引用本文
齐忠友, 冯志强, 温泉波, 等.
东北地区嫩江东北部早古生代闪长岩的成因探讨:锆石U-Pb年代学和地球化学证据[J]. 吉林大学学报(地球科学版), 2017, 47(1): 113-125
Qi Zhongyou, Feng Zhiqiang, Wen Quanbo, et al.
Petrogenesis of the Early Paleozoic Diorite in the Northeast Nenjiang Area: Evidence from Zircon U-Pb Chronology and Geochemistry[J]. Journal of Jilin University(Earth Science Edition), 2017, 47(1): 113-125.
东北地区嫩江东北部早古生代闪长岩的成因探讨:锆石U-Pb年代学和地球化学证据
1. 黑龙江省区域地质调查所, 哈尔滨 150080;
2. 吉林大学地球科学学院, 长春 130061;
3. 太原理工大学矿业工程学院, 太原 030024
2. 吉林大学地球科学学院, 长春 130061;
3. 太原理工大学矿业工程学院, 太原 030024
摘要:
东北兴安地块与松嫩地块的拼贴演化历史一直存在较大争议, 而早古生代岩浆记录的发现无疑对该问题的解决具有重要意义。笔者在黑龙江省嫩江依克特地区识别出了早古生代闪长岩体, 其LA-ICP-MS锆石U-Pb年龄为（435.3±1.1）Ma, 该闪长岩体的SiO2质量分数为55.01%~61.82%, 全碱（Na2O+K2O）质量分数为4.55%~6.94%, Na2O/K2O值变化（2.01~48.60）较大, Al2O3质量分数为14.97%~16.67%, 具有中等程度的K2O（0.10%~2.12%）、TiO2（0.99%~1.42%）和P2O5（0.33%~0.49%）以及低的TFeO/MgO（0.51~0.96）值, 属于中钾钙碱性系列。其A/CNK值为0.78~1.35, A/NK值为1.63~2.21, 大体符合I型花岗岩特点。依克特闪长岩的稀土总量较高（w（ΣREE）=227.02×10-6~289.17×10-6）, 轻重稀土分异明显[（La/Yb）N=9.86~13.93], 并具有弱的铕异常（Eu/Eu*=0.88~1.02）；具有明显高场强元素（Nb和Ti）亏损的特征。上述特征表明, 岩浆源区为受俯冲流体交代地幔楔的部分熔融。结合区域资料, 本文认为依克特闪长岩体形成于活动大陆边缘环境, 与嫩江-黑河洋的洋壳持续俯冲相关。
关键词:
早古生代
闪长岩
锆石U-Pb年代学
地球化学
小兴安岭
嫩江
Petrogenesis of the Early Paleozoic Diorite in the Northeast Nenjiang Area: Evidence from Zircon U-Pb Chronology and Geochemistry
1. Heilongjiang Province Institute of Regional Geological Survey, Haerbin 150080, China;
2. College of Earth Science, Jilin University, Changchun 130061, China;
3. College of Mining Engineering, Taiyuan University of Technology, Taiyuan 030024, China
2. College of Earth Science, Jilin University, Changchun 130061, China;
3. College of Mining Engineering, Taiyuan University of Technology, Taiyuan 030024, China
Supported by the Natural Science Foundation of China (41602235, 41502207, 41302175) and the Project of China Geological Survey (12120114033501)
Abstract: NE China was traditionally considered the eastern part of the Central Asian Orogenic Belt (CAOB) and was composed of different mico-blocks in the Paleozoic. There are some debates about the collision age and location between the Xing'an and Songliao-Nenjiang blocks in NE China. The discovery of the records of the Early Paleozoic magmatism is a key to solve the debates. Early Paleozoic diorites are indentified in this study in the Nenjiang area, western Heilongjiang Province. The LA-ICP-MS zircon U-Pb dating indicates an age of (435.3±1.1) Ma. The diorites have 55.01%-61.82 wt% SiO2, and 14.97%-16.67 wt% Al2O3, with Na2O+K2O=4.55%-6.94 wt%, and exhibit high Na2O/K2O and low FeOT/MgO (0.51-0.96) ratios, and moderate K2O (0.10%-2.12%), TiO2 (0.99%-1.42%), and P2O5 (0.33%-0.49%). These results indicate that the diorites belong to medium K calc-alkaline series. Their A/CNK and A/NK values range from 0.78 to 1.35 and 1.63 to 2.21 respectively, which are generally consistent with those of type I granites. The diorites display right-inclined rare earth element (REE) patterns (La/Yb)N=9.86-13.93, with relatively high total REE abundances (ΣREE=227.02×10-6-289.17×10-6), and week Eu anomalies (Eu/Eu*=0.88-1.02). In trace elements, the diorites are characterized by depletion in high field strength elements (HFSEs, such as Nb and Ti). The primary magma of the diorites in the northeast Nenjiang area was generated by partial melting of mantle wedge that had been metasomatized by subduction-related fluids. Integrating regional data and the research result of this study it is suggest that the Nenjiang diorites was formed in an active continental margin setting, resulting from subduction of the paleo Nenjiang-Heihe oceanic plate located between the Xing'an and Songliao blocks.
Key words:
Early Paleozoic
diorite
U-Pb dating
geochemistry
Lesser Xing'an Range
Nenjiang area
0 引言
中亚造山带(又称阿尔泰造山带)，作为全球最大、最为复杂的造山带之一，一直以来是广大学者研究的热点，其演化过程的研究将对全球板块运动、古大陆的分裂和聚合、矿产资源的形成机制与分布有着重要意义[1-9]。尽管对于中亚造山带研究有着诸多的意义，但由于中亚造山带覆盖广阔，相关细节研究仍然较为缺乏。近年来，虽然对中亚造山带西段开展了众多研究[10-14]，但其东段，尤其是东北地区，经历了古亚洲洋构造域和西太平洋构造域在时间和空间上的叠加与改造[15]，以及大量的植被和中、新生代盆地沉积的覆盖，导致了东北地区各块体拼贴演化过程仍存在较大争论。
东北地区西部自西向东依次包括额尔古纳地块、兴安地块、松嫩(松辽)地块，各地块之间分别以得尔布干断裂、嫩江-黑河缝合带为界(图 1a)[16]。关于得尔布干断裂，早期学者将其作为古生代时期额尔古纳地块和兴安地块的拼贴界线[17-20]。但最新研究结果表明，得尔布干断裂是一条具有明显重力异常[16, 21]的中生代走滑断裂[22-24]，并不具有缝合带性质，而在其东侧却发现了相关缝合带的证据，因而根据新林E-MORB型蛇绿混杂岩(539 Ma K-Ar)[25]、阿里河辉石岩(629 Ma U-Pb)[26]、吉峰蛇绿混杂岩中的E-MORB型辉长岩[27]、头道桥蓝片岩(511 Ma U-Pb)[28-29]以及塔河造山后花岗岩(~480 Ma U-Pb)[30]，将形成于早古生代的新林-喜桂图缝合带作为额尔古纳地块和兴安地块的拼贴界线。
至于兴安地块与松嫩地块之间的嫩江-黑河洋被提出后，其所代表大洋的俯冲闭合过程及两地块拼贴时限一直存在争议；部分学者根据多宝山斑岩型Cu矿成矿年龄(~480 Ma)，认为嫩江-黑河洋在早奥陶世开始俯冲消减[31-36]，于晚泥盆世之前消亡[37-39]，导致兴安地块与松嫩地块碰撞拼贴，晚古生代形成统一佳蒙地块[40-42]；部分学者根据岩浆活动认为该大洋于晚泥盆世-早石炭世消亡[43-47]；另部分学者则认为早二叠世该大洋仍未闭合[48-50]。由此可见，嫩江-黑河洋是从奥陶纪一直持续俯冲到晚泥盆世？早石炭世末？还是二叠纪？仍存在较大争论。
最近，笔者在嫩江依克特地区识别出一套早古生代闪长岩体，本文对该岩体进行了详细的岩石学、年代学和地球化学研究，以期探讨早古生代嫩江地区的大地构造背景与该闪长岩形成的动力学机制，为构建兴安与松嫩地块之间大洋演化提供最新的数据资料。
1 地质背景与样品描述研究区位于黑龙江省嫩江依克特东北部，大地构造位置上位于扎兰屯-嫩江-黑河缝合带北段，兴安地块以东，松嫩地块以西，研究区属于小兴安岭的中部，盛产铜、钼等矿产资源。早期资料显示该区出露的最老地层单元为凤水沟河组，主要由一套片岩、片麻岩、变粒岩、长英质角岩和大理岩组成[51]；但最新锆石U-Pb年龄测试显示，黑河附近凤水沟河组中变粒岩及其片麻状花岗岩侵入体最小值分别为256 Ma和183 Ma，并不是先前认为的新元古代，而是晚古生代[52]。奥陶系为中酸性凝灰岩、熔岩及陆相复理石建造，显示活动大陆边缘特点[50-52]；志留系以稳定陆源碎屑岩夹火山岩为主，可见图瓦贝化石[53-56]；泥盆系为海相碳酸盐沉积夹中基性火山岩[51]；石炭系-二叠系主要为火山岩及部分碎屑岩[56]。区内分布着大面积的古生代花岗质岩石(图 1b)，以二长花岗岩和闪长岩为主。研究区的闪长岩仅分布依克特以东一带，呈多个小岩株出露，发育面积较小(约5.16 km2)。在1:20万霍龙门幅地质图中，这些闪长岩时代被归属于早石炭世[56]。野外观察表明，依克特闪长岩岩体岩性较单一，受后期构造运动改造明显，普遍具片理化、碎裂岩化，局部具糜棱岩化(图 2a，b)。
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| a、b.闪长岩野外照片；c、d.闪长岩镜下特征。Q.石英；Amp.角闪石；Pl.斜长石。 图 2 依克特闪长岩野外及镜下照片 Figure 2 Field and microscopic photographs of the diorites in the Yikete area |
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本文所测定的嫩江依克特地区闪长岩样品(D9225)的岩石学特征如下(图 2)：
采样点位于嫩江县依克特(49°58′05″N，125°48′39″E)。岩石呈灰白色，以柱粒结构为主，似斑状结构次之(图 2a、b)，岩石粒度为0.5~5.0 mm。主要矿物由斜长石、角闪石、石英组成，局部见5%黑云母及少量钾长石。斜长石呈半自形粒状，聚片双晶发育，体积分数为50%~60%，具绿帘石化及黝帘石化；角闪石半自形柱状，体积分数为30%~40%，大部分充填于斜长石空隙间，有时与斜长石构成嵌晶含长结构，具不同程度的帘石化及碳酸盐化(图 2c、d)。
2 分析方法本文测年锆石的分选在河北廊坊地质调查院完成，锆石U-Pb同位素定年在中国地质调查局天津地质调查中心实验室进行。将人工重砂分选的锆石颗粒用环氧树脂固定并抛光，使锆石颗粒露出核部。在测定之前，用体积分数为3%的HNO3清洗样品表面，以除去表面污垢；然后进行透射光和反射光照相，并在英国Gatan公司生产的Mono CL3+阴极发光装置系统上进行阴极发光(CL)照相。实验采用激光剥蚀等离子体分析技术(LA-ICP-MS)，实验激光束斑直径为32 um，频率为10 Hz，激光能量为0.09 J，采用高纯氦气作为剥蚀物质的载气，每个分析点的气体背景采集时间为30 s，信号采集时间为40 s。采用美国国家标准技术研究院研制的人工合成硅酸盐玻璃标准参考物质NIST SRM610进行仪器最佳化，利用哈佛大学国际标准锆石91500作为外部校正[57]。分析结果采用GLITTER (ver4.0 Macquarie University)程序。年龄计算采用Isoplot程序(Ver3.23)处理。实验数据运用Andersen的方法进行同位素比值校正[58]，以消除普通204 Pb的影响。详细流程和原理参见文献[59]的阐述。测试数据见表 1。
表 1 嫩江依克特闪长岩(D9225)锆石LA-ICP-MS U-Pb分析结果
Table 1 LA-ICP-MS zircon U-Pb isotope data of the Yikete diorites (D9225)
| 样品号 | wB/10-6 | 同位素比值 | 年龄/Ma | |||||||||||
| Pb | U | 206Pb/238U | 1σ | 207Pb/235U | 1σ | 208Pb/232Th | 1σ | 232Th/238U | 1σ | 206Pb/238U | 1σ | 207Pb/235U | 1σ | |
| 1 | 10 | 128 | 0.069 7 | 0.000 4 | 0.665 4 | 0.012 0 | 0.028 6 | 0.001 1 | 0.680 7 | 0.003 5 | 434 | 3 | 518 | 9 |
| 2 | 3 | 41 | 0.070 0 | 0.000 5 | 0.556 6 | 0.038 0 | 0.024 2 | 0.001 0 | 0.796 1 | 0.005 4 | 436 | 3 | 449 | 31 |
| 3 | 2 | 26 | 0.070 4 | 0.000 6 | 0.540 4 | 0.048 0 | 0.024 7 | 0.001 0 | 0.888 5 | 0.005 2 | 439 | 4 | 439 | 39 |
| 4 | 10 | 119 | 0.069 8 | 0.000 4 | 0.575 9 | 0.013 2 | 0.023 1 | 0.000 9 | 1.076 8 | 0.005 9 | 435 | 3 | 462 | 11 |
| 5 | 16 | 192 | 0.069 9 | 0.000 4 | 0.541 1 | 0.008 2 | 0.022 3 | 0.000 8 | 0.894 8 | 0.006 8 | 436 | 3 | 439 | 7 |
| 6 | 41 | 520 | 0.069 6 | 0.000 4 | 0.535 4 | 0.004 4 | 0.021 8 | 0.000 8 | 0.801 9 | 0.004 1 | 434 | 3 | 435 | 4 |
| 7 | 8 | 96 | 0.070 0 | 0.000 4 | 0.574 0 | 0.018 0 | 0.020 8 | 0.000 8 | 0.952 0 | 0.004 7 | 436 | 3 | 461 | 14 |
| 8 | 9 | 105 | 0.069 5 | 0.000 4 | 0.612 6 | 0.018 7 | 0.021 1 | 0.000 8 | 1.157 9 | 0.006 0 | 433 | 3 | 485 | 15 |
| 9 | 7 | 80 | 0.069 7 | 0.000 5 | 0.585 3 | 0.017 6 | 0.021 0 | 0.000 8 | 1.102 0 | 0.006 1 | 434 | 3 | 468 | 14 |
| 10 | 3 | 37 | 0.068 7 | 0.000 5 | 0.539 4 | 0.029 5 | 0.023 3 | 0.001 0 | 0.801 9 | 0.007 9 | 429 | 3 | 438 | 24 |
| 11 | 18 | 234 | 0.069 9 | 0.000 4 | 0.540 5 | 0.006 1 | 0.021 2 | 0.000 8 | 0.779 8 | 0.003 7 | 436 | 3 | 439 | 5 |
| 12 | 9 | 103 | 0.069 8 | 0.000 4 | 0.538 3 | 0.015 9 | 0.021 0 | 0.000 8 | 1.148 4 | 0.005 6 | 435 | 3 | 437 | 13 |
| 13 | 3 | 38 | 0.069 7 | 0.000 5 | 0.540 7 | 0.039 6 | 0.022 2 | 0.001 0 | 0.639 1 | 0.003 2 | 434 | 3 | 439 | 32 |
| 14 | 6 | 75 | 0.070 0 | 0.000 4 | 0.543 5 | 0.016 5 | 0.021 3 | 0.000 8 | 0.758 1 | 0.003 7 | 436 | 3 | 441 | 13 |
| 15 | 11 | 143 | 0.069 9 | 0.000 4 | 0.576 3 | 0.010 6 | 0.021 2 | 0.000 8 | 0.806 7 | 0.004 0 | 435 | 3 | 462 | 9 |
| 16 | 13 | 158 | 0.070 1 | 0.000 4 | 0.547 5 | 0.008 6 | 0.020 9 | 0.000 8 | 1.082 3 | 0.005 2 | 437 | 3 | 443 | 7 |
| 17 | 4 | 47 | 0.069 4 | 0.000 5 | 0.643 5 | 0.031 7 | 0.022 0 | 0.000 9 | 1.111 5 | 0.005 6 | 433 | 3 | 505 | 25 |
| 18 | 26 | 331 | 0.070 0 | 0.000 4 | 0.553 0 | 0.005 8 | 0.019 9 | 0.000 8 | 0.874 1 | 0.004 2 | 435 | 3 | 447 | 5 |
| 19 | 3 | 41 | 0.069 9 | 0.000 5 | 0.590 1 | 0.039 0 | 0.019 7 | 0.000 8 | 1.197 8 | 0.006 6 | 435 | 3 | 471 | 31 |
| 20 | 3 | 37 | 0.070 2 | 0.000 4 | 0.552 5 | 0.008 9 | 0.020 4 | 0.000 8 | 1.114 1 | 0.005 4 | 437 | 3 | 447 | 7 |
| 21 | 12 | 151 | 0.070 2 | 0.000 4 | 0.569 6 | 0.003 6 | 0.019 3 | 0.000 7 | 0.869 3 | 0.006 1 | 437 | 3 | 458 | 3 |
| 22 | 39 | 486 | 0.069 8 | 0.000 5 | 0.539 3 | 0.032 9 | 0.019 2 | 0.000 8 | 1.032 7 | 0.005 0 | 435 | 3 | 438 | 27 |
| 23 | 6 | 67 | 0.070 0 | 0.000 4 | 0.581 7 | 0.013 1 | 0.019 8 | 0.000 8 | 1.144 7 | 0.006 8 | 436 | 3 | 466 | 10 |
| 24 | 10 | 121 | 0.070 1 | 0.000 5 | 0.549 7 | 0.031 5 | 0.019 6 | 0.000 8 | 0.882 5 | 0.005 1 | 437 | 3 | 445 | 25 |
| 25 | 4 | 50 | 0.070 1 | 0.000 5 | 0.549 2 | 0.003 9 | 0.019 3 | 0.001 0 | 0.659 5 | 0.032 0 | 436 | 3 | 444 | 3 |
| 注：同位素比率已采用208 Pb校正法进行了普通铅校正。 | ||||||||||||||
选择新鲜样品经过无污染碎样后，在中国地质调查局天津地质调查中心实验室进行主量、微量和稀土元素分析。主量元素采用X-荧光光谱法(XRF)分析，分析准确度和精度优于5%；微量元素和稀土元素的分析采用电感耦合等离子质谱(ICP-MS)分析方法，准确度和精度优于10%；测试数据见表 2。
表 2 依克特闪长岩主量元素、微量元素分析结果
Table 2 Major and trace element analyzing results of the Yikete diorites
| 样品号 | SiO2 | TiO2 | Al2O3 | Fe2O3 | FeO | MnO | MgO | CaO | Na2O | K2O | P2O5 | 烧失量 | 总量 | Mg# | K2O+ Na2O |
A/ CNK |
A/ NK |
P | La | Ce | Pr | Nd | Sm | Eu | Gd | Tb | Dy | Ho | Er | Tm | Yb | Lu | Y | Cs | Rb | Sr | Ba | Ga | Nb | Ta | Zr | Hf | Th | V | Cr | Co | Ni | B | Sc | U | Ti | ∑REE | δEu | (La/ Yb) N |
| D9226 | 60.43 | 1.24 | 16.67 | 2.92 | 2.63 | 0.09 | 2.75 | 4.10 | 4.82 | 2.12 | 0.37 | 1.63 | 99.77 | 50.89 | 6.94 | 0.94 | 1.63 | 1 614.00 | 45.77 | 135.4 | 15.75 | 55.10 | 9.18 | 2.99 | 8.45 | 1.34 | 6.46 | 1.53 | 3.38 | 0.66 | 2.72 | 0.44 | 34.67 | 15.59 | 73.10 | 780.20 | 868.50 | 30.60 | 51.67 | 5.16 | 364.30 | 19.56 | 14.73 | 162.30 | 81.90 | 17.46 | 45.14 | 22.50 | 15.59 | 3.27 | 7 405.00 | 289.17 | 1.02 | 11.34 |
| D9227 | 61.82 | 0.99 | 15.95 | 2.65 | 2.95 | 0.10 | 2.92 | 3.92 | 3.98 | 1.98 | 0.33 | 2.23 | 99.82 | 52.02 | 5.96 | 1.01 | 1.84 | 1 435.00 | 46.37 | 95.02 | 11.23 | 41.77 | 7.88 | 2.24 | 6.99 | 1.15 | 5.96 | 1.13 | 3.18 | 0.48 | 3.17 | 0.45 | 27.58 | 12.45 | 50.40 | 404.80 | 665.70 | 18.76 | 21.95 | 1.43 | 311.80 | 14.40 | 8.01 | 95.00 | 56.40 | 15.80 | 31.70 | 18.71 | 12.45 | 1.56 | 5 924.00 | 227.02 | 0.90 | 9.86 |
| D9225 | 55.01 | 1.42 | 14.97 | 3.42 | 4.55 | 0.14 | 6.01 | 6.84 | 3.31 | 1.24 | 0.49 | 2.42 | 99.82 | 60.95 | 4.55 | 0.78 | 2.21 | 2 143.00 | 51.83 | 96.93 | 12.59 | 47.60 | 8.79 | 2.43 | 7.79 | 1.34 | 6.64 | 1.58 | 3.41 | 0.68 | 2.76 | 0.45 | 34.14 | 27.36 | 42.10 | 679.80 | 402.00 | 26.70 | 25.96 | 1.66 | 219.50 | 10.64 | 6.00 | 234.30 | 220.30 | 35.00 | 106.70 | 9.15 | 27.36 | 1.58 | 8 514.00 | 244.82 | 0.88 | 12.66 |
| TC30 | 59.89 | 1.28 | 16.50 | 2.49 | 3.31 | 4.19 | 2.74 | 2.25 | 4.86 | 0.10 | 0.38 | 1.76 | 99.74 | 49.44 | 4.96 | 1.35 | 2.04 | 1 678.00 | 48.76 | 95.01 | 11.71 | 45.04 | 7.62 | 2.19 | 6.87 | 1.01 | 5.04 | 0.98 | 2.54 | 0.43 | 2.36 | 0.36 | 24.50 | 0.90 | 40.60 | 617.70 | 952.30 | 22.31 | 33.58 | 1.41 | 426.10 | 19.31 | 6.15 | 125.20 | 51.70 | 19.60 | 39.10 | 22.20 | 14.67 | 1.42 | 7 699.00 | 229.92 | 0.91 | 13.93 |
| 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)。 | ||||||||||||||||||||||||||||||||||||||||||||||||||||||
嫩江县依克特地区闪长岩(D9225)锆石CL图像(图 3)显示，锆石为短柱状到长柱状，多为半自形，较发育振荡环带，粒径为80~120 μm，长宽比值为1:1~2:1，Th/U值多为0.64~1.16(表 1)，显示为岩浆锆石。测年数据结果见表 1，25个测试点集中分布在谐和线上，得到206 Pb /238 U加权平均年龄为(435.3±1.1) Ma (MSWD=0.43，n=25)(图 4)。该年龄被解释为闪长岩体侵位年龄，表明其形成于早志留世，并不是前人认为的早石炭世。
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| 图 3 嫩江东依克特闪长岩中部分锆石的CL图像 Figure 3 CL images of selected zircon from the Yikete diorite |
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| 图 4 嫩江依克特地区闪长岩锆石U-Pb谐和图(a)和频数图(b) Figure 4 Concordia diagram (a) and frequency diagram (b) showing LA-ICP-MS zircon U-Pb dating result for the Yikete diorites |
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依克特闪长岩的SiO2质量分数为55.01%~61.82%，全碱(Na2O + K2O)质量分数为4.55%~6.94%，Na2O/K2O值(2.01~48.60)变化较大，并且Na2O质量分数远大于K2O质量分数，Al2O3质量分数为14.97%~16.67%，具有中K2O (0.10%~2.12%)、TiO2(0.99%~1.42%)和P2O5(0.33%~0.49%)质量分数以及低的TFeO/MgO (0.51~0.96)值特征。该闪长岩大部分落入中钾钙碱性系列(图 5)，与同时代多宝山矿集区内高钾-中钾火山岩相类似[60]。其A/CNK值为0.78~1.35，属于次铝-过铝质，A/NK值为1.63~2.21，里特曼指数(σ)为1.45~2.76。总体来看，该区闪长岩为略贫碱、次铝质钙碱性岩石，主体符合I型花岗岩特点。
依克特闪长岩的稀土元素总质量分数为227.02×10-6~289.17×10-6，轻稀土元素(LREE)相对重稀土元素(HREE)富集，LREE/HREE值为9.09~10.93，平均值为10.01，(La/Yb)N值为9.86~13.93。在稀土元素球粒陨石标准化模式图(图 6a)上，所有样品均表现为右倾的曲线，伴随有弱的Eu负异常(Eu/Eu*值为0.88~1.02)。微量元素蛛网图(图 6b)显示，高场强元素(HFSE) Nb、Ti元素负异常，Th、Zr正异常，大离子亲石元素(LILE) Rb、Sr、K负异常特征，总体与俯冲带岛弧岩浆作用类似。Nb、Ti的亏损反映了岩浆受到了地壳物质的强烈混染或者可能与源区流体的交代作用有关。闪长岩中Ba/Nb的比值变化较大，而Ba/Rb的比值相对稳定，说明岩石受后期的蚀变作用较弱[63]，这与岩相学观察相吻合，其主量和微量元素分析结果基本上代表了原始岩浆的特征。
对于依克特闪长岩的形成时代，前人曾根据野外地层接触关系将该侵入岩归属于泥盆纪-二叠纪[53]，但没有同位素定年资料的支持。本文测定闪长岩的锆石具有岩浆成因的生长环带，它们的Th/U值多为0.64~1.16，暗示这些锆石为岩浆成因，因此其年龄(435.3±1.1) Ma代表锆石的结晶年龄，亦即闪长岩体的侵位年龄，表明依克特地区闪长岩形成于早志留世。这与其侵入奥陶系裸河组[56]的地质事实相吻合。此外，依克特闪长岩的年龄与多宝山地区早古生代的玄武安山岩(450 Ma)、安山岩(447 Ma)[60]的年龄相近，代表了嫩江地区早志留世岩浆作用的深成侵入相。
4.2 岩石成因依克特闪长岩显示贫碱(全碱质量分数为4.55%~6.94%)、次铝-过铝质钙碱性特点，具较高的Mg#值(49.44~60.95)和富Na，显示岩浆源区为岩石圈地幔的属性。闪长岩样品富集Ba、Hf，亏损Nb、Ti特征可能主要有两种形成机制：1)强烈地壳混染；2)由于俯冲带流体而形成的富集地幔熔融。Nb/U、Ta/U值通常可以作为判断地壳混染的参考指示。样品的Nb/U、Ta/U值分别为17.49、1.13，明显低于MORB/OIB值(Nb/U=47、Ta/U=2.7)[64]，而接近于地壳值(Nb/U=12.1、Ta/U=1.1)[65]，并且样品La/Nb和Ba/Nb低于陆壳值[66]，显示出一定地壳混染特征。然而，依克特闪长岩又具有弱的Zr、Hf正异常，表明其不是简单陆壳混染的产物。结合该区域同时代的中基性火山岩的锆石较高εHf(t)值(+11.5~+17.6)和较高εNd(t)值(5.24~5.77)[60]，依克特闪长岩所表现的地壳混染特征可能与来自俯冲板片的流体/熔体交代作用有关。
4.3 地质意义东北地区主要由众多微陆块组成，自西向东依次包括额尔古纳、兴安、松嫩、佳木斯地块[67]。研究表明，额尔古纳和兴安地块已于早古生代完成拼贴[26-29]。然而，关于额尔古纳兴安地块与松嫩地块之间洋盆(嫩江-黑河洋)的直接证据(如蛇绿岩、构造混杂岩)缺乏，进而导致该洋盆建立及其两地块的拼贴仍存在争论[67-71]。近年来，众多学者从古生代火成岩角度研究来解释嫩江-黑河洋的演化。
关于嫩江-黑河洋洋壳俯冲，则是依据嫩江县多宝山斑岩Cu-Mo矿床成矿年龄(~480 Ma/Re-Os)和其地球化学特征，提出大兴安北段嫩江地区早古生代早期岩浆作用及斑岩性Cu-Mo矿床的形成与嫩江-黑河洋洋壳俯冲有关，形成于活动大陆边缘环境[31-36]。该俯冲作用可能一直持续到石炭纪[43-47]，而早石炭世晚期兴安地块与松嫩地块拼贴，导致小兴安岭西北部(嫩江-黑河)地区晚古生代(290~260 Ma)造山后A型花岗岩的出现[72-73]，大体反映了嫩江-黑河洋的发展与消亡过程。
嫩江依克特地区早古生代闪长岩((435.3±1.1) Ma)及同时代基性火山岩地球化学特征[60]，正好添补了该洋盆在晚奥陶世至早志留世的岩浆作用，且该时期的闪长岩形成可能与来自俯冲板片的流体/熔体交代作用有关。因此，依克特闪长岩代表岛弧岩浆作用的侵入相，同时也进一步说明兴安与松嫩地块拼贴要晚于早志留世。
5 结论1)嫩江依克特地区闪长岩形成于于早志留世(435.3±1.1) Ma，而非前人认为的早石炭世。
2)嫩江依克特地区闪长岩岩浆来源受俯冲板片流体交代的地幔楔部分熔融控制。
3)嫩江依克特地区早志留世闪长岩形成于活动大陆边缘环境，与嫩江-黑河洋板片俯冲相关。
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