Iron isotope fractionation during fluid metasomatism and ore-forming processes in magmatic-hydrothermal systems

Iron isotopes of magnetite have been used to unravel the sources and evolutionary processes of magma and ore deposits, but most studies have focused on bulk-rock samples, which possibly provide mixed information. Magnetite is susceptible to fluid-induced metasomatism, e.g., recrystallization and coupled dissolution-reprecipitation (CDR) processes in magmatic-hydrothermal systems, resulting in textural and chemical modification and re-equilibration. The behaviors of Fe isotopes during fluid metasomatism, however, are poorly understood. Magnetite from iron oxide-apatite (IOA) deposits commonly shows multi-generation and metasomatic textures, which have been suggested to form from magmatic melts/fluids to low-temperature hydrothermal processes. In this study, we carried out in situ Fe isotopic and chemical analyses on texturally constrained magnetite from ores and their hosting trachyandesite of the giant Luohe IOA deposit, eastern China, to assess the effect of fluid-assisted metasomatic processes on both chemical and Fe isotopic compositions, and to constrain the ore-forming processes. The ores contain three types of magnetite (Mag1, Mag2 and Mag3), all of which are texturally later than albite and diopside. Pristine Mag1 grains, formed at high temperatures (>700 degrees C), have ilmenite exsolution lamellae, and have lower Ti (0.61-1.55 wt%) but higher Ni/Cr ratios (mostly > 1) than those of magmatic magnetite (MagM) in the hosting trachyandesite. They also have delta Fe-56 values (0.12-0.52 parts per thousand) lower than those of MagM (0.54-0.65 parts per thousand), which overlap with those of high-temperature hydrothermal magnetite from iron-oxide copper-gold (IOCG), iron skarn, and porphyry Cu deposits, indicating that they were precipitated from hightemperature hypersaline fluids, as recorded by fluid inclusions within early-formed garnet, diopside, and coeval titanite. The heavy Fe isotope compositions of Mag1 are interpreted to be due to fluid exsolution under high temperatures and the preference of isotopically light Fe for earlier diopside (delta Fe-56 = 0.19 to 0.02 parts per thousand). Mag2 grains, which show triple junction textures, were formed through a fluid-induced recrystallization process at relatively lower temperatures (similar to 480 degrees C). They have delta Fe-56 values (0.29-0.53 parts per thousand) similar to those of Mag1 and previously reported high-temperature hydrothermal magnetite in other deposits. In contrast, Mag3 grains, which occur as rims on Mag1 grains, were formed via CDR at much lower temperatures (<300 degrees C). They have delta Fe-56 values (-0.15 to 0.22 parts per thousand) significantly lower than those of pristine Mag1 and overlap those of reported low-temperature hydrothermal magnetite. Decreasing formation temperatures from Mag1 to Mag3 are consistent with the decreasing trace element concentrations (Ti, Al, and V). Our study demonstrates that IOA deposits are formed from high-temperature hypersaline magmatic fluids and that the Fe isotopes of magnetite can be significantly modified during fluid metasomatism and ore-forming processes. Therefore, trace element and in situ Fe isotopic analyses on texturally well-constrained magnetite grains are crucial for determining the origin and evolution of magmatic-hydrothermal systems.