Abstract Celadonite is the most abundant K-rich hydrated mineral formed during basalt alteration. In convergent margins, celadonite from the altered oceanic crust sinks into the mantle and contributes to the mantle wedge metasomatism, recorded by incompatible element enrichment in lavas and mantle xenoliths samples from these settings. However, experimental data on the role of celadonite in subduction zones as a function of P-T are still scarce. Therefore, celadonite stability under “hot” and “cold” subduction settings is investigated experimentally in this study. Results show an early silica loss, with quartz/coesite replacing celadonite from 400 to 600 °C and 2.5–7.7 GPa. At 700 °C and 2.5 GPa, celadonite is partially converted to phlogopite-annite, and at 800 °C and 4.0 GPa celadonite is absent. At temperatures above 800 °C, enstatite and phlogopite are the stable silicate phases from 2.5 to 7.7 GPa. Mossbauer spectroscopy and X-ray diffraction analyses show that the reaction of celadonite to phlogopite-annite is progressive and controlled by the Fe3+ to Fe2+ reduction in the octahedral site. Coupled to this, there is a transition of pyrite to pyrrhotite and the release of reducing fluids enriched in H2S, SiO2, OH− and K+ in the mantle wedge. These fluids have the potential to mobilize chalcophile elements (e.g. Cu, Zn) and act as mineralizing agents in shallower and more oxidizing crustal environments. Data in this study demonstrate that celadonite-phlogopite-annite series minerals are stable down to at least 230 km in the mantle, contributing to the sources of mantle metasomatism, arc-related magma genesis and possibly chalcophile mineralization.

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青瓷在俯冲环境中对地幔交代作用的作用

摘要 青瓷是玄武岩蚀变形成的最丰富的富钾水合矿物。在会聚边缘，来自改变的洋壳的青瓷沉入地幔并促成地幔楔交代作用，由来自这些环境的熔岩和地幔捕虏体样品中不相容的元素富集记录。然而，关于青瓷在俯冲带中作为 PT 函数的作用的实验数据仍然很少。因此，本研究通过实验研究了“热”和“冷”俯冲环境下青瓷的稳定性。结果显示早期二氧化硅损失，石英/柯石英在 400 至 600 °C 和 2.5-7.7 GPa 之间取代了青瓷。在 700 °C 和 2.5 GPa 条件下，青瓷部分转化为金云母-花岗岩，而在 800 °C 和 4.0 GPa 条件下，青瓷不存在。在温度高于 800 °C 时，顽火石和金云母是 2.5 到 7.7 GPa 的稳定硅酸盐相。穆斯堡尔光谱和 X 射线衍射分析表明，青瓷向金云母-安妮特的反应是渐进的，并受八面体部位 Fe3+ 向 Fe2+ 还原的控制。与此相伴的是，黄铁矿向磁黄铁矿转变，并且在地幔楔中释放出富含 H2S、SiO2、OH− 和 K+ 的还原流体。这些流体有可能调动亲硫元素（例如铜、锌）并在更浅和更氧化的地壳环境中充当矿化剂。这项研究中的数据表明，青瓷-金云母-安妮特系列矿物在地幔中至少稳定在 230 公里处，有助于地幔交代作用、与弧相关的岩浆成因和可能的亲硫矿化的来源。