Ore-forming fluid source of the orogenic gold deposit: Implications from a combined pyrite texture and geochemistry study

Interpretation of bulk sulfur isotope data of the orogenic gold deposit is frequently hampered by complex zoning in pyrite, which calls for in-situ determination of sulfur isotope composition of sulfide minerals. The Qiuling gold deposit, located in Qinling orogen, is representative of orogenic type and selected here to further constrain the source of sulfur (and Au) and test the current popular ore genesis models for deposits of this type. Detailed backscattered electron imaging (BSE) study is applied to characterize intragrain texture, and subsequently in-situ sulfur isotope and trace element determination using secondary ion mass spectrometry (SIMS) and laser ablation-inductively coupled plasma-mass spectrometry (LA-ICP-MS) are used to reveal sulfur and metal source and evolution of the ore-forming fluid. Two generations of pyrite, i.e., pre-ore stage (Py1) and ore stage pyrite (Py2), were investigated in this study. In most cases, Py1 occurs as pyrite framboids, while Py2 as euhedral grains, in which Py2a as anhedral core, Py2b and Py2c as euhedral inner and outer rim, respectively. The δ34S values of both Py1 and Py2 have unusual wide ranges, i.e., a δ34S variation from −31.1 to +106.7‰ for Py1 (average +0.8‰) and from −2.7 to +24.1‰ for Py2 (average +13.2). The distribution pattern of δ34S values in Py1 is accommodated with Rayleigh fractionation in sulfate-restricted pore water. Modeling results show that neither temperature nor oxygen fugacity change could result the variations in δ34S values of Py2, and contribution of both preexisting pyrite and a pulse of ore-forming fluid with δ34S about +14.2‰ may be responsible for the observed variation in Py2. Such fluid may have been sourced from metamorphism of old strata such as the Neoproterozoic basement. Furthermore, Py2a shows an intimate relationship with Py1 in its δ34S values, indicating Py1 may have acted as part of sulfur source in the formation of Py2a. Py1 is rich in a suit of element such as Bi, Co, Mn, Ni, Tl and has the lowest As and Au. Py2a is similar with Py1 but with elevated As and Au. Py2b contains more abundant As and Au compared to Py2a. Py2c is rich in As and especially Au, but depleted in other elements compared to Py2a. The distribution pattern, coupled with sulfur isotope composition, indicates that Py2a was likely formed with a contribution of trace elements and sulfur from Py1 at the start of hydrothermal process. Py2b was formed with elevated proportion of contribution from t