Petrogenesis of Middle Devonian Chaoyangdi High Sr/Y Granite and Constraints on the Evolution of Xing-Meng Orogeny
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摘要: 兴蒙造山带位于华北板块和西伯利亚板块之间，具有复杂的构造演化历史，其构造格局和拼合机制一直存在较大争议.本次在兴蒙造山带南部的朝阳地识别出一套形成于伸展背景的中泥盆世高Sr/Y花岗岩，可对早古生代末期弧陆拼贴过程进行约束.朝阳地花岗岩锆石U-Pb年龄为386.8±2.9 Ma，属于中泥盆世.岩石地球化学分析显示高SiO2、Al2O3、Na2O含量，中等CaO、K2O含量，较低FeOt、MgO含量的特征，Na2O/K2O比值均大于1，属于中钾钙碱性I型花岗岩；A/CNK范围为1.02~1.08，属于弱过铝质系列；微量元素具有富集Rb、Ba、K等大离子亲石元素及Sr，弱亏损Nb、Ta、P、Ti等高场强元素的特征，Sr/Y比值高（103~146）；具有轻稀土富集的配分模式（（La/Yb）N=9.9~14.6），重稀土分馏较弱，（Gd/Yb）N范围为1.45~1.97，具有弱Eu正异常（δEu值1.31~1.80），地球化学分析表明，高Sr/Y比值继承自岩浆源区而非加厚地壳的熔融.朝阳地侵入岩均具有富集的Sr-Nd-Hf同位素组成，εNd（t）和εHf（t）均为负值（范围分别为-18.6~-17.9，-38.30~-23.59），锆石Hf模式年龄范围为2 825~3 745 Ma，集中于2 800~3 000 Ma，Nd模式年龄较集中（2 584~2 642 Ma）.综合岩石学、元素及同位素地球化学分析，朝阳地高Sr/Y侵入岩是中泥盆世在区域伸展背景下，由具有高Sr/Y比值的古老基性下地壳物质受减压和上涌软流圈加热共同作用发生部分熔融形成，代表泥盆纪白乃庙岛弧与华北陆块碰撞后区域伸展背景.Abstract: Xing-Meng orogeny is the accretionary orogeny between Siberia and North China plates with complex multi-stage subduction and accretion, and its tectonic evolution. has remained controversial for a long time. To reveal the arc-continent collision in the end of Early Paleozoic, this paper presents a study on Chaoyangdi Middle Devonian high Sr/Y granite in southern part of Xing-Meng orogeny zircon U-Pb dating results yield a formation age of 386.8±2.9 Ma, with the corresponding age of Middle Devonian (D2). Geochemical data shows that these rocks have high SiO2, Al2O3 and Na2O, moderate CaO and K2O, but low FeOt and MgO contents with the Na2O/K2O>1 and calc-alkaline series signature. The A/CNK ratios range from 1.02 to 1.08, indicating these samples are weak peraluminous series. Trace element analysis results display enrichment of LILEs, such as Rb, Ba, K and Sr, but depletion of HFSE, i.e., Nb, Ta, P and Ti, with high Sr/Y ratios (103-146), similar with adakitic-affinity. These rocks have strong fractionation between LREE and HREE ((La/Yb)N=9.9-14.6), no obvious HREE fractionation ((Gd/Yb)N=1.45-1.97) and weak positive Eu anomalies (δEu=1.31-1.80). All these geochemical characteristics suggest that high Sr/Y signature is inherited from magma source. Sr-Nd-Hf analyses show enriched isotopic signatures-both εHf(t) and εNd(t) are negative(-38.30 to -23.59 and -18.6 to -17.9) with old two-stage model age (2 825 to 3 745 Ma for Hf, 2 584 to 2 642 Ma for Nd), indicating an old enriched crustal source. Based on petrology, geochemistry and Hf-Sr-Nd isotopic characteristics, we conclude that the Chaoyangdi Middle Devonian intrusive rocks were formed by partial melting of ancient basic lower crust with high Sr/Y ratios and formed by post-collisional extension and heating of asthenosphere upwelling, indicating the regional extension after collision between the Bainaimiao arc and the North China Block.
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图 1 河北围场朝阳地地区地质简图
1.中泥盆世二长花岗岩；2.晚太古代单塔子岩群；3.古元古代宝音图岩群；4.中二叠世额里图组；5.早侏罗世下花园组; 6.晚侏罗世土城子组；7.早白垩世张家口组；8.早白垩世义县组；9.中新世汉诺坝组；10.第四系；11.新太古代花岗闪长质片麻岩；12.侏罗纪-白垩纪花岗岩；13.层理/片麻理产状；14.采样点.图1b据Jian et al.(2008)修改；图1d据中国地质科学院地质研究所, 2009, 1：25万西老府(K50C002003)地调图修改
Fig. 1. Geological sketch of Chaoyangdi region, Weichang County, Hebei
图 2 朝阳地侵入岩野外及镜下照片
a.中泥盆世二长花岗岩被早白垩世正长花岗岩侵入；b.中泥盆世二长花岗岩侵入新太古代单塔子群黑云斜长片麻岩中；c.二长花岗岩露头；d.二长花岗岩镜下照片.矿物代号：Qtz.石英；Pl.斜长石；Kf.钾长石；Bi.黑云母
Fig. 2. Field and microscope photographs of Chaoyangdi intrusive rocks
图 3 锆石阴极发光及LA-MC-ICPMS测年、Hf同位素分析点位
左下角数字为点号；实心圆圈为测年；虚线圈为Hf同位素分析
Fig. 3. Cathodoluminescence images and analysis spots of zircons
图 4 朝阳地侵入岩锆石LA-MC-ICPMS U-Pb测年谐和图
Fig. 4. Concordia diagrams for LA-MC-ICPMS zircon U-Pb dating of Chaoyangdi intrusive rocks
图 5 朝阳地侵入岩SiO2-K2O图解(a)和AR-SiO2图解(b)
图a据Le Maitre et al.(1989)；图b据Wright(1969)
Fig. 5. SiO2-K2O (a) and AR-SiO2 (b) diagram of Chaoyangdi intrusive rocks
图 6 朝阳地侵入岩SiO2-(K2O+Na2O)图解(a)和A/CNK-A/NK图解(b)
图a据Wilson(1989)；图b据Maniar and Piccoli(1989)
Fig. 6. SiO2-(K2O+Na2O) (a) and A/CNK-A/NK (b) diagram of Chaoyangdi intrusive rocks
图 7 朝阳地侵入岩原始地幔标准化微量元素蛛网图和稀土配分模式
原始地幔标准化数据根据Sun and McDonough(1989)
Fig. 7. Primitive mantle-normalized trace elements spider diagram (a) and chondrite-normalized REE patterns (b) of Chaoyangdi intrusive rocks
图 8 朝阳地侵入岩εHf(t)-t图解(a)和εNd(t)-(86Sr/87Sr)i图解(b)
图a据Yang et al.(2006)；图b中华北克拉通基性下地壳同位素组成据Jiang et al.(2013)
Fig. 8. εHf(t)-t (a) and εNd(t)-(86Sr/87Sr)i (b) diagrams of Chaoyangdi intrusive rocks
图 9 朝阳地侵入岩埃达克岩判别图解
图a据Defant and Drummond(1990)；图b据Martin et al.(2005)
Fig. 9. Adakite discrimination diagrams of Chaoyangdi intrusive rocks
图 10 华北北缘晚古生代末期构造演化模式
Fig. 10. The tectonic evolution model of northern of North China in Late Paleozoic
表 1 朝阳地侵入岩锆石U-Pb测年分析结果
Table 1. Zircon LA-MC-ICPMS U-Pb dating data of Chaoyangdi intrusive rocks
点号 Pb
(10-6)U
(10-6)Th/U 同位素比值 年龄(Ma) 谐和度
(%)206Pb/238U 1σ 207Pb/235U 1σ 206Pb/238U 1σ 207Pb/235U 1σ 1 16 271 0.27 0.061 7 0.000 7 0.463 1 0.009 3 386 4 386 8 100 2 8 121 0.59 0.064 1 0.000 7 0.497 0 0.018 1 400 4 410 15 98 3 11 186 0.25 0.063 0 0.000 7 0.484 7 0.018 2 394 4 401 15 98 4 12 188 0.96 0.061 4 0.000 7 0.482 9 0.013 4 384 4 400 11 96 5 7 80 0.25 0.091 7 0.002 2 0.861 1 0.060 2 565 13 631 44 88 6 7 116 0.54 0.061 4 0.000 7 0.461 3 0.016 7 384 4 385 14 100 7 11 184 0.19 0.062 3 0.001 0 0.471 1 0.018 6 390 6 392 16 99 8 8 135 0.46 0.062 8 0.000 7 0.476 8 0.014 7 393 4 396 12 99 9 7 126 0.22 0.061 7 0.001 0 0.474 4 0.031 8 386 6 394 26 98 10 9 128 0.31 0.068 9 0.000 9 0.583 8 0.017 2 430 6 467 14 91 11 16 277 0.31 0.061 6 0.000 7 0.466 1 0.008 3 386 4 388 7 99 12 8 145 0.20 0.061 2 0.000 7 0.461 5 0.023 8 383 4 385 20 99 13 11 180 0.29 0.061 6 0.000 7 0.478 3 0.013 8 385 4 397 11 97 14 19 322 0.25 0.060 5 0.000 7 0.453 0 0.012 1 379 4 379 10 100 15 18 299 0.24 0.061 5 0.000 7 0.474 0 0.008 5 385 4 394 7 98 16 12 206 0.27 0.061 5 0.000 7 0.465 4 0.014 2 384 4 388 12 99 17 7 119 0.29 0.062 7 0.000 8 0.516 1 0.038 0 392 5 423 31 92 18 6 105 0.32 0.061 2 0.000 7 0.484 6 0.029 8 383 5 401 25 95 19 15 243 0.37 0.062 3 0.000 7 0.470 9 0.011 1 390 4 392 9 99 
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表 2 朝阳地侵入岩主量元素(%)和微量元素(10-6)分析结果
Table 2. Major (%) and trace (10-6) elements data of Chaoyangdi intrusive rocks
样品号 15YS12 15YS13 15YS14 15YS15 15YS17 15YS18 标样测试值 标样推荐值 相对偏差 允许误差 SiO2 71.17 69.62 70.19 71.23 71.5 69.51 73.18 72.83 0.24 0.33 Al2O3 15.69 16.08 15.95 15.71 15.45 16.31 13.43 13.4 0.11 1.91 Fe2O3t 1.85 2.22 2.21 1.32 1.76 2.33 - - - - CaO 2.32 2.36 2.21 1.42 2.26 2.5 1.53 1.55 0.65 4.2 MgO 0.49 0.56 0.54 0.27 0.35 0.56 0.4 0.42 2.44 5.92 K2O 2.89 3.3 2.76 2.91 2.72 2.85 5.06 5.01 0.5 2.87 Na2O 4.63 4.51 4.72 5.4 4.95 4.73 3.13 3.13 0 3.38 TiO2 0.21 0.23 0.24 0.15 0.2 0.27 0.29 0.29 0 6.46 P2O5 0.08 0.1 0.094 0.059 0.067 0.098 0.092 0.093 0.54 8.3 MnO 0.055 0.053 0.057 0.046 0.054 0.064 0.06 0.06 0 9.08 烧失量 0.63 0.95 1.03 1.49 0.69 0.78 0.69 0.69 0 0 Na2O/K2O 1.6 1.37 1.71 1.86 1.82 1.66 - - - - Cr 4.03 3.97 5.31 1.17 3.27 5.01 3.95 3.6 4.64 22.25 Ni 2.28 2.26 3.15 0.79 2.26 2.58 1.63 2.3 17.05 23.86 Co 2.09 2.07 2.49 0.92 1.46 2.57 2.7 3.4 11.48 22.45 Rb 58 60.4 64.6 66.8 44.2 52.4 - 466 - - Cs 1.23 1.23 1.46 1.59 1.14 0.92 36.9 38.4 1.99 15.1 Sr 823 689 883 714 638 886 - 106 - - Ba 1 150 1 240 1 240 1 060 1 200 1 020 286 343 9.06 10.14 Nb 7.35 7.54 7.79 10.6 6.89 9.14 42.7 40 3.26 14.99 Ta 0.38 0.39 0.36 0.58 0.34 0.51 6.29 7.2 6.75 19.93 Zr 95.9 112 126 94.7 95.7 128 176 167 2.62 11.62 Hf 2.47 3 3.13 2.47 2.39 2.96 6.26 6.3 0.32 20.36 U 0.54 0.52 0.55 1.01 0.46 0.64 18.2 18.8 1.62 17.03 Th 1.5 2.08 1.89 1.93 1.39 2.51 45.7 54 8.32 14.23 La 9 13.7 12.7 12.1 9.51 18.3 51 54 2.86 14.23 Ce 24.2 26.2 27.4 25.2 22.3 32.8 106 108 0.93 12.59 Pr 2.04 2.86 2.52 2.29 2.04 3.51 12.8 12.7 0.39 18.17 Nd 7.94 10.8 9.5 8.31 7.76 13 46.1 47 0.97 14.58 Sm 1.47 1.91 1.61 1.4 1.4 2.16 7.58 9.7 12.27 18.99 Eu 0.79 0.95 0.87 0.71 0.77 0.92 0.69 0.85 10.39 27.78 Gd 1.32 1.79 1.48 1.35 1.22 2.14 7.71 9.3 9.35 19.12 Tb 0.19 0.24 0.21 0.19 0.16 0.26 1.33 1.65 10.74 25.11 Dy 0.98 1.14 1.02 1.06 0.88 1.32 8.15 10.2 11.17 18.84 Ho 0.19 0.23 0.2 0.21 0.18 0.27 52.7 62 8.11 13.89 Er 0.56 0.68 0.59 0.62 0.52 0.78 1.76 2.05 7.61 24.29 Tm 0.09 0.11 0.095 0.1 0.088 0.13 5.32 6.5 9.98 20.26 Yb 0.65 0.76 0.65 0.77 0.59 0.9 1.03 1.06 1.44 26.87 Lu 0.11 0.12 0.11 0.13 0.097 0.14 6.99 7.4 2.85 19.84 Y 5.8 6.69 6.03 5.66 5.59 8.04 1.1 1.15 2.22 26.53 ΣREE 49.53 61.49 58.955 54.44 47.515 76.63 - - - - Sr/Y 142 103 146 126 114 110 - - - - δEu 1.73 1.57 1.72 1.58 1.8 1.31 - - - -
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表 3 朝阳地侵入岩Sr-Nd同位素组成
Table 3. Sr-Nd isotopic compositions of Chaoyangdi intrusive rocks
样品 87Rb/86Sr 87Sr/86Sr 2σ (87Sr/86Sr)i 147Sm/144Nd 143Nd/144Nd 2σ (143Nd/144Nd)i εNd(t) TDMC(Ma) 15YS12 0.203 905 0.707 643 6 0.706 519 0.117 081 0.511 483 7 0.511 186 -18.6 2 642 15YS13 0.253 640 0.707 674 5 0.706 276 0.111 840 0.511 481 7 0.511 197 -18.4 2 626 15YS14 0.211 674 0.707 545 7 0.706 378 0.107 175 0.511 482 6 0.511 210 -18.2 2 606 15YS15 0.270 703 0.708 021 6 0.706 529 0.106 541 0.511 494 4 0.511 224 -17.9 2 584 15YS17 0.200 447 0.707 638 7 0.706 534 0.114 092 0.511 481 3 0.511 192 -18.5 2 633 15YS18 0.171 117 0.707 553 7 0.706 610 0.105 075 0.511 470 4 0.511 204 -18.3 2 616
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表 4 朝阳地侵入岩锆石Hf同位素组成
Table 4. Zircon Hf isotopic compositions of Chaoyangdi intrusive rocks
No. t(Ma) 176Yb/177Hf 176Lu/177Hf 176Hf/177Hf 2σ εHf(t) 2σ TDMC(Ma) fLu/Hf 2 400 0.030 536 0.001 203 0.281 788 0.000 017 -26.7 0.6 3 039 -0.96 3 394 0.031 291 0.001 223 0.281 753 0.000 017 -28.1 0.6 3 120 -0.96 4 384 0.029 097 0.001 067 0.281 819 0.000 019 -25.9 0.7 2 978 -0.97 7 390 0.066 219 0.002 441 0.281 860 0.000 021 -24.7 0.7 2 905 -0.93 8 393 0.029 832 0.001 065 0.281 807 0.000 022 -26.1 0.8 2 999 -0.97 9 386 0.023 872 0.000 808 0.281 466 0.000 029 -38.3 1.0 3 745 -0.98 13 385 0.023 579 0.000 941 0.281 799 0.000 018 -26.6 0.6 3 020 -0.97 14 379 0.031 442 0.001 161 0.281 891 0.000 016 -23.5 0.6 2 825 -0.97 15 385 0.025 350 0.001 005 0.281 777 0.000 022 -27.4 0.8 3 069 -0.97 16 384 0.038 599 0.001 452 0.281 827 0.000 024 -25.7 0.8 2 966 -0.96 18 383 0.034 149 0.001 240 0.281 824 0.000 023 -25.8 0.8 2 969 -0.96 19 390 0.042 098 0.001 537 0.281 872 0.000 024 -24.0 0.8 2 865 -0.95 注：Hf同位素计算所用的参数有：(176Lu/177Hf)CHUR=0.033 2，(176Hf/177Hf)CHUR, 0=0.282 772，(176Lu/177Hf)DM=0.038 4，(176Hf/177Hf)CHUR, 0=0.283 25，衰变常数λ=1.867×10-11，fDM=0.16，fCC=-0.55.
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