ma, 加权平均年龄为405.4±1.4Ma(MSDW=0.98)(图4),可以代表该花岗岩的形成时代。

图4 花岗岩体锆石U-Pb年龄图解Fig.4 Zircon U-Pb age of granite

从主、微量元素分析结果看(表2),本次研究的花岗岩体具有富硅(SiO2=70.69%~73.81%)、富铝(Al2O3=14.00%~15.74%)、全碱含量中等(K2O+Na2O=5.98%~8.00%)特征,钾相对钠总体略偏富集(K2O/Na2O=0.78~1.61);岩石中钙含量(CaO=2.05%~2.43%)中等,低铁(Fe2O3+FeO=1.68%~2.16%)、低镁(MgO=0.35%~0.52%)、低钛(TiO2=0.18%~0.23%)以及低磷(P2O5≤0.07%)。在硅碱图解上(图5a),SiO2和K2O显示较好的负相关性,总体表现为钙碱性向高钾钙碱性过渡的特征。铝饱和指数较高(A/CNK=1.09~1.12),属于强过铝质花岗岩(A/CNK≥1.1),在A/CNK-A/NK图解(图5b)中位于过铝质区域。

岩石中高场强元素(HFSE)总体含量较高,Th变化于11.9×10-6~17.1×10-6,U在0.98×10-6~1.64×10-6之间,Zr在85×10-6~128×10-6之间,Hf在2.63×10-6~4.06×10-6之间变化;Y(34.7×10-6~48.9×10-6)含量也较高。Nb(7.05×10-6~9.24×10-6)、Ta(0.53×10-6~2.65×10-6)含量相对偏低,Nb/Ta比值变化较大(3.49~13.30,仅一个比值为3.49,其余在10~13之间)。大离子亲石元素(LILE)Rb(139×10-6~197×10-6)、Sr(112×10-6~153×10-6)等与地壳丰度相当。原始地幔标准化蛛网图(图6a)显示,各样品微量元素分布模式一致,呈现Th、K、Pb、Nd、Zr、Hf的相对正异常,Ti、P、Sr、Nb、Ta和Ba相对负异常,尤其Ti和P较低,接近原始地幔值。

岩石稀土总量较高,变化不大,ΣREE介于122×10-6~180×10-6,轻稀土相对富集(LREE/HREE=5.31~6.18,(La/Yb)N=4.0~5.48),而且分馏较明显((La/Sm)N=2.55~2.87), 重稀土仅具轻微分馏((Gd/Yb)N=1.06~1.33)。

表2花岗岩主量(wt%)、微量稀土(×10-6)元素组成

Table 2 Major (wt%) and trace (×10-6) elements data for granite

样品号KKTH10-117KKTH10-118KKTH10-119KKTH10-120KKTH10-121样品号KKTH10-117KKTH10-118KKTH10-119KKTH10-120KKTH10-121SiO273.4572.9670.6972.3073.81Al2O314.2214.2415.7414.9614.00CaO2.052.332.132.212.43Fe2O30.861.350.911.031.23FeO0.880.810.770.830.92K2O3.263.134.943.912.62Na2O3.293.113.063.063.36MgO0.370.520.350.420.49MnO0.060.050.040.050.05P2O50.040.050.050.070.06TiO20.180.230.180.190.21CO20.160.100.140.190.10H2O+0.480.620.340.440.36LOI0.630.640.530.800.60Total99.93100.1499.87100.46100.24A/NK1.591.671.511.611.67A/CNK1.121.121.101.121.09Na2O+K2O6.556.248.006.975.98Mg#0.280.310.280.300.30Rb147139181197149Ba4435201078536372Th12.614.911.91417.1U1.371.330.981.641.41Ta0.880.690.532.650.79Nb8.978.067.059.248.09Sr112143153140141Zr96.710385110128Hf3.183.432.633.614.06Li728280.867.683.1B13.476.735.724.3Be2.362.067.882.833.72Sc9.910.27.9210.510.5V20.8262227.227.2Cr10.5010.4010.2012.1013.60Co3.283.823.193.813.93Ni5.736.095.996.827.73Pb23.6022.8029.4027.1022.80Cs25.5014.6029.7012.8036.40Ga16.8017.0017.3019.1017.90Tl0.930.841.091.271.03Mo0.140.09<0.050.160.15La25.4031.6022.4024.5031.90Ce71.4068.9046.2063.0074.50Pr6.958.225.916.898.40Nd26.3032.1023.1027.1032.20Sm6.427.295.246.137.18Eu1.061.150.901.061.12Gd5.836.524.725.485.81Tb1.121.200.850.981.05Dy7.087.255.146.296.76Ho1.441.521.041.321.46Er4.584.583.134.194.57Tm0.660.640.420.550.61Yb4.564.172.933.854.26Lu0.650.60.430.540.62Y46.748.934.742.648ΣREE163.5175.7122.4151.9180.4LREE137.5149.3103.8128.7155.3HREE25.9226.4818.6623.225.14LREE/HREE5.315.645.565.556.18(La/Yb)N4.005.445.484.565.37δEu0.520.500.540.550.51

在球粒陨石标准化配分图解中(图6b),所有样品的曲线均表现出轻稀土弱富集、分馏较明显,重稀土平缓、分馏不明显的右倾型REE配分模式,且由于较明显的负铕异常(δEu=0.50~0.55)而呈现“V”型谷状。

样品Sr、Nd同位素组成列于表3。同位素计算采用的花岗岩年龄为本次测定的LA-MC-ICP-MS锆石U-Pb年龄405.4Ma。样品中87Rb/86Sr=3.323~4.867,87Sr/86Sr=0.72259~0.72810,变化不大;Sr初始值较低,4件样品变化于0.70155~0.70341,有1件样品低于石质陨石的初始值(0.69897),为不合理的低值,暗示其Rb-Sr同位素体系可能受到某些扰动,因此予以剔除。Rb/Sr=1.15~1.68;147Sm/144Nd=0.1343~0.1455,143Nd/144Nd=0.51235~0.51237,变化均不大。fSm/Nd介于-0.32~-0.26,落在-0.6~-0.2之间,在地壳Sm/Nd范围内;Sm/Nd比值变化于0.222~0.240,显示分异小、较均一的Sm/Nd同位素体系。两阶段模式年龄t2DM集中在1.35Ga左右,属于中元古代;εNd(t)均为负值,变化于-3.07~-2.16。

5 讨论

5.1 花岗岩年代学

本文研究的花岗岩出露地的野外岩相特征与矿区北部的三叠纪阿拉尔花岗岩体(LA-MC-ICP-MS锆石U-Pb年龄为211Ma,Liuetal., 2014)边部特征颇为相似,因此笔者曾一度认为它可能不属于位于3号脉东部的泥盆纪英云闪长岩-花岗闪长岩-黑云母二长花岗岩复式岩体(图1c),可能是和阿拉尔黑云母花岗岩同期的小岩株。但本次精确的锆石U-Pb测年结果表明,花岗岩形成时代为405.4±1.4Ma(MSDW=0.98),属于早泥盆世岩体。显然,它比阿拉尔花岗岩的侵入时期早得多,与3号伟晶岩脉也没有成因上的联系(3号伟晶岩脉形成起始于210Ma左右;刘锋等,2012b),应属于东部复式花岗岩基的一部分,只是岩相有差异。

表3近3号脉花岗岩Sr-Nd同位素组成

Table 3 Representative Sr-Nd isotopic compositions of granite

样品号KKTH10-117KKTH10-118KKTH10-119KKTH10-120KKTH10-121Rb(×10-6)140.8121.9174.6183.8139.5Sr(×10-6)91.85106.3129.3109.5110.287Rb/86Sr4.4453.3233.9134.8673.66687Sr/86Sr0.72810.7225920.724330.7258070.722715±2σ0.0000140.0000150.0000140.0000130.000014(87Sr/86Sr)i0.702440.703410.701740.697710.70155Sm(×10-6)5.2365.7784.7594.9825.835Nd(×10-6)21.77425.46721.2421.77726.289147Sm/144Nd0.14550.13730.13550.13840.1343143Nd/144Nd0.512350.512360.512370.512350.51235±2σ0.0000050.0000080.0000060.0000080.000005εNd(t)-3.07-2.41-2.16-2.56-2.43t2DM(Ga)1.401.351.331.361.35fSm/Nd-0.26-0.30-0.31-0.30-0.32

图6 花岗岩微量元素原始地幔标准化蛛网图(a)和稀土元素球粒陨石标准化图解(b)(标准化值据Sun and McDonough, 1989)Fig.6 Primitive mantle-normalized trace element spider diagrams (a) and chondrite-normalized REE patterns (b) of granite (normalization values after Sun and McDonough, 1989)

以往大量的年代学研究表明,阿尔泰造山带古生代岩浆侵入活动存在四个峰值:460Ma、408Ma、375Ma和265Ma(Wangetal., 2006;曾乔松等,2007),花岗岩类分布广泛,多数形成于400Ma左右。尤其是北阿尔泰中部的喀纳斯-可可托海古生代岩浆弧内以早泥盆世侵入活动为主要特征,如铁列克岩体(403Ma)(童英等,2005)、喀纳斯岩体(398Ma)、琼库尔岩体(399Ma)(童英等,2007)、可可托海变质辉长岩(409Ma)(Wangetal., 2006)等。本文研究的花岗岩体侵入时代以及空间产出与上述一致,说明该岩体同样形成于区内岩浆活动最为强烈时期。这为阿尔泰造山带晚古生代早期强烈的岩浆活动规律提供了又一年代学证据。

5.2 岩石成因

花岗岩主要有几种地质作用形成:地幔源岩浆的结晶分异,深变质的混合岩化作用以及地壳岩石的深熔作用等(路凤香和桑隆康,2002)。一般认为,与碰撞有关的强过铝质(SP)花岗岩的源区主要是变质沉积岩(如泥质岩、砂屑岩或杂砂岩),岩石圈加厚及幔源岩浆底侵是导致下地壳熔融及长英质花岗岩产生的重要原因(Sylvester, 1998; 李鹏春等,2005;Yangetal., 2007;杨富全等,2007)。本次研究的黑云母二长花岗岩的矿物成分及组合、富硅、略富钾(总体上K2O>Na2O),贫Fe、Mg、Ti、P以及强过铝质特征表明该花岗岩属于髙钾钙碱性强过铝质(SP)花岗岩(Chappel and White, 1992),和Lachlan及欧洲海西带中变质沉积岩熔融成因的SP花岗岩类相类似(Chappel and White, 1992;Sylvester,1998)。

图7 岩体CaO/(MgO+FeOT)-Al2O3/(MgO+FeOT)关系图(据Altherr et al., 2000)Fig.7 CaO/(MgO+FeOT) vs. Al2O3/(MgO+FeOT) diagram of the pluton (after Altherr et al., 2000)

研究表明,强过铝质花岗岩主要由富铝质的地壳岩石经过部分熔融作用形成(Green, 1995),它的Al2O3/TiO2比值大于100时指示部分熔融温度小于875℃,属于高压型,小于100时指示熔融温度大于875℃,属于高温型(Sylvester, 1998)。本次研究的花岗岩Al2O3/TiO2(62~87)比值均小于100,应属于高温型强过铝质花岗岩。另有研究表明,对于SiO2含量在67%~77%的强过铝质花岗岩,CaO/Na2O比值可以很好地指示源区物质成分,当比值>0.3时指示源区为砂岩、正变质岩,当比值<0.3时指示源区为泥岩(Sylvester, 1998)。由此推测本区黑云母二长花岗岩(CaO/Na2O比值均大于0.3)源区物质可能主要为砂岩或正变质岩。CaO/(MgO+FeOT)-Al2O3/(MgO+FeOT)图解也显示该花岗岩为变质杂砂岩源区的部分熔融产物(图7)。偏低的FeO+Fe2O3+MgO+TiO2含量(均小于3%)及低Mg#(0.28~0.31)表明岩浆可能经历了较高程度的分异演化。

源区物质成分不同,部分熔融产生的强过铝质花岗质熔体成分特征也不同(Altherr and Siebel, 2002)。如果由云母类脱水熔融形成,其熔体会富含Rb、Cs,且K2O/Na2O比值较高;如果由角闪石脱水熔融形成,就富含Na、Ca,且K2O/Na2O比值较低(赵永久等,2007)。本区的黑云母二长花岗岩Rb、Cs含量较高,具有髙钾低钠特征,暗示该花岗岩可能与富含云母的源区脱水熔融有关。同时,岩体中Ba相对于Th、Rb亏损明显,Nd两阶段模式年龄在1.33~1.40Ga,体现了成熟度较高的陆壳岩石特征(马昌前等,2004),源区可能属于一套中元古代物质。样品中87Sr/86Sr(0.72259~0.72810)、143Nd/144Nd(0.51235~0.512367)接近于陆源沉积物,εNd(t)的负值与中亚造山带中花岗岩具有高正εNd(t)值的特征不同,可能反映了阿尔泰前寒武纪基底或微陆块的物源特征(童英等,2007),而较低Sr初始值则可能指示有幔源组分加入。

本区黑云母二长花岗岩Nb/Ta比值与地壳平均值11(Taylor and McLennan, 1985)基本相当、明显小于地幔平均值17.8(McDonough and Sun, 1995);Zr/Hf比值变化小(30.0~32.3),非常接近于地壳相应值33(Taylor and McLennan, 1985),明显不同于地幔平均值37(McDonough and Sun, 1995),说明岩石主要以地壳组分的贡献为主。但Th/U(8.5~12.1,平均10.6)明显高于地壳平均值2.8(Taylor and McLennan, 1985),Rb/Th比值(8.7~15.2,平均11.8)略高于球粒陨石比值(约8),Zr (85×10-6~128×10-6,多数>100×10-6)高于普通S型花岗岩(Zr<100×10-6,温度800℃)(Watson and Harrison, 1983),与高Zr的Lachlan和欧洲海西褶皱带的SP花岗岩(高温>875℃)较为类似。Rb/Zr(1.2~2.1)>1,也类似于海西S型浅色花岗岩(Harris and Inger, 1992),说明可能有部分幔源组分的加入。另外,微量元素原始地幔标准化图解中Ba、Sr、Nb、Ta、Ti的亏损也暗示花岗岩浆主要不是由软流圈部分熔融直接产生(Foleyetal., 1992),而可能与地壳或地壳混染有关、或源区有富含Nb、Ta、Ti的残留矿物、或有板块俯冲作用引起的岩石圈富集地幔的参与(Dunganetal., 1986)。

综上所述,本次研究的黑云母二长花岗岩具有“S”型花岗岩特征,与来源于变质沉积岩部分熔融的“S”型长英质岩石类似;可能为中元古代富含云母的变质杂砂岩在高温条件下经过部分熔融形成,但受到较多幔源组分等因素的影响。

5.3 地球动力学意义

相对而言,针对阿尔泰造山带泥盆纪岩浆活动以及构造环境的研究最为广泛、深入,但认识上也是争议最多的,有陆缘裂谷(陈毓川等,1996;王京彬等,1998)、岛弧或弧后盆地(Windleyetal., 2002; Xuetal., 2003;Xiaoetal., 2004;陈汉林等,2006;单强等,2007)、陆缘弧(Wangetal.,2006;童英等,2007;丛峰等,2007;杨富全等,2008)、陆缘伸展(Yuanetal., 2007)等的不同认识。即使如此,他们大多数的共同之处在于都认同阿尔泰晚志留世-泥盆纪处于活动大陆边缘,岩浆活动与板块俯冲有关。研究也已证明,阿尔泰造山带大致从晚寒武纪开始发生俯冲、碰撞、增生,至早石炭世才基本奠定了阿尔泰造山带的构造格架(Windleyetal., 2002; Xiaoetal., 2004; Wangetal., 2006)。本次研究的黑云母二长花岗岩与岩石圈伸展体制下强烈壳幔相互作用导致的岩浆活动不同(Xieetal., 2008; 袁顺达等,2012),其时间上、空间上的特点均说明它形成于与板块俯冲有关的活动大陆边缘环境。

图8 花岗岩的Nb-Y图解(据Pearce et al., 1984)Fig.8 Nb-Y diagram of the granite pluton(after Pearce et al., 1984)

花岗岩的形成受构造环境的影响和控制,尤其稀土及微量元素特征明显受成岩的构造环境制约。不同构造环境中形成的花岗岩/酸性火山岩的微量元素地球化学特征存在明显的不同 (Forsteretal., 1997)。本区黑云母二长花岗岩的Yb<5×10-6,绝大多数样品中Ta<1×10-6,Ta/Yb比值总体在0.5之下,表现出了与俯冲作用有关的弧岩浆作用的特点(Condie, 1986)。Sr、Ti、Ba、P、Nb、Ta等明显的负异常和Th、U、La、Zr、Hf等的正异常则与造山带弧岩浆作用形成的钙碱性系列岩石特征相符(Wilson, 1989; Rollinson,1993; Sajonaetal., 1996)。岩石稀土配分型式表现出的LREE的相对弱富集,HREE比较平坦以及Eu的中等负异常,也与弧环境下形成的酸性岩类特征相似(王中刚等,1989)。在花岗岩微量元素Y-Nb构造判别图解上(图8),所有样品均落入火山弧+同碰撞花岗岩区域。

在碰撞造山带,虽然放射性衰变可提供部分热量,但如果没有外界热能的供给,地壳熔融产生大型“S”型花岗岩岩基可能性不大(Kokonyangietal., 2004)。前人研究表明,“S”型花岗岩可以是同碰撞造山阶段挤压环境下地壳加厚而发生部分熔融的产物。在汇聚构造活动期间(碰撞或俯冲),深熔作用使地壳深部岩石尤其是富水沉积单元脱水,含水流体又润滑其周围岩石,从而引发大范围的熔融作用形成岩浆,后经岩浆的结晶分离作用产生S型花岗岩(肖庆辉,2002)。对于阿尔泰造山带而言,早泥盆世时期正处于俯冲-碰撞高峰阶段(古亚洲洋的北向俯冲、碰撞(Wangetal., 2006)),岩浆活动强烈,地壳急剧加厚。本区黑云母二长花岗岩可能正是由于这一时期强烈的俯冲-碰撞导致的地壳加厚产生大量热能,引发了阿尔泰微古陆边缘内部的深熔作用而最终形成。

6 结论

(1)本文研究的黑云母二长花岗岩的年龄为405.4±1.4Ma(MSDW=0.98),属于早泥盆世岩体。这一年代学结果可以证明该花岗岩体与3号伟晶岩脉没有成因上的联系。

(2)黑云母二长花岗岩总体趋向于髙钾钙碱性,属于高温型强过铝质(SP)花岗岩。

(3)岩石微量、稀土元素特征以及较低的Sr初始值εNd(t)均为负值等同位素特征表明该花岗岩为中元古代基底变质沉积岩经过部分熔融形成,但有较多幔源物质的参与。

(4)黑云母二长花岗岩体是在阿尔泰造山带早泥盆世时期,由于板块俯冲、碰撞引发深熔作用,促使陆缘深部岩石脱水、熔融,后上升侵位而形成,属于陆缘弧花岗岩。

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