Progress in Subduction-Related Boninite Research
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摘要: 玻安岩（Boninite）是一种特殊的镁铁质火山岩，主要形成于与板块俯冲相关的特殊地质环境，是俯冲起始的直接地质记录. 其斑晶矿物组合以橄榄石和辉石为主，不含斜长石，具有高Mg和Si含量、低Ti含量，富集大离子亲石元素和轻稀土元素，亏损高场强元素和中稀土元素. 典型的玻安岩呈特殊的“U”型稀土元素配分模式. 玻安岩的特殊化学成分反映了其地幔熔融的特殊条件，如高温、低压和相对富水的环境. 初始岩浆形成涉及地幔的二次熔融过程，发生在地幔经历初次熔融并亏损之后. 这种特殊的熔融过程为揭示地幔源区组成、熔融程度及流体在地幔熔融和俯冲起始过程中的作用提供了重要信息. 本文回顾了俯冲带玻安岩的矿物学、地球化学特征及岩石成因机制，总结了其深部动力学和岩浆演化过程，并探讨其对地球动力学领域的重要意义. 最后，还探讨了当前研究中的问题及未来可能的研究方向.Abstract: Boninite is a special type of magnesium-iron volcanic rock, primarily formed in unique geological environments associated with plate subduction. It serves as a direct geological record of the subduction initiation. The phenocryst are mainly olivine and pyroxene, with no plagioclase. Boninite is characterized by high Mg and Si, but lower Ti content. They are also and enriched in large ion lithophile elements (LILEs) and light rare earth elements (LREEs), but depleted in high field strength elements (HFSEs) and medium rare earth elements (MREEs). Typicalboninite exhibits a distinctive "U"-shaped rare earth element (REE) distribution pattern.The unique chemical composition of boninite reflects its uniquemantle melting conditions, such as high temperature, low pressure, and relatively high water content.Primarymagma was generated throughre-melting processes in the mantle source, which has already undergone partial melting before. This unique melting process provides crucial insights into mantle source composition, degree of melting, and the role of fluids in mantle melting and the initiation of subduction.In this review, we discuss the mineralogy, geochemical characteristics, and petrogenetic mechanisms of subduction-related boninite, emphasizing its significance in geodynamics and magma evolution processes. Finally, we also summarized the current research issuesand potential future directions in boninite studies.
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Key words:
- boninite /
- geochemistry /
- petrogenesis /
- mantle melting /
- subduction initiation /
- subduction zone
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图 1 全球玻安岩分布图
玻安岩数据来自GEOROC数据库（
https://georoc.eu/ ）Fig. 1. Map of global boninites distribution
图 2 使用Pearce and Reagan(2019)的方法和划分定义的玻安岩分类图
玻安岩数据来自GEOROC数据库（
https://georoc.eu/ ）Fig. 2. Boninite classification plots using methods and division definitions from Pearce and Reagan (2019)
图 3 IODP 352钻探在Bonin弧前外侧获得的玻安岩显微照片（正交偏光）
修改自Pearce and Arculus（2021）；a. 低硅玻安岩以橄榄石为主，斜方辉石次之，基质以单斜辉石和斜长石微晶为主；b. 高硅玻安岩的斑晶是斜方辉石和少量橄榄石，基质主要是斜方辉石和单斜辉石微晶
Fig. 3. Photomicrograph of boninites obtained from IODP Expedition 352 in the Bonin outer forearc (orthogonal polarized light)
图 4 IODP 352航次玻安岩及其相关岩石玻璃原始地幔标准化微量元素图
原始地幔值来自Sun and McDonough (1995)，LSB和HSB富集大离子亲石元素（如Rb、Ba、Sr），流体不易迁移元素（如Zr和Hf），亏损Nb等高场强元素，高硅玻安岩总体含量较高，数据源自Reagan et al.(2023).
Fig. 4. Primitive mantle normalized concentrations of incompatible trace elements in boninite glasses and associated rock glasses from IODP Expedition 352
图 5 不同区域的玻安岩的球粒陨石归一化稀土元素模式图
球粒陨石归一化值来自Sun and McDonough（1989）；数据来源于：Bloomer and Hawkins（1987）；Srivastava（2006）；Cluzel et al.（2016）；Golowin et al.（2017a）；Reagan et al.（2017）；Woelki et al.（2018）；Pearce and Arculus（2021）；Zhao et al.（2021）；图中展示的数据均为各个区域玻安岩的平均成分
Fig. 5. Normalized rare-earth element models of chondrites from bonintes from many regions
图 6 不同系列玻安岩的206Pb/204Pb和207Pb/204Pb图
玻安岩数据来自GEOROC数据库（
https://georoc.eu/ ）Fig. 6. 206Pb/204Pb and 207Pb/204Pb maps of different series of boninites
图 7 玻安岩成因机制图
修改自Pearce and Arculus（2021）；第一阶段熔融地幔源区为含有橄榄石、斜方辉石和单斜辉石的二辉橄榄岩，这一熔融阶段产生玄武岩熔体且留下的残余物中单斜辉石含量很少（< 5%）. 此阶段熔体保持单斜辉石饱和. 第二阶段熔融，在流体输入、高温或减压作用下，更深的地幔残留物再次熔融. 起初产生的仍是单斜辉石饱和的玄武岩熔体（成分A），但随着单斜辉石亏损，生成Si、Mg含量高且不含单斜辉石的熔体（成分B）
Fig. 7. Diagram illustrating the mechanisms of boninite genesis
图 8 IODP 352航次U1439C孔和U1442A孔岩芯玻安岩岩浆混合证据
引自Shervais et al.（2021）；a~c. U1439C岩浆混合结构：a. 浅色HMA与深色LSB混合；b.浅色的低铬HMA与深色的高铬LSB的冷却边缘接触；c. 浅色HMA与深色LSB混合；d. Cr含量相近的HSB岩浆呈尖形接触：深色熔体斑晶较多，浅色熔体边缘玻璃化，厚约5 mm，内部玻璃化较少；e. TS195薄片（f图中的虚线矩形位置，TS195为薄片名称）的放大图像，两个HSB熔体之间的呈尖状接触；f. 玻璃碎屑角砾岩与玻安岩碎屑混合；HSB.高硅玻安岩；HMA.高镁安山岩；LSB.低硅玻安岩
Fig. 8. Evidence of boninitic magma mixing in core samples from Holes U1439C and U1442A of IODP Expedition 352
图 9 西太平洋IBM地区玻安岩成因模型图
修改自Reagan et al. (2017)；Pearce and Arculus(2021)；(1).展示了太平洋板块与原菲律宾海板块之间转换断层的俯冲前状态; (2).因古老且冷太平洋板块下沉和回撤，导致上覆原菲律宾海板块发生伸展作用，引发海底扩张，并产生弧前玄武岩，导致地幔变亏损; (3).俯冲带释放流体和熔体交代亏损地幔使其再富集. 流体和熔体从俯冲板片中释放出来进入上地幔，导致亏损的地幔发生再富集作用; (4).地幔再富集作用降低了残余地幔的固相线，导致第二阶段熔融，有利于形成LSB成分的洋壳; (5).随着板片回撤的减缓，海底扩张停止，开始平行于板片的俯冲（slab-parallel），但新大洋岩石圈下的第二阶段熔融持续，形成含有HSB的初生岛弧; (6).俯冲完全建立后，新的、未亏损的地幔进入地幔楔，正常的岛弧岩浆活动开始. PPS（Proto-Philippine Sea）.原始的菲律宾海; PAC（Pacific）.太平洋
Fig. 9. Diagrammatic model illustrating the genesis of boninites in the IBM region of the Western Pacific
表 1 典型玻安岩的主量元素含量和分类
Table 1. Major element contents and classification of typical boninites
地点 1 2 3 4 5 6 7 8 子类型 HSB HSB HSB HSB HSB LSB LSB LSB low-Ca Type 1 low-Ca Type 1 low-Ca Type 2 low-Ca Type 2 low-Ca Type 3 high-Ca high-Ca high-Ca SiO2 61.11 57.19 58.80 56.26 58.01 54.03 55.61 52.44 TiO2 0.16 0.22 0.43 0.27 0.11 0.22 0.29 0.35 Al2O3 11.47 9.74 14.64 10.57 9.74 11.27 14.30 15.41 FeO 5.99 7.70 4.71 7.53 6.76 8.03 5.67 6.20 Fe2O3 1.50 1.93 1.18 1.77 1.69 2.01 1.42 1.55 MnO 0.13 0.17 0.12 0.17 0.14 0.18 0.16 0.15 MgO 11.57 15.84 9.70 14.86 15.43 13.99 9.22 9.07 CaO 5.11 4.68 6.48 6.17 6.69 9.40 11.82 13.22 Na2O 2.25 2.34 2.64 1.61 1.07 0.77 1.33 1.49 K2O 0.66 0.14 1.19 0.73 0.37 0.09 0.19 0.09 P2O5 0.04 0.04 0.10 0.06 0.01 0.02 0.00 0.04 total 100.00 100.00 100.00 100.00 100.00 100.00 100.00 100.00 Diagnostics CaO/ Al2O3 0.45 0.48 0.44 0.58 0.69 0.83 0.83 0.86 Ti8 0.18 0.27 0.45 0.32 0.13 0.26 0.30 0.36 Si8 62.05 59.24 59.24 58.06 59.95 55.60 55.93 52.72 注：地点信息：1.马里亚纳海沟（Bloomer and Hawkins，1987）；2.New Caledonia（ Cluzel et al.，2016 ）；3.日本西南部Setouchi带（Tatsumi et al.，2003 ）；4.Chichijima（Dobson et al.，2006 ）；5.Bushveld侵入体（Hatton and Sharpe，1989）；6.汤加北部Lau盆地（Falloon et al.，2008 ）；7.Troodos地块上部枕状熔岩（Cameron，1985）；8.Manihiki高原（Golowin et al.，2017a ）；氧化物含量以重量百分比（%）表示；分析数据中的总铁含量按FeO和Fe2O2（比例为4∶1）分配，并在分类前将总量调整为100%，以遵循IUGS制定的方案；高硅玻安岩（HSB）、低硅玻安岩（LSB）的定义依据Pearce and Reagan（2019）（见图 2）；高钙和低钙及其进一步细分为Type 1~3的分类见文章第三节；Ti8和Si8是将TiO2和SiO2值投影到MgO=8%的玻安岩下边界的结果，投影方法参考Pearce and Reagan（2019）
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