Petrogenesis of Jinniu rock mass in Chuzhou area: Melting of delaminated lower crust or mixing of crust and mantle?
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摘要:
滁州冶山地区研究程度较低,前人研究认为金牛岩体属于冶山岩体的边缘相,本次对金牛岩体开展独立研究。金牛侵入岩锆石U-Pb定年结果为(129±2)Ma,属于早白垩世早期。锆石原位Hf同位素分析显示,具有较均一的负εHf(t)值(-2.82~-6.52)和较古老的地壳模式年龄tDMC(1360~1600 Ma)。金牛岩体为碱性(σ:5.08~5.74)、准铝质(A/CNK:0.803~0.844)岩石,具有较强的轻重稀土元素分异、无明显-弱负Eu异常、相对富集轻稀土元素、大离子亲石元素,明显亏损重稀土元素和高强场元素的特点,综合对比冶山岩体,认为金牛岩体与冶山岩体同期不同源。结合区域构造演化特征及岩石地球化学、Hf同位素特征,金牛岩体很可能为来源于富集岩石圈地幔的富水底侵基性岩浆与古老下地壳部分熔融形成的岩浆混合的产物,其源动力与太平洋板块的俯冲有关。
Abstract:The research on Lower Yangtze block in Yeshan area of Chuzhou is very insufficient. Previous researchers held that Jinniu rock mass belongs to marginal facies of Yeshan pluton. In this paper, the authors studied Jinniu pluton. Zircon U-Pb dating indicates that The Jinniu pluton of Yeshan area of Lower Yangtze block was formed at 129±2 Ma, suggesting a product of Early Cretaceous. Zircon Hf isotopic composition has relatively uniform negative εHf(t) values(-2.82——6.52) and old Hf isotopic crustal model ages (1360-1600 Ma). The Jinniu pluton is alkaline(σ:5.08-5.74)), metaluminous rock body(A/CNK:0.803-0.844), which is characterized by relatively strong differentiation between light and heavy rare earth elements, indistinct negative Eu anomalies, enrichment of LREE and LILE, and depletion of HREE and HFSE. Comprehensive comparative study of the Yeshan rock mas shows that the Jinniu rock mass and Yeshan rock mass belong to two different sources of the same period. Regional tectonic evolution characteristics and geochemistry of rocks and Hf isotope characteristics indicate that the source of the Jinniu rock mass seems to have been a mixed product of underplating water-rich basic magma from enriched lithospheric mantle and partially melted ancient lower crust due to the subduction of Paleo-Pacific Plate.
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Keywords:
- Chuzhou district /
- Jinniu rock mass /
- zircon U-Pb dating /
- zircon Hf isotope /
- crust-mantle mixing
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1. 引言
下扬子滁州地区位于秦岭—大别造山带以东,江南造山带以北,紧邻郯庐断裂带,受华北板块、扬子板块、秦岭微板块相互控制。区内位于特提斯和古太平洋构造域的结合部位,经历了复杂的地质构造演化(王鸿桢等, 1990;Yin et al.1993;Zhang et al. 2004;叶舟等,2006;梅廉夫等,2008;王凯等,2015)。晚二叠世扬子板块向北俯冲由海相沉积向陆相沉积转换,三叠纪—早侏罗世早期以扬子陆块与华北地块之间的拼合和碰撞造山为主(Li et al.1993;张国伟等,2001;汤加富等,2003;张复新等,2004;Xu et al.2006;谢士稳等,2016)。区内出露大量燕山期岩浆岩。前人工作主要集中于宁镇、宁芜、铜陵、庐枞、安庆、九瑞、鄂东等7个大型矿集区(常印佛等,1991;Li et al.2008;周涛发等,2008;Sun et al., 2010;周涛发等,2011;段超等,2011;马立成等,2011;杜建国等,2011;周涛发等,2012;范裕等,2014;薛怀民等,2015),而冶山—天长地区为中小型铁铜矿集区,研究工作较少,存在少量盲区。其中冶山铁矿作为江苏典型的矽卡岩型铁矿山,开采历史悠久,相关报道却极少(周鑫龙等,2007;资锋等,2011;孙浅,2013)。冶山铁矿北矿区、东矿区成矿岩体为冶山岩体,冶山铁矿铁石岗矿区成矿岩体为金牛岩体,前人一直认为金牛岩体是冶山岩体的边缘相。本次工作发现金牛岩体与冶山岩体岩性差别较大,航磁异常图上形态分布像独立的岩体,两者的岩浆来源是否一样,为了验证想法,选择金牛岩体、冶山岩体作为研究对象,坑道采集新鲜样品,进行岩石地球化学、锆石U-Pb定年和锆石Hf同位素分析,讨论冶山—天长地区复杂的壳幔相互作用。
2. 地质概况
研究区位于南京市六合区北部苏皖交界处,大地构造位置上处于下扬子地块北东部,郯庐断裂带以东,江浦—天长隆起带中段之六合—冶山隆起带东北端(图 1)。江浦—六合隐伏断裂(⑤)、天长—仪征隐伏断裂(㉑)、天长—龙河集隐伏断裂(㉒)是重要的区域性控岩控矿构造。
区内揭露的地层主要有:黄墟组(Z1h):出露于冶山南部,岩性以灰岩、白云质灰岩为主,与灯影组断裂接触。灯影组(Z2dn):主要岩性以白云岩为主,夹硅质、泥质条带,系北矿段、东矿段下部矿体围岩。铁石岗矿段地层亦属灯影组,以小捕虏体存在于辉石二长岩的软弱带中。荷塘组(∈1ht):岩性以硅质页岩、炭质页岩、砂质页岩为主,夹煤层,含黄铁矿及磷质结核。幕府山组(∈1m):主要岩性以白云岩为主,夹硅化角岩(原岩可能为泥岩、炭质泥岩),局部为硅化灰岩、蚀变白云岩。底部为硅化(质)条带白云岩,其下为震旦系白云岩。西横山组(J3x)灰黄、紫红色长石英砂岩,含砾岩,夹薄层粉砂层,底部为杂砾岩,偶见火山岩砾石。龙王山组(K1l)安山岩、安山质角砾熔岩、黑云母石英粗安岩夹安山质凝灰岩及粉砂质泥岩。葛村组(K1g)紫红、灰绿色安山质沉角砾凝灰岩、沉凝灰岩,偶夹泥质粉砂岩。浦口组(K2p)细砂岩、粉砂岩、粉砂质泥岩和泥质粉砂岩;下部泥质粉砂岩、钙质粉砂岩、层状角砾岩。赤山组(K2c2))细粒岩屑石英砂岩、粉砂岩、钙质砂岩、顶部夹白色砂岩及泥岩。
区内与成矿有关的侵入岩形成于燕山晚期,北部为冶山岩体,分布于冶山及其以北;南部为金牛岩体,分布于金牛山—横山一带(图 1)。冶山岩体和金牛岩体是区内内生金属矿产的主要成矿母岩,为区内铁、铜、多金属矿的形成提供了矿质来源及主要成矿流体。岩体与由震旦系、寒武系碳酸盐岩的接触带,是区内矽卡岩型铁矿的有利成矿部位。冶山铁矿的北、东矿段位于冶山岩体与围岩接触带,铁石岗矿段位于金牛岩体与围岩接触带。但冶山地区第四系覆盖严重,水系发育,露头出露较少,无法准确观察到冶山岩体与金牛岩体的野外接触关系、岩相分带情况。
3. 样品描述
本次研究针对金牛岩体于不同标高坑道采集分析了4个样品(YST-1、YST-8、YST-9、YST-16),样品新鲜,具体位置见图 1,对其中YST-1样品进行了锆石U-Pb定年及锆石原位Hf同位素分析。金牛岩体岩性主要为辉石二长岩,灰白微带肉红色,二长结构,块状构造。矿物组成:中长石含量33%~35%,钾长石30%~35%,普通辉石15%,黑云母7%~8%。副矿物:磁铁矿、钛铁矿、磷灰石、榍石等。手标本及镜下特征见图 2。
图 2 金牛岩体、冶山岩体手标本和显微照片a—冶山岩体花岗闪长岩;b—花岗闪长岩显微照片(正交偏光);c—花岗闪长岩显微照片(正交偏光);d—金牛岩体辉石二长岩;e—辉石二长岩显微照片(正交偏光);f—辉石二长岩显微照片(正交偏光).矿物缩写:Qtz—石英;Pl—斜长石;Kf—钾长石;Fs—长石;Bt—黑云母;Amp—角闪石;Chl—绿泥石Figure 2. Representative samples and microscope photos of Jinniu rock mass, Yeshan rock massa-Granodiorite of Yeshan rock mass; b-Microscope photos of granodiorite (crossed nicols); c-Microscope photos of granodiorite(crossed nicols); d-Pyroxene-monzonite of Jinniu rock mass; e-Microscope photos of pyroxene-monzonite(crossed nicols); f-Microscope photos of pyroxenemonzonite (crossed nicols).Abbreviations: Qtz -Quartz; Pl-Plagioclase; Kf-K-feldspar; Fs-Feldspar; Bt-Biotite; Amp-Amphibole; Chl-Chlorite为对比研究,在冶山岩体采集了4个样品,具体采样位置见图 1。其中冶山铁矿坑道内采集2个样品(YSB-1、YSB-8),关塘铁矿坑道内采集1个样品(GT-1),和尚田采石场采集1个样品(HST-1)。对其中YSB-1样品进行锆石U-Pb定年及锆石原位Hf同位素分析。冶山岩体岩性主要为花岗闪长岩,灰白—浅肉红色,全晶质半自形不等粒结构、块状构造。矿物组成:更—中长石42%~50%,钾长石15%~25%,石英15%~20%,角闪石4%~9%,黑云母1%~5%。副矿物:磁铁矿、磷灰石,少量锆石、榍石。(石英)二长岩:灰白色,二长结构,块状构造。石英5%~10%,斜长石60%~65%,钾长石10%~ 15%,暗色矿物15%~20%,暗色矿物为黑云母和角闪石,在部分角闪石中有辉石核。手标本及镜下特征见图 2。
4. 分析测试方法
选择新鲜的岩石挑选锆石,由河北省区域地质矿产调查研究所完成。然后在双目镜下挑选颗粒完整、透明度高、无裂隙、长宽比较大、环带清晰的锆石,置于环氧树脂中,进行抛光。制靶后进行反射光、透射光显微照相,以及阴极发光(CL)图像分析。在南京大学内生金属矿床成矿机制研究国家重点实验室完成锆石U-Pb定年, 测试仪器为带激光熔蚀装置的Agilent HP 7500 ICP-MS分析仪。样品同位素比值及元素含量计算采用GLITTER (Ver4.0, Mac-quarie University)程序, 普通Pb校正采用Andersen (2002)的方法, 校正后年龄计算及谐和图的绘制用Isoplot程序完成(Ludwig,2001)。在带有Merchantek/New Wave Research213 nm激光溶蚀探针的Nu Plasma MC-ICP-MS机上进行了锆石Lu-Hf同位素原位分析, 实验以He作为载气, 激光束斑直径为60 μm, 溶蚀时间为60 s, 溶蚀深度约为40 μm, 剥蚀频率为5 Hz, 实验采用MT作为外部标样, MT的176Hf/ 177Hf比值为0.282530±30。εHf (t)计算采用的176Lu的衰变常数为1.865×10−11 (Scherer et al., 2001), 球粒陨石176Hf/177Hf= 0.282772, 176Lu/177Hf=0.0332(Blichert-Toft et al., 1997)。亏损地幔Hf模式年龄(tDM1)采用176Hf/177Hf= 0.283251, 176Lu/ 177Hf=0.0384计算(Vervoort et al.1999), 二阶段Hf模式年龄(tDm2)采用平均大陆壳176Lu/177Hf=0.015计算(Griffin et al., 2002)。
全岩主量元素分析在国土资源部南京矿产资源监督检测中心完成,采用荷兰帕纳科公司(PANalytical B.V.)Axios, Magix波长色散XRF测定,分析项目13种;全岩微量元素(含稀土元素)采用WSP-1型二米平面光棚摄谱仪、Axios Advanced型X射线荧光光谱仪,检测限优于0.5×10-9,相对标准偏差优于5 %。分析项目43种。
5. 分析结果
5.1 锆石U-Pb年龄
金牛岩体辉石二长岩(YST-1)挑选出来的锆石,透明度较好,呈淡黄色、淡褐色,少量无色,多为半自形颗粒,边部发生磨圆或溶蚀,宽度15~120 μm,长度40~150 μm,振荡环带不明显,部分无环带、弱分带(图 3)。YST-1辉石二长岩锆石Th/U比值绝大多数明显大于0.5接近1。属于典型的岩浆岩锆石特征(Möller et al., 2003;吴元保等,2004)。共选定21颗锆石进行测试分析(表 1),测点YST-1-07可能存在Pb丢失,谐和度较低,未参加计算谐和年龄。剩余20个测点锆石的206Pb/238U表面年龄介于(113±2) Ma~(143±2)Ma,其中14个测点206Pb/ 238U年龄集中在(123±2) Ma~(135±2)Ma,年龄范围比较集中,且数据点在谐和图中集中分布在一致曲线上及附近。测点206Pb/238U加权平均年龄为(129± 2)Ma(MSWD=2.4) (图 3a),代表了辉石二长岩的结晶年龄;冶山岩体锆石206Pb/238U加权平均年龄为(128±2)Ma(MSWD=2.3) (图 3b)。可以看出冶山岩体和金牛岩体属于燕山晚期早白垩世岩浆活动的产物。
表 1 冶山岩体(YSB-1)、金牛岩体(YST-1)锆石U-Pb定年结果Table 1. Zircon U-Pb dating results of Jinniu rock mass, Yeshan rock mass5.2 锆石Lu-Hf同位素
锆石Hf同位素分析结果显示,冶山铁矿金牛岩体辉石二长岩(YST-1) Hf同位素组成相对比较均一(表 2,图 4)。金牛岩体辉石二长岩(YST-1)锆石的176Hf/177Hf变化为0.282505~0.282618,对应的εHf (t)值范围是-2.82~-6.52, 平均值为-4.61,地壳模式年龄tDMC为1360~1600 Ma。指示金牛岩体岩浆主要起源于富集地幔,在岩浆演化过程中受到壳源物质的混染。而冶山岩体花岗闪长岩(YSB-1)锆石的176Hf/ 177Hf变化为0.282172~0.282252,对应的εHf (t)值范围是-15.76~-18.54,平均值为-17.23,地壳模式年龄tDMC为2170 ~2340 Ma,指示冶山岩体岩浆演化过程中混入了更多古老下地壳的物质,混染程度更高。说明冶山岩体与金牛岩体岩浆源区有差异。
表 2 冶山岩体(YSB-1)、金牛岩体(YST-1)锆石Hf同位素组成Table 2. Zircon Hf isotopic data of Jinniu rock mass, Yeshan rock mass5.3 地球化学
5.3.1 主量元素特征
金牛岩体辉石二长岩SiO2含量介于57.24%~ 57.72%,平均57.54%;Al2O3含量为16.66%~17.23%,平均17.02%;MgO含量介于3.18% ~3.54%,平均3.34%;CaO含量4.26%~4.53%,平均4.40%;Na2O+ K2O含量8.73%~9.38%,平均9.15%;里特曼指数(σ)介于5.08~5.74均在3~9,为碱性岩;Na2O含量略高于K2O,Na2O/K2O介于1.00~1.09,平均1.04,显示该岩体相对富钠(表 3)。在TAS图解中,金牛岩体辉石二长岩样品落入二长岩区域内,属于碱性系列;冶山岩体花岗闪长岩样品落入花岗闪长岩区域内,属于亚碱性系列(图 5);铝饱和指数(ASI)A/CNK为0.803~0.844,在A/NK-A/CNK图中显示为准铝质特点(图 6)。在SiO2-K2O图解中,落入钾玄质系列(图 7),而冶山岩体全部落入高钾钙碱性系列区域。
表 3 金牛岩体、冶山岩体全岩主量元素(%)及微量元素(10-6)分析结果Table 3. Major(%) and trace element (10-6) concentrations of Jinniu rock mass, Yeshan rock mass5.3.2 稀土元素特征
金牛岩体辉石二长岩∑REE为241.10×10-6~ 263.02×10-6,平均值为249.43×10-6,表现为较高的稀土总量;明显高于冶山岩体的稀土总量。LREE/ HREE为11.88~12.79,平均为12.17,(La/Yb)N为18.87~20.30,平均为19.26,表现为较强的轻重稀土分异;δEu变化于0.91~1.00,无明显-弱负Eu异常,说明岩石形成过程中没有明显的斜长石分离结晶;δCe为1.02(表 3),而一般认为Ce亏损是古俯冲带及古洋壳残骸标志之一,说明岩浆来源于洋壳俯冲熔融的可能性较小。
REE配分曲线(图 8)均为右倾,表明轻、重稀土具有相似的分异特征((La/Sm)N=3.64~4.25,(Gd/Yb)N=2.97~3.23)。
5.3.3 微量元素特征
金牛岩体辉石二长岩微量元素原始地幔标准化蛛网图(图 9)总体表现为陡右倾形式,相对富集Rb、Ba、Th、U、K、Sr等大离子亲石元素;明显亏损Ta、Nb、Ti等高强场元素。Sr在斜长石、磷灰石中分配系数最大,Ba在黑云母、钾长石中分配系数最大(干国樑,1993),因此可以推测,Sr、Ba的显著富集说明源区斜长石、磷灰石和黑云母在部分熔融过程早期进入溶体中;Ti则主要向角闪石、黑云母中富集(干国樑,1993),Ti的亏损说明角闪石、黑云母更多发生了大量结晶分离。在Sr/Y-Y图解和(La/Yb)N-YbN判别图解中,冶山岩体样品落入埃达克岩区内,而金牛岩体落入经典岛弧岩石区域(图 10)。
6. 讨论
6.1 金牛岩体与冶山岩体关系的厘定
前人一直把冶山岩体与金牛岩体看作一个整体进行研究分析,例如:江苏省及上海市区域地质志中认为冶山岩体主要组成岩石为石英闪长岩,边部出现石英闪长斑岩-闪长玢岩,为同一岩体的不同岩相(江苏省地质矿产局,1984)。1:5万河桥幅等区域地质调查报告❶显示六合冶山石英闪长岩岩体,金牛山和金牛乡闪长玢岩岩体和安徽天长横山石英闪长岩岩体实为一个大岩体,称冶山岩体。1: 25万南京市幅(I50C004004)区域地质调查报告❷同样指示冶山岩体主要岩性为石英闪长岩和闪长玢岩,局部边缘为花岗闪长岩、石英二长岩等。本次工作基于矿物学、岩石学、岩石地球化学、锆石LuHf同位素等资料分析研究,认为金牛岩体与冶山岩体为“同期不同源”岩体,理由如下:
金牛岩体岩性主要为辉石二长岩,冶山岩体岩性主要为花岗闪长岩、(石英)二长岩。其中花岗闪长岩的磁化率约为900(K×10-6 4πSI)、(石英)二长岩的磁化率约为350(K×10-6 4πSI),辉石二长岩的磁化率约为2500 (K×10-6 4πSI),两个岩体在矿物成分、物性上存在明显区别。
金牛岩体为碱性、准铝质岩石,在SiO-K2O图解中,落入钾玄质系列区域,而冶山岩体为钙碱性、准铝质岩石,在SiO-K2O图解中,落入高钾钙碱性系列区域(图 7)。金牛岩体的稀土总量明显高于冶山岩体(图 8)。金牛岩体在Sr/Y-Y图解和(La/Yb)N-YbN判别图解中,落入经典岛弧岩石区域,冶山岩体样品落入埃达克岩区内(图 10)。
金牛岩体结晶年龄为(129±2) Ma,冶山岩体结晶年龄为(128±2) Ma。表明冶山岩体和金牛岩体形成时代基本上一致。
金牛岩体辉石二长岩锆石εHf(t)值范围是-2.82~-6.52, 平均值为-4.61,地壳模式年龄tDMC为1360 ~1600 Ma,而冶山岩体εHf(t)值范围是-15.76~-18.54,平均值为-17.23,地壳模式年龄tDMC为2170 ~2340 Ma,说明冶山岩体与金牛岩体岩浆源区有差异。
在1:5万航磁推断图中(图 11),冶山岩体与金牛岩体具有明显不一样的产状特征。冶山岩体呈似椭圆状分布,航磁等值线较平缓;金牛岩体明显受北东向断裂控制,呈北东向展布,航磁等值线较密集、梯度较陡。
6.2 岩浆源区与演化
金牛岩体辉石二长岩中锆石U-Pb年龄为129± 2) Ma,与宁芜地区侵入岩形成时代125~131 Ma(胡劲平等,2010;侯可军等,2010;范裕等,2010;段超等,2011;袁峰等,2011;王丽娟等,2014;王丽娟等,2015)、溧水地区侵入岩形成时代125~136 Ma相一致(王丽娟等, 2014;王丽娟等,2014;张少琴等,2015);锆石锆石εHf(t)值范围是-2.82~-6.52, 相对均一,指示岩浆演化过程中没有明显的岩浆混合或围岩混染,与宁芜地区侵入岩εHf(t)值-2~-5(胡劲平等,2010;侯可军等,2010;袁峰等,2011;王丽娟等,2014;杨颍鹤等,2015)、溧水地区侵入岩εHf(t)值-5~-10相似(王丽娟等,2014;王丽娟等,2014;张少琴等,2015)。前人研究认为宁芜地区、溧水地区的火山岩-侵入岩的岩浆源区为富集岩石圈地幔,并混入少量地壳物质(王元龙等,2001;Wang et al.2006;侯可军等,2010)。金牛岩体锆石阴极发光图像没有发现明显的继承锆石核,指示着岩浆在上升过程中没有经历显著的中、上地壳的混染,同时说明岩浆形成温度较高,导致源区继承锆石完全溶解。同时金牛岩体表现为轻重稀土分异强烈、富集Rb、Ba、Th、U、K、Sr等大离子亲石元素和轻稀土元素、亏损Ta、Nb、Ti等高强场元素等特征,与来自富集岩石圈地幔的岩浆具有相似的地球化学特征。
富集地幔源区一般是地幔交代作用形成,本区岩石具有富集K、Zr-Hf亏损Nb-Ta、Ti特征, 同时岩浆岩锆石εHf(t)值为负值,说明交代流体/溶体很可能起源于陆壳组分,而不是来源更深的地幔流体或洋壳脱水流体或溶体。陆源物质很可能是扬子板块向北深俯冲带入到地幔深部的。
金牛岩体辉石二长岩中锆石Lu-Hf同位素地壳模式年龄tDMC为1360 ~1600 Ma,与扬子克拉通基底岩石tDMC值统计的结果:主体形成于1.3~2.4 Ga相一致(Chen et al., 1998;张本仁等,2002),表明金牛岩体的岩浆源区应具有扬子地壳的属性。这些事实表明金牛岩体的源区可能来源于一个陆壳流体/溶体交代过的富集地幔。
主量元素Harker图解上元素的变化规律较明显,说明岩浆演化过程中没有受到上地壳物质混染影响。其中金牛岩体和冶山岩体MgO、Fe2O3T、CaO、TiO2、及Co与SiO2含量呈明显的负相关(图 12,图 13),说明岩浆演化过程中可能发生了辉石、角闪石等镁铁质矿物的分离结晶;Dy/Yb值随SiO2含量的增加呈减小的趋势也显示出角闪石发生了分离结晶(图 13);Al2O3随着演化(Mg#降低)而升高、CaO随着演化(Mg#降低)而降低、稀土元素配分图显示δEu无明显-弱负Eu异常(图 13,图 8),说明岩石形成过程中没有明显的斜长石分离结晶,CaO的降低可能与辉石、角闪石、磷灰石分离结晶有关;Sr的含量随着SiO2增高而基本不变(图 13),也表明岩体岩浆演化过程中斜长石分离结晶不明显;岩石的稀土总量随SiO2升高而表现出下降趋势(图 13),P2O5与SiO2含量呈明显的负相关(图 12),很可能与磷灰石等富含稀土矿物分离结晶有关,这与显微镜下看到磷灰石副矿物相一致。
Richard et al.(2001)、Annen et al.(2005)研究认为在岩浆演化过程中,角闪石发生结晶分离、斜长石分离结晶不明显,岩浆需要较高的水含量。说明金牛岩体是富水的基性岩浆演化形成。
6.3 地球动力学背景
冶山地区位于扬子地块的东北缘,其西北侧比邻华北地块东南缘和郯庐断裂带,西南靠近长江断裂,岩体的侵位严格地受郯庐断裂、长江断裂以及其他基底深断裂的控制,特殊的空间分布格局暗示着岩石的成因与郯庐、长江等深大断裂活动可能密切相关。
冶山地区属于长江中下游成矿带的东部,长江中下游成矿带又是中国东部燕山期成矿带的重要组成部分,受整个中国东部的构造背景控制,有其独特的演化背景,白垩纪经历了由挤压环境向伸展环境的重大转换(宋传中等,2011)。而研究区西北侧的华北地块在早白垩世发生了强烈的岩石圈减薄作用,这期地质事件在时间上与长江中下游的岩浆活动作用基本一致,它们之间很可能存在成因联系。目前流行的岩石圈减薄的机制主要为两种:岩石圈拆沉和热-机械侵蚀两种(常印佛等,1991;Li X H et al.2010;刘海泉等,2010;薛怀民等,2010;周涛发等,2011;闫峻等,2012;),前者强调岩石圈重物质的“突发性”下沉;后者则强调软流圈轻物质“逐渐地”上涌。无论中生代岩石圈减薄还是上述深大断裂的活动都与太平洋板块向亚洲大陆俯冲有关。太平洋板块向西的俯冲至少在中晚侏罗就已开始影响中国东部(Zhou et al., 2000;Zhou et al., 2006;孙卫东等,2008)。中国东部燕山期大规模岩浆活动与岩石圈减薄、壳幔相互作用等深部过程有关(吴福元等,1999;徐义刚,1999;陶奎元等,1999;吴福元等,2003;张旗等,2009),长江中下游地区晚中生代岩浆岩是强烈的壳幔相互作用的产物(Xu et al., 2002;Wang et al., 2006)。资锋等(2011)、刘盛遨(2011)认为冶山岩体是拆沉下地壳熔融产生的埃达克质岩浆在上升过程中与地幔橄榄岩发生反应的产物,属于路凤香等(2006)划分的大陆内部壳-幔作用3种类型中的第二类,下地壳拆沉进入弱化(weakening)了的岩石圈地幔发生的作用。
肖庆辉等(2006)认为中国东部中生代白垩纪(140~65 Ma)岩石圈进入全新的从挤压向伸展转变和巨大减薄阶段。周涛发等(2007)认为长江中下游成矿带的中生代成岩成矿作用发生于大陆边缘环境向陆内断块环境的转换期,大约131 Ma后为典型的伸展拉张背景。本文研究选取得的冶山岩体、金牛岩体年龄都接近130 Ma, 表明冶山地区岩浆活动处于区域构造演化的板内伸展阶段。同时在花岗岩R1-R2图解(图 14)中冶山岩体样品落入板块碰撞后隆起期花岗岩,在(Yb+Nb) -Rb图解(图 15)中冶山岩体和金牛岩体样品落入火山弧型花岗岩区域。
Sun et al. (2010)曾用“洋脊俯冲”来解释中国东部及长江中下游的岩浆活动和成矿作用。而大陆或造山带高钾钙碱性-钾玄岩系列岩石的成因往往被解释为与深部岩石圈的剪切作用有关(袁峰等,2011)。与此同时发生的郯庐断裂带大规模左行走滑作用也有可能是诱发深部岩石圈发生剪切的重要机制。在中生代,受太平洋板块俯冲作用的影响,郯庐断裂带发生了巨大的左行平移运动,并导致深部地幔的热扰动作用、软流圈上涌和地温梯度增高,从而诱发了郯庐断裂带两侧及其周缘地区发生了强烈的岩石圈减薄作用和广泛的地幔熔融事件,形成了沿断裂带分布的岩浆岩,并活化了成矿物质的运移,形成与火山岩-侵入岩有关的系列铁铜金矿床。更接近路凤香等(2006)划分的大陆内部壳-幔作用3种类型中的第一类,地幔来源的底侵溶体与下地壳作用。
综上本文认为冶山地区很可能经历了软流圈物质上涌烘烤岩石圈地幔,致使富集地幔部分熔融,富集地幔部分熔融形成的基性岩浆在壳幔边界发生底侵作用,造成古老下地壳物质部分熔融,金牛岩体为富水的基性岩浆与较少的壳源物质混合形成。
7. 结论
(1) 金牛侵入岩与冶山侵入岩为“同期不同源”岩体。
(2) 金牛岩体锆石U-Pb年龄为(129±2) Ma,属于早白垩世早期。
(3) 金牛岩体很可能为来源于富集岩石圈地幔的富水底侵基性岩浆与古老下地壳部分熔融混合形成的产物,其源动力与太平洋板块俯冲有关。
注释
❶张作训等. 1986.中华人民共和国1:5万河桥、涧溪、穆店、旧铺、竹镇、马集、施官、六合、新集、仁和、瓜埠镇、陈集、仪征县(北)幅区域地质调查报告(地质部分)[R].南京:江苏省地质矿产局第一地质大队.
❷张登明,冯金顺,刘志平, 等. 2003.中华人民共和国1:25万南京市幅(I50C004004)区域地质调查报告[R].南京:江苏省地质调查研究院.
致谢: 野外工作得到了南京钢铁集团冶山矿业有限公司王科宁、赵博工程师的大力支持和帮助,室内工作得到了江苏省地质调查研究院魏邦顺高级工程师、张少琴工程师和南京大学武兵老师的热心帮助,特别感谢审稿专家的宝贵意见。 -
图 2 金牛岩体、冶山岩体手标本和显微照片
a—冶山岩体花岗闪长岩;b—花岗闪长岩显微照片(正交偏光);c—花岗闪长岩显微照片(正交偏光);d—金牛岩体辉石二长岩;e—辉石二长岩显微照片(正交偏光);f—辉石二长岩显微照片(正交偏光).矿物缩写:Qtz—石英;Pl—斜长石;Kf—钾长石;Fs—长石;Bt—黑云母;Amp—角闪石;Chl—绿泥石
Figure 2. Representative samples and microscope photos of Jinniu rock mass, Yeshan rock mass
a-Granodiorite of Yeshan rock mass; b-Microscope photos of granodiorite (crossed nicols); c-Microscope photos of granodiorite(crossed nicols); d-Pyroxene-monzonite of Jinniu rock mass; e-Microscope photos of pyroxene-monzonite(crossed nicols); f-Microscope photos of pyroxenemonzonite (crossed nicols).Abbreviations: Qtz -Quartz; Pl-Plagioclase; Kf-K-feldspar; Fs-Feldspar; Bt-Biotite; Amp-Amphibole; Chl-Chlorite
表 1 冶山岩体(YSB-1)、金牛岩体(YST-1)锆石U-Pb定年结果
Table 1 Zircon U-Pb dating results of Jinniu rock mass, Yeshan rock mass
表 2 冶山岩体(YSB-1)、金牛岩体(YST-1)锆石Hf同位素组成
Table 2 Zircon Hf isotopic data of Jinniu rock mass, Yeshan rock mass
表 3 金牛岩体、冶山岩体全岩主量元素(%)及微量元素(10-6)分析结果
Table 3 Major(%) and trace element (10-6) concentrations of Jinniu rock mass, Yeshan rock mass
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