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    俯冲循环组分对大洋地幔不均一性的定量约束

    胡航 余星 韩喜球

    胡航, 余星, 韩喜球, 2022. 俯冲循环组分对大洋地幔不均一性的定量约束. 地球科学, 47(7): 2616-2630. doi: 10.3799/dqkx.2021.057
    引用本文: 胡航, 余星, 韩喜球, 2022. 俯冲循环组分对大洋地幔不均一性的定量约束. 地球科学, 47(7): 2616-2630. doi: 10.3799/dqkx.2021.057
    Hu Hang, Yu Xing, Han Xiqiu, 2022. Quantitative Constraints of Subduction Cycle Components on Oceanic Mantle Heterogeneity. Earth Science, 47(7): 2616-2630. doi: 10.3799/dqkx.2021.057
    Citation: Hu Hang, Yu Xing, Han Xiqiu, 2022. Quantitative Constraints of Subduction Cycle Components on Oceanic Mantle Heterogeneity. Earth Science, 47(7): 2616-2630. doi: 10.3799/dqkx.2021.057

    俯冲循环组分对大洋地幔不均一性的定量约束

    doi: 10.3799/dqkx.2021.057
    基金项目: 

    国家自然科学基金项目 42172231

    国家自然科学基金项目 41872242

    大洋“十三五”资源环境专项 DY135-S2-1-02

    自然资源部第二海洋研究所基本科研业务费专项 JT2001

    自然资源部第二海洋研究所基本科研业务费专项 JG2001

    详细信息
      作者简介:

      胡航(1997-),男,研究生,地球化学专业. ORCID:0000-0003-2305-9104. E-mail:huhang@sio.org.cn

      通讯作者:

      余星, E-mail: yuxing@sio.org.cn

    • 中图分类号: P542

    Quantitative Constraints of Subduction Cycle Components on Oceanic Mantle Heterogeneity

    • 摘要: 大洋地幔内部存在广泛的不均一性,其成因可有多种模式,其中俯冲循环作用对地幔组成的变化具有重要影响. 为明确各循环组分对亏损地幔的改造作用及其在富集源区中的相对贡献,系统总结了不同循环组分(远洋沉积物、俯冲洋壳、陆壳)的平均微量元素特征,计算了各循环组分在俯冲过程中经历的化学变化. 基于改造后的循环组分,开展与亏损地幔源区的混合和熔融模拟. 结果表明,HIMU型玄武岩可以由纯俯冲洋壳(≤10%)与亏损地幔(≥90%)混合形成的源区,经较低程度熔融(0.5%~1.5%)形成;而EMI型玄武岩可以由俯冲洋壳(≤10%)、俯冲剥蚀的下陆壳物质(≤3%)、亏损地幔(≥90%)混合形成的源区,经较低程度熔融(1%~2%)形成;EMII型玄武岩可以由俯冲洋壳(≤10%)、GLOSS-II(全球俯冲沉积物)或上陆壳物质(≤0.8%)与亏损地幔(≥90%)混合形成的源区,经较低程度熔融(1%~1.5%)形成.

       

    • 图  1  典型大洋玄武岩Sr-Nd-Pb同位素组成

      洋岛玄武岩及MORB同位素数据来源于Earthchem数据库

      Fig.  1.  Sr-Nd-Pb isotopic compositions of typical oceanic basalts

      图  2  俯冲循环模型:海底蚀变及俯冲脱水过程中的成分变化(据Bebout, 2007修改)

      Fig.  2.  Subduction cycle model: composition changes during seafloor alteration and subduction dehydration (modified after Bebout, 2007)

      图  3  不同洋壳组分及俯冲沉积物的微量元素含量对比

      Fig.  3.  Comparative diagrams of trace element contents in different oceanic crust components and subducted sediments

      图  4  洋岛玄武岩微量元素比值相关图(数据来源见图 1)

      Fig.  4.  Correlation of trace element ratios of oceanic island basalts(data source is shown in Fig. 1)

      图  5  玄武岩微量元素配分图和微量元素比值对比

      a.洋岛玄武岩数据为收集数据的平均值,N-MORB、E-MORB数据来自Sun and McDonough(1989);b. 元素比值为各类型洋岛玄武岩的平均值标准化到三种类型玄武岩的平均值

      Fig.  5.  Trace element pattern and comparison of trace element ratios in basalts

      图  6  定量模拟源区及熔体微量元素特征

      熔融模式为石榴石‒橄榄岩源区的分离部分熔融,DM组成来自Salters and Stracke(2004);微量元素的熔融分配系数来自Stracke et al.(2003)

      Fig.  6.  Quantitative simulation of trace elements in source and melt

      图  7  Ba/Nb-Rb/Nb元素比值及模拟趋势图和源区组成模式

      趋势线代表在恒定的熔融程度下(1%),源区中不同比例循环物质形成的玄武岩的元素特征

      Fig.  7.  The ration of Ba/Nb-Rb/Nb and modeled mixing trajectories and source region composition pattern

      表  1  不同循环组分的微量元素(10‒6)组成

      Table  1.   Trace element (10‒6) compositions of different cyclic components

      蚀变洋壳a 新鲜玄武岩b 大洋辉长岩c 全洋壳d 俯冲洋壳e 上陆壳f 下陆壳f GLOSS-IIg 俯冲沉积物
      Cs 0.153 0.014 08 0.018 77 0.051 0.025 4.9 0.3 4.9 2.79
      Rb 9.58 1.262 0.562 2.99 0.57 84 11 83.7 55.24
      Ba 22.6 13.87 9.5 13.87 6.59 628 259 786 534.48
      Th 0.07 0.187 1 0.155 2 0.142 0.088 10.5 1.2 8.1 5.59
      U 0.3 0.071 1 0.043 6 0.115 0.027 2.7 0.2 1.73 1.19
      Nb 1.22 3.507 1.695 2.03 1.95 12 5 9.42 6.97
      Ta 0.097 0.192 0.11 0.129 0.124 0.9 0.6 0.698 0.51
      La 1.84 3.895 4.79 3.83 1.68 31 8 29.1 22.12
      Ce 6.01 12.001 14.89 11.95 5.89 63 20 57.6 44.35
      Pb 0.240 4 0.489 0.601 0.48 0.09 17 4 21.2 18.44
      Nd 6.62 11.179 10.22 9.55 7.45 27 11 27.6 21.80
      Sr 115 113.2 157.8 136 81 320 348 302 163.08
      Zr 66.5 104.24 77.6 82 64 193 68 129 68.37
      Hf 1.92 2.974 2.12 2.28 1.78 5.3 1.9 3.42 1.88
      Sm 2.5 3.752 3.09 3.11 2.69 4.7 2.8 6 4.80
      Eu 0.91 1.335 1.14 1.13 1.04 1.0 1.1 1.37 1.10
      Ti 7 080 9 690 8 052 8 212 7 735 3 840 4 920 3 840 2 918.40
      Gd 3.65 5.007 4.1 4.24 4.03 4.0 3.1 5.81 4.71
      Dy 4.40 6.304 5.0 5.19 5.01 3.9 3.1 5.43 4.40
      Y 26.9 35.82 26.9 29.1 28.5 21 16 33.3 26.97
      Er 2.77 4.143 2.8 3.14 3.13 2.30 1.9 3.09 2.50
      Yb 2.69 3.90 2.77 3.03 2.99 1.96 1.5 3.01 2.44
      Lu 0.425 0.589 0.402 0.45 0.45 0.31 0.25 0.459 0.37
      Rb/La 5.21 0.324 0.117 0.781 0.339 0.263 0.032 0.277 0.339
      U/Pb 1.248 0.145 4 0.072 5 0.24 0.3 0.159 0.05 0.082 0.645
      Th/Pb 0.291 0.383 0.258 0.296 0.978 0.618 0.3 0.382 0.303
      Th/U 0.233 2.632 3.559 6 1.235 3.26 3.89 6.0 4.68 4.697
      注:a. 蚀变洋壳微量元素组成,数据来自Staudigel et al.(1995, 1996);b. 平均N-MORB微量元素组成,数据来自Hofmann(1988);c. 平均大洋辉长岩微量元素组成,数据来自Hart et al.(1999);d. 全洋壳组分由25%N-MORB、25%蚀变洋壳、50%辉长岩组成;e. 俯冲洋壳是在全洋壳的基础上经历俯冲脱水后的洋壳成分,元素活动性据Stracke et al.(2003);f. 平均上陆壳成分、下陆壳成分,数据源于Rudnick and Gao(2003);g. 全球俯冲沉积物数据源于Plank(2014), 俯冲沉积物成分根据Johnson and Plank(2000)的900 ℃元素活动性参数计算得出.
      下载: 导出CSV
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    • 收稿日期:  2021-03-10
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