Fractionation Behavior of Stable Isotopes (Fe-K-Li-B-Ba) in Subducted Plates
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摘要: 俯冲带是壳幔循环的重要场所，K、Ba、B和Li作为流体活动性元素，富集在俯冲带流体中；同时各个储库的同位素差异使得其成为研究各种俯冲带流体的良好示踪剂. 总结了近年来有关俯冲带Fe同位素与俯冲带变质流体氧化还原状态的研究进展，以及K、Ba、Li和B同位素在俯冲各个阶段的地球化学行为，包括俯冲物质的同位素组成，俯冲板片变质流体的稳定同位素分馏，及俯冲板片物质再循环沉积物、蚀变洋壳及俯冲带蛇纹岩与上覆地幔楔的相互作用再循环过程中伴随的元素分配和稳定同位素分馏. 随着稳定同位素测试精度的提升和以上同位素在不同地质储库和地质过程的数据完善，可以更有助于理解俯冲带中的相关物理化学变化过程.Abstract: Subduction zones are important sites for recycled material, K, Ba, B and Li, as fluid-mobile elements, are enriched in melts and fluids. At the same time, the isotopic difference of each geochemical reservoir makes it a good tracer for studying various fluid in subduction zone. In recent years, research progresses of Fe isotopetracing the redox state of fluid in subduction zone and K, Ba, Li, B isotope behaviors in the subduction zone are summarized and stable isotopic behavior in a series of geochemical process, including isotopic composition of subducted materials, isotopic fractionation with dehydrated fluid during subduction, interactions between recycled sediments, altered oceanic crust and serpentinite and overlying mantle wedge and elements and stable isotope fractionation in subduction zones. With the improvement in measurement and the improvement of sample data in geochemical reservoir and geochemical sample, stable isotope is helpful to understand the physico chemical processes in subduction zones.
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Key words:
- stable isotope /
- subduction zone /
- isotopic tracing /
- crustal material recycled /
- geochemistry
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图 1 俯冲带中的K, Ba, B和Li同位素体系
K同位素数据来自Hu et al.(2020, 2021); Wang et al.(2020); Ba同位素数据来自Bridgestock et al.(2018); Li et al.(2019a); Nielsen et al.(2018, 2020)；B同位素数据来自Ryan and Chauvel(2014); Palmer(2017); Marschall and Foster(2018)；Li同位素数据来自Millot et al., (2004); Ottolini et al., (2004); Magna et al.(2006); Jeffcoate et al.(2007); Tang et al.(2007)
Fig. 1. Schematic illustration of K, Ba, B, Li isotope systematics in a subduction-zone setting
图 2 岛弧岩浆岩δ138Ba值与87Sr/86Sr (a)和206Pb/204Pb (b)的关系图
Ba，Sr，Pb同位素数据来源Nielsen et al.（2018，2020）；Wu et al.（2020）；地幔值来自Nielsen et al.，（2018），Li et al.（2019a）；蚀变洋壳值来自Wu et al.（2020）；沉积物值来自Plank and Langmuir.，（1998）；Bridgestock et al.（2018）；Nielsen et al.（2018，2020）
Fig. 2. δ138/134Ba data versus 87Sr/86Sr(a) and 206Pb/204Pb (b) of arc volcanic lavas
图 3 岛弧熔岩δ11B值与放射性同位素143Nd/144Nd (a), 87Sr/86Sr (b)的关系图
岛弧岩浆岩δ11B，143Nd/144Nd，87Sr/86Sr数据来源Ewart and Hawkesworth，（1987）；Woodhead（1989）；Ishikawa and Nakamura（1994）；Shibata and Nakamura（1997）；Ishikawa and Tera（1997，1999）；Taylor and Nesbitt（1998）；Ishikawa et al.（2001）；Straub and Layne（2002）；Rosner et al.（2003）；Leeman et al.（2004，2017）；Moriguti et al.（2004）；Barry et al.（2006）；Tonarini et al.（2007，2011），平均俯冲沉积物（GLOSS Ⅱ）值来自Plank（2014），弧前蛇纹石化地幔橄榄岩值来自Benton et al.（2004）；Savov et al.（2004，2005，2007）
Fig. 3. δ11B data versus143Nd/144Nd (a) and 87Sr/86Sr (b) of arc volcanic lavas
图 4 岛弧熔岩δ7Li值与1/[Li]关系图
数据来源Moriguti and Nakamura（1998）；Tomascak et al.（2002）；Tomascak（2004）；Magna et al.（2006）；Tang et al.（2013）；Hanna et al.（2020）；Liu et al.（2020b）
Fig. 4. Correlations between δ7Li and 1/[Li] of arc volcanic lavas
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