引用本文
刘永江, 刘宾强, 冯志强, 等. 大兴安岭中北段老道口闪长岩锆石U-Pb年龄、地球化学特征及构造意义[J]. 吉林大学学报(地球科学版), 2016, 46(2): 482-498
Liu Yongjiang, Liu Binqiang, Feng Zhiqiang, et al. SIMS Zircon U-Pb Age, Petrogeochemistry and Its Tectonic Implication of Laodaokou Diorite in the Mid-North Part of Great Xing'an Range[J]. Journal of Jilin University(Earth Science Edition), 2016, 46(2): 482-498.
大兴安岭中北段老道口闪长岩锆石U-Pb年龄、地球化学特征及构造意义
1. 吉林大学地球科学学院, 长春 130061;
2. 东北亚矿产资源评价国土资源部重点实验室, 长春 130061;
3. 黑龙江省区域调查研究所, 哈尔滨 150080
2. 东北亚矿产资源评价国土资源部重点实验室, 长春 130061;
3. 黑龙江省区域调查研究所, 哈尔滨 150080
摘要: 鄂伦春自治旗老道口闪长质岩体位于兴蒙造山带东段、大兴安岭中北段,原定义为老道口单元的老道口岩体主要由闪长岩、石英二长岩和闪长玢岩组成。锆石SIMS U-Pb定年测定闪长岩年龄为(126.09±0.95)Ma,属于早白垩世岩浆活动的产物,并非前人认为的形成于寒武纪。闪长岩的w(SiO2)为56.13%~57.91%,w(TiO2)为0.97%~0.99%,w(MgO)和w(TFe2O3)分别为2.00%~2.12%和6.73%~7.41%,Mg#值为36.00~38.00,w(Na2O)为4.29%~4.53%,w(K2O)为1.38%~1.59%,K2O/Na2O为0.31~0.37,w(Al2O3)为17.95%~18.36%,相对富钠高铝,稀土元素球粒陨石标准化曲线显示其具有富含轻稀土元素(LREE)、贫重稀土元素(HREE)以及Eu(0.85~0.87)弱负异常的特点。老道口闪长岩强不相容元素Th、U、K显著富集和高场强元素Nb、Ta明显亏损,其岩浆源区可能为俯冲流体交代的岩石圈地幔。闪长岩富集Ba、K、Rb、Th、U等大离子亲石元素,高场强元素Nb、Ta、Ti、P等明显亏损,指示了与俯冲作用相关的地球化学特征。结合老道口岩体地球化学特点和区域构造背景,认为该岩体很可能形成于蒙古-鄂霍茨克洋闭合造山后的岩石圈伸展构造环境。
关键词:
SIMS锆石U-Pb 测年
蒙古-鄂霍茨克缝合带
闪长岩
岩石圈地幔
老道口岩体
兴蒙造山带
SIMS Zircon U-Pb Age, Petrogeochemistry and Its Tectonic Implication of Laodaokou Diorite in the Mid-North Part of Great Xing'an Range
1. College of Earth Sciences, Jilin University, Changchun 130061, China;
2. Key Laboratory of Mineral Resources Evaluation in Northeast Asia, Ministry of Land and Resources of China, Changchun 130061, China;
3. Heilongjiang Province Institute of Regional Geology Survey, Harbin 150080, China
2. Key Laboratory of Mineral Resources Evaluation in Northeast Asia, Ministry of Land and Resources of China, Changchun 130061, China;
3. Heilongjiang Province Institute of Regional Geology Survey, Harbin 150080, China
Supported by National Key Fundamental Reasearch Development Programme “973”(2013CB429802); Geological Survey Projects of China Geological Survey(12120115001001-08)and the Open Fund Project of the Key Laboratory of Mineral Resources Evaluation in Northeast Asia, Ministry of Land and Resources of China
Abstract: Laodaokou unit is located in Oroqen Autonomous Banner, Inner Mongolia, the east of Xing'an Mongolian orogenic belt, northern Great Xing'an Range. The unit is mainly composed of diorite, adamellite, and dioritic porphyrite. SIMS U-Pb dating of zircon of the diorite provides the age of (126.09±0.95) Ma, indicating that the plution was formed in Early Cretaceous instead of Cambrian as thought before. The major element data show that the diorites contains 56.13%-57.91% of SiO2, 0.97%-0.99% of TiO2, 2.00%-2.12% of MgO, 6.73%-7.41% of TFe2O3, 36.00-38.00 of Mg#, 4.29%-4.53% of Na2O, 1.38%-1.59% of K2O, 17.95%-18.36% of Al2O3. The K2O/Na2O ratios range from 0.31 to 0.37. The diorites are rich in alumina and sodium relatively. The rare earth elements chondrite standardized curves show that they are rich in light REE and depleted of heavy REE with weak negative δEu (0.85-0.87). Laodaokou plution is rich in large ion lithophile element (LILE)(e.g., Ba、K、Rb、Th、U), but depleted of high field strength elements (HFSE) (e. g., Nb、Ta、Ti、and P). The geochemical signatures above imply a characteristic related to subduction, and this suggests that the magmatic source of Laodaokou diorites were from the lithospheric mantle, which was metasomatosed by subduction fluid. Combining with the geochemical characteristics of Laodaokou plution and its regional tectonic settings, we conclude that the plution might be formed under a lithospheric extension after the closure of Mongolia-Okhotsk Ocean.
Key words:
SIMS ziron U-Pb dating
Mongolia-Okhotsk suture zone
diorite
lithospheric mantle
Laodaokou diorites
Xing'an Mongolian orogenic belt
0 引言
兴蒙造山带是西伯利亚板块和华北板块之间中小块体群组成的大范围构造拼合带，显生宙以来经历了额尔古纳地块、兴安地块、松嫩地块、佳木斯地块、兴凯地块等的拼合[1, 2, 3, 4, 5]。古生代期间，兴蒙造山带主要受古亚洲洋构造域的影响；中生代，经历了蒙古鄂霍茨克构造体系和环太平洋构造体系的叠加与改造[5, 6, 7, 8, 9, 10]，具有复杂的构造活动和岩浆作用。大兴安岭地区位于兴蒙造山带东段，横跨于额尔古纳地块、兴安地块、松嫩地块之上，主体部分位于兴安地块和额尔古纳地块，以出露大面积中生代火山岩为特征。
近年来研究表明，大兴安岭地区晚中生代岩浆活动开始于晚侏罗世，早白垩世达到高峰，止于晚白垩世。关于岩浆岩形成的构造背景，尚存在较大争议，目前有地幔柱成因[5, 11]、蒙古鄂霍茨克洋俯冲成因[12, 13, 14]、太平洋板块俯冲成因[15, 16]等多种观点。然而，越来越多的学者把大兴安岭中生代岩浆岩的成因构造与蒙古鄂霍茨克海闭合，发生碰撞后伸展的环境相联系[13, 14, 17, 18, 19]。如李世超等[20]认为形成年龄为135 Ma的大兴安岭中段柴河地区玛尼吐组火山岩具有明显的减压-伸展的成因特征，时间和空间上[21]均与蒙古鄂霍茨克洋闭合造山后伸展有很好的对应，形成于蒙古鄂霍茨克闭合造山后的岩石圈伸展构造环境；武广等[22]认为大兴安岭北端洛古河东花岗岩形成年龄为(129.8±2.2)Ma，属后碰撞花岗岩，形成于蒙古鄂霍茨克海碰撞造山过程的后碰撞阶段；杨奇荻等[23]指出大兴安岭中南段甘珠尔庙地区晚中生代花岗岩((139~125)Ma)的形成背景与蒙古鄂霍茨克洋闭合碰撞后伸展有关；Ying等[24]从A型花岗岩、变质核杂岩和同沉积盆地的角度论证了大兴安岭中生代火山岩与蒙古鄂霍茨克造山带的重力坍塌形成的伸展构造有关。然而，多数研究都集中于大兴安岭北段、南段及额尔古纳地块上的满洲里、根河等地区，而对位于大兴安岭中北段的鄂伦春地区中生代火山岩的研究明显滞后，高精度年代学数据和元素地球化学资料很少。
本次研究区位于我国内蒙古东北地区的兴蒙造山带东段、大兴安岭中北段、蒙古鄂霍茨克造山带的东南侧(图 1a)，地理位置上处于承接南北的重要作用。鄂伦春老道口闪长岩体除了1∶20万阿里河幅赵海山，表尚虎，陈荣升，等.阿里河幅(M51(16))1∶20万区域地质调查报告.哈尔滨：黑龙江省地质矿产局，1994.中提到外，鲜有其他报道。本文对老道口岩体进行了详细的岩相学、SIMS U-Pb测年和地球化学研究，以期阐明其成因及构造约束，为进一步深刻理解大兴安岭地区中生代构造岩浆活动提供科学依据。
1 地质背景
大兴安岭地区鄂伦春自治旗老道口位于蒙古鄂霍茨克缝合-造山带的东南侧、大兴安岭中北段。大兴安岭以其鲜明的NE走向横跨在古亚洲洋构造域不同地质单元之上，其巨型火山岩带呈NNE向横亘于西伯利亚板块和华北板块及其缝合带上[21]。大兴安岭从晚侏罗世进入强烈的火山喷发阶段，继之是大规模的岩浆侵位，早白垩世时大兴安岭地区已经属于造山后环境[27, 28, 29, 30, 31, 32]。研究区位于大兴安岭中北部，夹持于新林喜桂图旗缝合带和贺根山嫩江黑河缝合带之间。大兴安岭北部地区晚中生代火山-岩浆活动强烈，广泛发育晚侏罗世早白垩世陆相中基性和中酸性火山岩，自下而上依次为上侏罗统塔木兰沟组，下白垩统吉祥峰组、上库力组和伊列克得组[33, 34]。这套火山岩的时代过去多被认为是晚侏罗世[35]，但目前的研究表明晚侏罗世火山岩仅分布在局部地区[36]，而大范围分布的火山岩的时代主要为早白垩世[7]。根据阿里河幅1∶20万地质图资料[25]，研究区主要出露的岩石单元包括泥盆纪粗粒二长花岗岩、中粒二长闪长岩，侏罗纪中细粒钾长花岗岩、中粒二长花岗岩和白垩纪花岗斑岩等(图 1)。
2 岩体地质及岩相学特征老道口岩体出露于老道口西北约1 km处，呈岩株产出，NE向展布，面积2.8 km2[37]。据野外观察发现，该岩体侵入泥盆纪阿里河单元中，在接触处有3 cm左右的冷凝边和后者的捕掳体，界线波状弯曲；同时，该岩体又侵入到邻区早白垩世花岗斑岩，且侵入关系明显。老道口岩体岩石类型主体为闪长岩、闪长玢岩，局部为石英二长岩，岩石颜色变化较大，总体呈灰绿色，局部呈灰黑、灰褐色，且结构不均匀。岩石片理发育，强烈变形，结构疏松，极易风化呈砂状。岩体相带不明显，各种岩石类型之间呈渐变过渡关系(图 2a)。
 |
| a、b(LDK-01-a).闪长岩野外露头及镜下； c、d(LDK-02).石英二长岩野外露头及镜下。Pl.斜长石；Q.石英；Hb.角闪石；Bt.黑云母；Kfs.钾长石。图 2 老道口闪长岩体野外照片及显微照片(正交偏光)Fig.2 Photograph of outcrops and photomicrogranphs of diorites in Laodaokou |
闪长岩(LDK-01-a)：主要矿物成分为斜长石(~60%)、角闪石(~25%)和黑云母(~15%)，全晶质结构，块状构造。斜长石半自形他形，一级灰白干涉色，二轴晶，聚片双晶、卡氏双晶发育，部分发生绢云母化蚀变。角闪石半自形他形粒状、板条状，单偏光镜下绿色，多色性明显，横切面对称消光，发育两组角闪石式解理，夹角56°(~124°)。黑云母自形半自形片状，具有显著的多色性和吸收性，一组极完全解理，正中突起，正延性，干涉色二级顶至三级顶，二轴晶负光性，光轴角小。另含有少量磷灰石、磁铁矿、榍石和锆石等副矿物(图 2a、b)。
石英二长岩(LDK-02)：似斑状结构，斑晶主要为斜长石(~40%)、碱性长石(~40%)和石英(~10%)，基质为细碎的石英和长石颗粒(~10%)，块状构造。斜长石自形半自形，板状、棱角状，聚片双晶发育，表面不干净，发生高岭土化蚀变。碱性长石半自形他形板状、短柱状，粒径较斜长石小，发生帘石化蚀变。石英颗粒较细碎，与破碎的长石颗粒共同构成基质，发育蠕虫结构(图 2 c、d)。
闪长玢岩(LDK-03)：斑状结构，斑晶主要为斜长石，基质为细碎的石英、长石和角闪石等，块状构造。斜长石(~50%)斑晶和基质中都有，其中，斑晶斜长石(~30%)为自形半自形板状，发育聚片双晶，发生强烈绢云母化和高岭土化。基质主要为石英(~25%)、长石(~20%)、角闪石(~25%)。基质排列杂乱无章，没有定向性。
3 SIMS锆石U-Pb年代学 3.1 样品采集及测试技术对闪长岩样品(LDK-01-a)进行年龄测定。其中，锆石的挑选工作在河北省廊坊区域地质调查研究所实验室利用标准重矿物分离技术分选完成。锆石的透射光、反射光和阴极发光(CL)图像的采集和SIMS U-Pb年龄测定均在中国科学院地质与地球物理研究所完成。用于U-Pb年龄测定的锆石样品颗粒和锆石标样Plésovice[38](或TEMORA[39])和Qinghu[40]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像分析，以检查锆石的内部结构和帮助选择适宜的测试点位。样品靶在真空下镀金以备分析。U、Th、Pb的测定在CAMECA IMS-1280二次离子质谱仪(SIMS)上进行，详细分析方法见文献[40]。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[41]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[39, 40, 41, 42, 43, 44]。
3.2 测试结果老道口闪长岩锆石为无色，呈自形-半自形长柱状，大小200~400 μm，长宽比为1∶1~5∶1(图 3a)，呈板条状结构，个别颗粒具扇形结构，发育典型岩浆振荡环带，较高的Th/U值(0.64~1.28)(表 1)，这些都反映了岩浆锆石的特点[45, 46]。个别颗粒因破碎而显得形态多样(图 3a)。LDK-01-a样品的SIMS锆石U-Pb年结果见图 3和表 1。年龄为(121.5±5.3)~(130.9±2.2)Ma。对20个颗粒进行加权平均年龄计算所得结果为(126.09±0.95)Ma，MSWD=0.54，所测20个点均分布在谐和线上或其附近(图 3b)，代表该岩体的形成时代，为早白垩世，并非前人认为的形成于寒武纪。
表 1 老道口闪长岩SIMS锆石U-Pb同位素分析结果
Table 1 SIMS zircon U-Pb data of Laodaokou diorite
| 测点号 | wB/10-6 | Th/ U | 同位素比值 | 年龄/Ma | |||||||
| U | Th | 207Pb/235U | 1σ | 206Pb/238U | 1σ | 207Pb/235U | 1σ | 206Pb/238U | 1σ | ||
| LDK-01-a01 | 66 | 53 | 0.81 | 0.132 75 | 6.62 | 0.019 6 | 1.98 | 126.6 | 7.9 | 125.0 | 2.5 |
| LDK-01-a02 | 72 | 58 | 0.81 | 0.133 27 | 5.74 | 0.019 5 | 1.56 | 127.0 | 6.9 | 124.3 | 1.9 |
| LDK-01-a03 | 298 | 290 | 0.97 | 0.131 59 | 3.22 | 0.019 6 | 1.69 | 125.5 | 3.8 | 125.0 | 2.1 |
| LDK-01-a04 | 163 | 175 | 1.07 | 0.138 21 | 3.92 | 0.019 8 | 1.51 | 131.4 | 4.9 | 126.6 | 1.9 |
| LDK-01-a05 | 118 | 130 | 1.10 | 0.144 19 | 4.48 | 0.020 5 | 1.68 | 136.8 | 5.7 | 130.9 | 2.2 |
| LDK-01-a06 | 280 | 262 | 0.93 | 0.134 21 | 3.56 | 0.019 6 | 1.54 | 127.9 | 4.3 | 125.1 | 1.9 |
| LDK-01-a07 | 154 | 150 | 0.97 | 0.138 41 | 5.24 | 0.019 6 | 1.66 | 131.6 | 6.5 | 125.3 | 2.1 |
| LDK-01-a08 | 192 | 200 | 1.04 | 0.143 88 | 3.61 | 0.020 0 | 1.55 | 136.5 | 4.6 | 127.4 | 2.0 |
| LDK-01-a09 | 212 | 268 | 1.27 | 0.134 79 | 3.55 | 0.019 7 | 1.52 | 128.4 | 4.3 | 125.4 | 1.9 |
| LDK-01-a10 | 187 | 239 | 1.28 | 0.133 83 | 5.49 | 0.019 8 | 1.50 | 127.5 | 6.6 | 126.6 | 1.9 |
| LDK-01-a11 | 172 | 170 | 0.99 | 0.134 77 | 4.89 | 0.019 5 | 1.64 | 128.4 | 5.9 | 124.4 | 2.0 |
| LDK-01-a12 | 139 | 161 | 1.16 | 0.130 21 | 4.35 | 0.019 7 | 1.71 | 124.3 | 5.1 | 125.6 | 2.1 |
| LDK-01-a13 | 71 | 57 | 0.81 | 0.140 00 | 5.93 | 0.019 9 | 1.74 | 133.0 | 7.4 | 127.2 | 2.2 |
| LDK-01-a14 | 163 | 176 | 1.08 | 0.137 20 | 3.93 | 0.019 9 | 1.54 | 130.5 | 4.8 | 126.7 | 1.9 |
| LDK-01-a15 | 45 | 29 | 0.64 | 0.153 47 | 6.84 | 0.020 1 | 1.97 | 145.0 | 9.3 | 128.4 | 2.5 |
| LDK-01-a16 | 275 | 316 | 1.15 | 0.138 47 | 3.75 | 0.020 0 | 1.61 | 131.7 | 4.6 | 127.5 | 2.0 |
| LDK-01-a17 | 100 | 111 | 1.11 | 0.139 48 | 4.85 | 0.019 7 | 1.56 | 132.6 | 6.0 | 125.7 | 1.9 |
| LDK-01-a18 | 100 | 76 | 0.76 | 0.135 33 | 4.89 | 0.020 1 | 1.53 | 128.9 | 5.9 | 128.0 | 1.9 |
| LDK-01-a19 | 102 | 89 | 0.88 | 0.136 04 | 5.91 | 0.019 6 | 2.65 | 129.5 | 7.2 | 125.0 | 3.3 |
| LDK-01-a20 | 51 | 59 | 1.16 | 0.122 61 | 7.55 | 0.019 0 | 4.39 | 117.4 | 8.4 | 121.5 | 5.3 |
 |
| 图 3 老道口闪长岩锆石CL图锆石(a)和SIMS U-Pb谐和年龄图(b)Fig.3 Cathodoluminescence ( CL) images of zircons(a)and SIMS U-Pb concordia age(b)of Laodaokou diorite |
样品元素含量分析测定工作在中国科学院地质与地球物理研究所完成，采用X射线荧光光谱仪对样品的主量元素进行了分析，分析精度和准确度优于5%。通过等离子质谱仪(X-series)进行痕量元素和稀土元素的分析。具体分析结果见表 2。
表 2 老道口地区闪长岩主量元素、微量元素和稀土元素质量分数
Table 2 Chemical compositions of major elements，trace elements，and REE elements of Laodaokou diorite
| 样品号 | SiO2 | TiO2 | Al2O3 | TFe2O3 | MnO | MgO | CaO | Na2O | K2O | P2O5 | 烧失量 | 合计 | Mg# | Na2O/K2O |
| LDK-03-A | 56.13 | 0.97 | 17.95 | 7.41 | 0.10 | 2.09 | 5.89 | 4.33 | 1.51 | 0.34 | 2.16 | 98.88 | 36.00 | 2.87 |
| LDK-03-B | 57.91 | 0.97 | 18.19 | 6.73 | 0.08 | 2.01 | 5.30 | 4.29 | 1.59 | 0.33 | 1.66 | 99.06 | 37.00 | 2.70 |
| LDK-03-C | 57.27 | 0.99 | 18.36 | 6.86 | 0.09 | 2.12 | 5.75 | 4.53 | 1.48 | 0.35 | 1.40 | 99.20 | 38.00 | 3.06 |
| LDK-03-D | 57.12 | 0.98 | 18.22 | 6.74 | 0.09 | 2.05 | 5.87 | 4.45 | 1.38 | 0.34 | 1.40 | 98.64 | 38.00 | 3.22 |
| LDK-03-E | 56.93 | 0.97 | 18.14 | 6.92 | 0.09 | 2.00 | 5.71 | 4.31 | 1.46 | 0.34 | 1.58 | 98.45 | 36.00 | 2.95 |
| 样品号 | Li | Sc | V | Cr | Co | Ni | Cu | Zn | Ga | Rb | Sr | Y | Zr | Nb |
| LDK-03-A | 13.64 | 11.69 | 123.36 | 10.39 | 20.99 | 15.30 | 63.34 | 46.52 | 19.36 | 5.38 | 708.47 | 20.91 | 180.09 | 6.97 |
| LDK-03-B | 13.81 | 15.00 | 127.18 | 9.08 | 19.29 | 9.28 | 49.69 | 33.24 | 20.46 | 30.29 | 1 018.52 | 21.41 | 181.19 | 7.51 |
| LDK-03-C | 13.52 | 14.58 | 131.79 | 6.46 | 19.72 | 6.61 | 56.94 | 36.76 | 20.51 | 19.38 | 967.46 | 20.63 | 186.16 | 7.03 |
| LDK-03-D | 12.04 | 14.45 | 128.82 | 6.63 | 19.39 | 6.58 | 59.97 | 55.61 | 20.60 | 15.51 | 1 001.32 | 20.52 | 183.43 | 7.08 |
| LDK-03-E | 13.39 | 12.20 | 132.62 | 7.15 | 17.41 | 7.51 | 45.99 | 46.00 | 20.54 | 12.74 | 879.19 | 20.73 | 176.46 | 7.13 |
| 样品号 | Cs | Ba | La | Ce | Pr | Nd | Sm | Eu | Gd | Tb | Dy | Ho | Er | Tm |
| LDK-03-A | 1.25 | 754.55 | 18.02 | 39.37 | 5.68 | 23.65 | 5.02 | 1.34 | 4.33 | 0.64 | 3.65 | 0.75 | 2.03 | 0.28 |
| LDK-03-B | 1.67 | 771.23 | 24.09 | 53.82 | 7.00 | 28.47 | 5.76 | 1.50 | 4.85 | 0.69 | 3.88 | 0.80 | 2.15 | 0.31 |
| LDK-03-C | 0.99 | 820.03 | 22.07 | 39.09 | 6.42 | 26.28 | 5.44 | 1.47 | 4.65 | 0.66 | 3.72 | 0.76 | 2.04 | 0.29 |
| LDK-03-D | 0.87 | 755.29 | 22.76 | 45.72 | 6.72 | 27.55 | 5.65 | 1.50 | 4.75 | 0.69 | 3.78 | 0.75 | 2.05 | 0.29 |
| LDK-03-E | 1.24 | 767.17 | 20.55 | 37.64 | 6.31 | 26.09 | 5.39 | 1.45 | 4.60 | 0.67 | 3.76 | 0.77 | 2.08 | 0.29 |
| 样品号 | Yb | Lu | Hf | Ta | Pb | Th | U | Eu/ Eu* | Ce/ Ce* | La/ Sm | Nb/ Ta | Sr/ Y | Sm/ Nd | ΣREE |
| LDK-03-A | 1.85 | 0.31 | 4.46 | 0.39 | 25.89 | 2.54 | 0.70 | 0.33 | 0.28 | 3.59 | 17.87 | 0.37 | 0.21 | 106.92 |
| LDK-03-B | 2.00 | 0.32 | 4.74 | 0.44 | 8.73 | 3.55 | 0.96 | 0.33 | 0.22 | 4.18 | 17.07 | 0.37 | 0.20 | 135.64 |
| LDK-03-C | 1.88 | 0.31 | 4.77 | 0.41 | 9.41 | 2.69 | 0.76 | 0.32 | 0.23 | 4.06 | 17.15 | 0.37 | 0.21 | 115.08 |
| LDK-03-D | 1.89 | 0.31 | 4.70 | 0.40 | 9.20 | 2.86 | 0.72 | 0.32 | 0.24 | 4.03 | 17.70 | 0.37 | 0.21 | 124.41 |
| LDK-03-E | 1.89 | 0.30 | 4.52 | 0.41 | 8.01 | 2.60 | 0.62 | 0.32 | 0.21 | 3.81 | 17.39 | 0.37 | 0.21 | 111.79 |
| 注：主量元素质量分数单位为%；微量元素和稀土元素质量分数单位为10-6。Mg#=100(w(MgO)/40.31)/(w(MgO)/40.31+w(TFeO)/71.85)。 | ||||||||||||||
老道口闪长岩w(SiO2)为56.13%~57.91%，w(Al2O3)为17.95%~18.36%，具有高铝质特点。样品的w(Na2O)和w(K2O)分别为4.29%~4.53%和1.38%~1.59%，Na2O/K2O值为2.70~3.22，表现出相对富Na2O的特征。在w(SiO2)-w(K2O+N2O)图解(图 4a)中，落在了闪长岩和正长闪长岩范围内。在w(SiO2)-w(K2O)图解(图 4b)中，样品落入了钙碱性系列范围内，其里特曼指数为0.83~0.89，小于3.3，具有钙碱性系列的岩浆演化趋势。w(MgO)中等，为2.00%~2.12%，Mg#值为36.00~38.00，小于高Mg闪长岩的Mg#，A/CNK为0.92~0.99，A／NK多为2.03~2.09，为准铝质岩石(图 5)。
4.3 微量元素
老道口地区闪长岩稀土元素质量分数不高，w(ΣREE)=(106.92~135.64)×10-6，LREE/HREE值为6.73~8.04，(La/Yb)N=6.57~8.12，反映轻重稀土分馏程度较高。δEu为0.85~0.87，表现出铕的弱负异常。在球粒陨石标准化的稀土元素配分曲线(图 6a)上，闪长岩轻稀土富集，曲线向右陡倾，重稀土相对亏损且分异特征不明显。在原始地幔标准化蛛网图(图 6b)上，相对于高场强元素和HREE，这些闪长岩富集大离子亲石元素(LILE：Ba，K)和元素化学性质活泼的不相容元素(U，Th，Pb)，相对亏损高场强元素(Nb、Ta、Zr、Hf、Ti)，指示了与俯冲作用相关的微量元素地球化学特征。闪长岩具有较高的w(Sr)((708.47~1 018.52)×10-6)及低的w(Yb)((1.85~2.00)×10-6)，并且具有较高的Nb/Ta及Sr/Y值，分别为17.07~17.87及33.88~48.80(表 2)，暗示了岩浆源区可能有陆壳物质的参与。但从变化不大的微量元素比值La/Sm(3.59~4.18)来看，地壳混染作用在岩浆演化过程中的影响是不大的，因此元素地球化学特征主要反映了其源区的地球化学性质[18, 52]。
5 讨论
5.1 岩石成因
老道口岩体富集大离子亲石元素(Ba，K)和元素化学性质活泼的不相容元素(U，Th，Pb)，明显亏损高场强元素(HFSE：Nb，Ta，Ti，P)，指示了与俯冲作用相关的微量元素地球化学特征[53]。老道口闪长岩强不相容元素(Th，U，K)显著富集和高场强元素(Nb，Ta)明显亏损，具该特点的闪长岩岩浆源区可能为俯冲流体交代的岩石圈地幔或是陆壳物质。由表 2可知，Nb/Ta值为17.07~17.87，明显高于壳源岩浆的Nb/Ta值(11~12)，而与幔源岩浆的Nb/Ta值(17.5)[54]相符，反映了岩浆的幔源特点。Zr/Hf值(38.23~40.38)接近于原始地幔值(36.27)，远高于大陆地壳值(11)，同样暗示岩浆的形成与地幔有关。因此，微量元素特征显示老道口闪长岩体岩浆应来源于地幔，而非地壳。样品的Th/Ce值为0.06~0.07，高于MORB(0.016)和OIB(0.05)的Th/Ce值，表明俯冲沉积物对源区组分有一定贡献[52]。Th/Ta值(6.34~8.07)、Th/Nb值(0.36~0.47)高，较好地反映了源区受俯冲流体交代作用的影响[55, 56, 57]，而在Rb/Y-Nb/Y和Nb/Zr-Th/Zr图解(图 7)中可以看出，闪长岩表现出流体交代富集的趋势。再者，大兴安岭中生代火山岩和花岗岩的Sr-Nd同位素组成稳定,εNd(t)值绝大多数集中在1~2，初始87Sr/86Sr值多数集中在0.705左右，变化范围大，反映火山岩和花岗质岩石的源区主要为起源于地幔的年轻地壳物质组成。因此，笔者认为老道口闪长岩可能是受俯冲的板片流体/沉积物交代的岩石圈地幔部分熔融而成，在上升过程中未受到明显的地壳混染，而岩石所表现出来的轻微混染特征可能受俯冲板片脱水形成的流体交代岩石圈地幔作用控制。
5.2 岩体形成时代
据阿里河幅1∶20万区域地质调查报告①，研究区已有的年代学资料多为全岩/单矿物K-Ar和锆石U-Pb等时线年龄等，其年龄变化区间为(60~225)Ma。如此不确切的年代学资料严重制约了对研究区中生代构造岩浆活动和火山岩形成的构造背景的研究，且由于K-Ar等时线测年方法本身的局限难以将上述年龄理解为岩体的形成年龄。本文采用锆石SIMS U-Pb定年的方法，锆石微量元素和SIMS定年分析表明闪长岩的锆石具有轻稀土元素亏损、重稀土元素富集以及高的Th/U值(0.64~1.28)；阴极发光图像揭示锆石具有典型的岩浆振荡环带，因此它们为岩浆成因锆石，所测得的年龄应代表岩体的形成时代。定年结果表明，闪长岩的年龄为(126.09±0.95)Ma，为早白垩世，并不是前人认为的形成于寒武纪。该年龄与大兴安岭地区广泛分布的中生代火山岩和花岗质岩石年龄一致(图 8)，这些年龄分布总体上呈NE向，与蒙古鄂霍茨克缝合带的展布方向一致，推测其形成可能受到蒙古鄂霍茨克造山带的影响。
①赵海山，表尚虎，陈荣升，等.阿里河幅(M51(16))1∶20万区域地质调查报告.哈尔滨：黑龙江省地质矿产局，1994.
 |
| 图 8 大兴安岭中北部中生代岩浆岩年龄分布图Fig.8 Age distribution of the Mesozoic igneous rocks in the northern Great Xing’an Range |
老道口闪长岩属钙碱性系列，代表一种伸展的构造背景。在大兴安岭其他地区，如柴河林场钾长花岗岩((133±3)Ma)形成于伸展的构造背景[63]；大兴安岭地区早白垩世广泛分布的火山岩也揭示了区域性伸展环境的存在[64]；早白垩世晚期广泛发育的变质核杂岩、A型花岗岩和裂谷盆地等也说明早白垩世中国东北地区处于区域性伸展环境[65, 66]。另外，部分学者对大兴安岭岩浆岩进行了岩石学、地球化学及同位素年代学等方面研究，也认为早白垩世时期是大兴安岭地区伸展构造背景下的岩浆演化重要阶段[64, 67, 68, 69, 70, 71, 72, 73, 74, 75, 76]。区域上，晚中生代地壳伸展的构造背景受何种体制制约还不是很清楚，一种可能的情况是，古亚洲洋最后消亡后的后造山环境[4, 77, 78, 79, 80, 81, 82, 83]，但是后碰撞阶段过程持续到晚中生代的可能性不大。另一种可能情况是受太平洋板块俯冲的影响，但张旗[84]认为西太平洋的向西俯冲对中国东部中生代岩浆活动影响有限，因为太平洋真正向西俯冲时间只有(125~110)Ma和(43~0)Ma两个时间段；李锦轶等[85]认为白垩世中晚期至古近纪初，中国东北及邻区的大陆才开始在古太平洋俯冲作用的影响下，遭受了伸展及岩石圈减薄作用的改造；许文良等[64]认为太平洋俯冲作用影响的空间范围主要在松辽盆地及其以东地区。由此猜测大兴安岭地区晚中生代地壳伸展的构造背景可能受到蒙古鄂霍茨克板块的影响。蒙古鄂霍茨克洋在晚古生代末期较为宽广[86]，局部已经存在俯冲[87, 88]，并延续至三叠纪；由于西伯利亚板块相对于中蒙地块的旋转，造成了鄂霍茨克板块从西向东的剪刀式关闭，西部晚三叠世开始闭合，东段的碰撞持续到晚侏罗世早白垩世[17, 27, 89, 90]。在晚侏罗世早白垩世，蒙古鄂霍茨克造山带进入造山后伸展的演化阶段[18]。研究区位于大兴安岭中北段，靠近蒙古鄂霍茨克缝合带，大兴安岭北部地区中生代火山岩具有由西向东年龄变新和源区深度增加的趋势[7, 91, 92]，暗示本区俯冲流体可能来源于蒙古鄂霍茨克洋壳。同时，蒙古鄂霍茨克洋呈剪刀式自西向东逐渐闭合，西部最终闭合时间为晚侏罗世，东部最终闭合碰撞造山为早白垩世，这一演化过程与本区闪长岩体的形成时间基本一致，进一步说明老道口岩体与蒙古鄂霍茨克洋的演化密切相关。
6 结论对老道口闪长岩体的年代学和地球化学研究获得了以下结论：
1)老道口闪长岩体的形成年龄为(126.09±0.95)Ma，为早白垩世，并非前人认为的形成于寒武纪。
2)老道口闪长岩体的岩浆源区为俯冲流体交代的岩石圈地幔，可能是受俯冲的板片流体/沉积物交代的岩石圈地幔部分熔融而成。
3)老道口闪长岩体可能成于蒙古鄂霍茨克洋闭合后的岩石圈伸展构造环境。
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