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Olivine-hosted Melt Inclusions in the Brahin Pallasite

We identified two types of melt inclusions in olivine crystals from the Brahin main-group pallasite, somewhat similar to those described in [1, 2]. Both types are relatively abundant and usually coexist within the same olivine grain. The first type are isolated, 1-10 µm large, elongated to tubular, and oriented along the [001] axis of the olivine host (as determined by EBSD). These inclusions are phosphate-rich, typically made of stanfieldite, a bubble, often phosphoran olivine (21-32 wt% P 2 O 5), plus occasional minute phases including metal-sulfide blebs or daubreelite. These isolated inclusions look primary, but microprobe mapping of P revealed the scars of former fractures joining these inclusions. The second type are 2-dimensional arrays of abundant chromite inclusions (<100 µm) and metal-sulfide assemblages (<50 µm). Typical metal-sulfide inclusions contain metal (kamacite and/or taenite) + troilite + phosphoran olivine (6-24 wt% P 2 O 5) + occasional minute grains of withlockite, shreibersite, daubreelite, and silica. These 2D arrays show the same morphological features that characterize secondary inclusions and healed fractures in olivine xenocrysts and other terrestrial minerals. Discussion: The phosphoran olivines are known in pallasites [3] but to our knowledge it is the first description of this mineral in inclusions. We identify this phase as olivine based on its steochiometry, (Mg,Fe,Ca) 4-x (Si 1-x P x) 2 O 8 , but its structure has not been ascertained so far. The value of 32 wt% P 2 O 5 is the highest of all P-rich olivines reported so far [3, 4, 5, 6]. Such high P contents suggest an extended solid solution between olivine and chopinite [7]. Melt inclusions in Brahin seem to record two distinct HT events. According to phase diagrams, a single silicate melt enriched in P might be sufficient to form these phosphate inclusions at T < 1200°C. On the contrary, at least two immiscible melts are required to form the secondary inclusions: a silicate-chromite melt and a metal-sulfide one. The abundance of chromite requires temperatures > ca. 1800°C in order to accommodate Cr in the silicate melt. It seems likely that these secondary inclusions result from a shock that took place while the stony-iron assembly of the Brahin pallasite was already formed. On the other hand, the lack of metal-sulfide associated with the phosphate-rich inclusions may imply that the iron part of the Brahin pallasite was not present when these inclusions were formed.