软流圈地幔成分不均一性的研究进展与意义

刘传周, 杨阳, 刘博达, 刘通. 2022. 软流圈地幔成分不均一性的研究进展与意义. 岩石学报, 38(12): 3712-3734. doi: 10.18654/1000-0569/2022.12.11
引用本文: 刘传周, 杨阳, 刘博达, 刘通. 2022. 软流圈地幔成分不均一性的研究进展与意义. 岩石学报, 38(12): 3712-3734. doi: 10.18654/1000-0569/2022.12.11
LIU ChuanZhou, YANG AlexandraYang, LIU BoDa, LIU Tong. 2022. Compositional heterogeneity of the asthenosphere: Advancement and implications. Acta Petrologica Sinica, 38(12): 3712-3734. doi: 10.18654/1000-0569/2022.12.11
Citation: LIU ChuanZhou, YANG AlexandraYang, LIU BoDa, LIU Tong. 2022. Compositional heterogeneity of the asthenosphere: Advancement and implications. Acta Petrologica Sinica, 38(12): 3712-3734. doi: 10.18654/1000-0569/2022.12.11

软流圈地幔成分不均一性的研究进展与意义

  • 基金项目:

    本文受国家杰出青年基金项目(42025201)资助

详细信息
    作者简介:

    刘传周, 1981年生, 研究员, 博士生导师, 主要从事地幔地球化学研究, E-mail: chzliu@mail.iggcas.ac.cn

  • 中图分类号: P542.5;P595

Compositional heterogeneity of the asthenosphere: Advancement and implications

  • 软流圈通常是指位于岩石圈之下、地幔过渡带之上的地幔圈层,可以发生长期缓慢变形,从而可以在全球范围内对流。软流圈是地球上岩浆岩的重要源区,并作为重要的参考体系广泛应用于讨论地球形成演化、壳幔相互作用、地壳生长等一系列重大地质问题。根据大洋玄武岩的研究结果,软流圈地幔被普遍认为具有相对均一的地球化学组成。然而,深海橄榄岩的元素与同位素组成却显示软流圈的成分存在强烈的不均一性。大量的研究显示软流圈中广泛残存有古老的再循环地幔,其来源既包括再循环的俯冲大洋岩石圈地幔,也包括通过不同方式进入软流圈的古老克拉通地幔。蛇绿岩的研究结果表明这种不均一性也同样存在于不同地质时期的软流圈地幔。本文通过总结洋中脊玄武岩、深海橄榄岩和蛇绿岩的相关研究,揭示软流圈地幔中不均一性的组成与来源,并讨论了它们对于软流圈在洋中脊下方熔融过程的影响。

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  • 图 1 

    全球N-MORB、D-MORB和E-MORB平均组成(数据来自Gale et al., 2013)

    Figure 1. 

    Trace elements of global N-MORB, D-MORB and E-MORD (data from Gale et al., 2013)

    图 2 

    东太平洋洋隆MORB的(La/Sm)NεNd随纬度的变化

    Figure 2. 

    Variations of (La/Sm)N and εNd of MORB along the latitude of the East Pacific Rise

    图 3 

    全球MORB的Sr-Nd-Pb-Hf同位素相关关系图

    Figure 3. 

    Sr-Nd-Pb-Hf isotope correlations of global MORB

    图 4 

    全球深海橄榄岩与弧前橄榄岩尖晶石Cr#-橄榄石Fo (数值来源于PetDB,www.earthchem.org/petdb.)

    Figure 4. 

    Olivine Fo versus spinel Cr# values of global abyssal peridotites and forearc peridotites (data from PetDB, www.earthchem.org/petdb.)

    图 5 

    全球深海橄榄岩单斜辉石REE配分图(数值来源于PetDB,www.earthchem.org/petdb.)

    Figure 5. 

    REE patterns of clinopyroxene in global abyssal peridotites (data from PetDB, www.earthchem.org/petdb.)

    图 6 

    全球深海橄榄岩单斜辉石(Sm/Yb)N-YbN(数值来源于PetDB,www.earthchem.org/petdb.)

    Figure 6. 

    Clinopyroxene (Sm/Yb)N ratios versus YbN contents of global abyssal peridotites (data from PetDB, www.earthchem.org/petdb.)

    图 7 

    全球深海橄榄岩单斜辉石与洋中脊玄武岩Sr-Nd-Hf同位素组成(数值来源于PetDB,www.earthchem.org/petdb.)

    Figure 7. 

    Sr-Nd-Hf isotope compositions of global MORB and clinopyroxene of global abyssal peridotites (data from PetDB, www.earthchem.org/petdb.)

    图 8 

    全球深海橄榄岩与洋中脊玄武岩εNd频谱图(数值来源于PetDB,www.earthchem.org/petdb.)

    Figure 8. 

    Histogram of εNd values of global abyssal peridotites and MORB (data from PetDB, www.earthchem.org/petdb.)

    图 9 

    软流圈地幔来源橄榄岩的187Os/188Os(a)和Re亏损年龄(b)频谱图(数值来源于PetDB,www.earthchem.org/petdb.)

    Figure 9. 

    Histogram of 187Os/188Os (a) and tRD ages of global asthenosphere-derived mantle peridotites (data from PetDB, www.earthchem.org/petdb.)

    图 10 

    雅江蛇绿岩地幔橄榄岩全岩MgO-Al2O3 (a)和MgO-CaO (b)

    Figure 10. 

    Whole-rock MgO vs. Al2O3 (a) and MgO vs. CaO (b) of the mantle peridotites from the Yarlung Tsangpo ophiolites

    图 11 

    雅江蛇绿岩地幔橄榄岩的橄榄石Fo-尖晶石Cr#(a)以及尖晶石Mg#-Cr#(b)

    Figure 11. 

    Olivine Fo vs. spinel Cr# (a) and spinel Mg# vs. Cr# (b) diagrams of the mantle peridotites from the Yarlung Tsangpo ophiolites

    图 12 

    新特提斯蛇绿岩地幔橄榄岩的Re-Os同位素组成及其与深海橄榄岩的统计学对比

    Figure 12. 

    Statistical comparisons of Re-Os isotopic distributions of the Neo-Tethyan ophiolitic peridotites and abyssal peridotites

    图 13 

    蛇绿岩地幔橄榄岩的Hf-Nd同位素协变图(a)以及Lu-Hf同位素等时线(b)

    Figure 13. 

    Covariations of Nd vs. Hf isotopes (a) and Lu vs. Hf isochrons (b) of global ophiolitic mantle peridotites

    图 14 

    洋中脊地幔熔融模型(据Liu and Liang, 2019)

    Figure 14. 

    Mantle melting model for mid-ocean ridges (after Liu and Liang, 2019)

    图 15 

    不均一地幔在洋中脊下上涌并发生部分熔融的示意图(据Liu and Liang, 2017b, 2020)

    Figure 15. 

    Schematic diagram showing the pseudo-2D ridge model for melting in an upwelling chemically heterogeneous mantle (after Liu and Liang, 2017b, 2020)

    图 16 

    化学不均一体随地幔上涌的演变(据Liu and Liang, 2017b)

    Figure 16. 

    Stretching and smearing of an enriched heterogeneity in an upwelling melting column (after Liu and Liang, 2017b)

    图 17 

    Nd-Hf同位素观测和地幔熔融模拟(据Liu and Liang, 2017b)

    Figure 17. 

    Nd-Hf isotope ratios and melting models(after Liu and Liang, 2017b)

    图 18 

    洋中脊玄武岩微量元素观测和地幔熔融模拟(据Liu and Liang, 2020)

    Figure 18. 

    Variations of trace element abundances in MORB and melt inclusions (a, after Laubier et al., 2012; White and Klein, 2014) and melting models considering the size of chemical heterogeneities and melt pooling area (b, after Liu and Liang, 2020)

    表 1 

    洋中脊地幔熔融和熔体汇聚模型

    Table 1. 

    Models of partial melting and melt segregation in mantle beneath mid-ocean ridges

    观测约束 洋中脊地幔熔融和熔体汇聚模型
    洋中脊下方只有化学平衡
    熔体通道1)
    洋中脊下方有深达30km
    化学不平衡熔体通道2)
    洋中脊下方有深达60km
    化学不平衡熔体通道2)
    野外 纯橄岩脉(cm-km宽) 有,但是千米级宽度
    岩石力学
    实验
    反应渗透熔体通道
    (Reactive Infiltration)
    剪切所致熔体通道
    地球
    物理
    洋壳厚度(~6km) 符合 符合 符合
    熔体分布中心50~60km 0~10km, 很浅 30km 60km
    地球
    化学
    深海橄榄岩稀土模式3)
    (230Th/238U)=1~1.4、
    (226Ra/230Th)=1~3.6、
    二者负相关
    二者正相关 (230Th/238U)=1~1.3、
    (226Ra/230Th)=1~1.8、
    二者负相关
    (230Th/238U)=1~1.3、
    (226Ra/230Th)=1~3.5、
    二者负相关
    注:1)化学平衡熔体运输模型, 如Weatherley and Katz (2016)Keller et al. (2017)Turner et al. (2017); 2)多种熔体汇聚模式的地幔熔融模型(Liu and Liang, 2019), 运输主要依靠熔体通道网络, 熔体通道内熔体与地幔残留体化学不平衡; 3)全球深海橄榄岩单斜辉石稀土含量数据由Warren (2016)整理, 含量归一化利用CI球粒陨石
    下载: 导出CSV
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收稿日期:  2022-06-22
修回日期:  2022-08-29
刊出日期:  2022-12-01

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