Hydrothermal rare earth elements mineralization in the Barra do Itapirapuم carbonatite, southern Brazil: behaviour of selected trace elements and stable isotopes (C, O)

The Barra do Itapirapuã carbonatite is located in southern Brazil and belongs to the Cretaceous Ponta Grossa alkaline–carbonatitic province related to the opening of the South Atlantic. The carbonatite complex is emplaced in Proterozoic granites and is mainly composed of plutonic magnesio- to ferrocarbonatite, with smaller amounts of subvolcanic magnesiocarbonatite. Hydrothermal alteration of the carbonatite has led to the formation of quartz, apatite, fluorite, rare earth fluorocarbonates, barite and sulfides in variable proportions. Trace element data, δ13C and δ18O are presented here, with the aim of better understanding the geochemical nature of hydrothermal alteration related to rare earth elements (REE) mineralization. The non-overprinted plutonic carbonatite shows the lowest REE contents, and its primitive carbon and oxygen stable isotopic composition places it in the field of primary igneous carbonatites. Two types of hydrothermally overprinted plutonic carbonatites can be distinguished based on secondary minerals and geochemical composition. Type I contains mainly quartz, rare earth fluorocarbonates and apatite as hydrothermal secondary minerals, and has steep chondrite normalized REE patterns, with ΣREE+Y of up to 3 wt.% (i.e., two orders of magnitude higher than in fresh plutonic samples). In contrast, the Type II overprint contains apatite, fluorite and barite as dominant hydrothermal minerals, and is characterized by heavy REE enrichment relative to the fresh samples, with flat chondrite normalized REE patterns. Carbon and oxygen stable isotope ratios of Types I and II are elevated (δ18O +8 to +12‰; δ13C −6 to −2‰) relative to the fresh samples. Hydrothermally overprinted carbonatites exposed to weathering show even higher δ18O values (δ18O 13 to 25‰) but no additional REE enrichment. The subvolcanic carbonatite has anomalously high δ13C of up to +1‰, which suggests crustal contamination through interaction with carbonate-bearing metasediments.