The Shizhuyuan oxidized skarn-greisen W–Sn deposit (South China) has widely developed scheelite in the prograde skarn stage, retrograde skarn stage, oxide stage, sulfide-quartz vein stage, greisen stage, and quartz-calcite-fluorite vein stage that are related to the reduced A-Type Qianlishan granite. In this contribution, we used trace elements, oxygen isotopic compositions, and U–Pb isotopes for tracing the W metallogenic processes in skarn and greisen, and the genesis of the Shizhuyuan W–Sn deposit. The total rare-earth element (∑REE) contents of scheelite grains from prograde and retrograde skarn stages to oxide stage show a decreasing fractionation trend (means from 1647 to 181 ppm) and the increasing trend in sulfide-quartz vein stage and greisen (mean = 428 ppm and 2074 ppm) indicate multi-stage fluid activities. Scheelites formed in skarn show HREE depletion REE patterns (La_N/Yb_N values means from 159 to 1.40) which results from paragenetic mineral precipitation (e.g., garnet and diopside), and negative or small positive Eu anomaly. In contrast, scheelite grains from the greisen stage have a flat REE pattern and a pronounced negative Eu anomaly identical to those of the Qianlishan granite that mirror the magmatic-hydrothermal fluid. The MoO₃ contents in scheelite decrease from the prograde and retrograde skarn stages through the oxide stage to the sulfide-quartz vein stage (mean = 27.4 wt%, 1.97 wt%, 0.51 wt%, and 0.12 wt%). However a slight rise in MoO₃ contents was observed in scheelite grains from the greisen to the latest-stage quartz-calcite-fluorite vein stage (mean = 0.28 wt% and 0.52 wt%, respectively). It is suggested to be the result of a change in fluid fO₂ conditions and periodic transition from oxidizing to reducing metallogenic environment.

The mean δ¹⁸O_H2O values of the ore-forming fluid in the different mineralization stages as calculated by δ¹⁸O_scheelite are 7.98 ‰ (prograde skarn), 6.20 ‰ (retrograde skarn), 4.96 ‰ (proximal greisen), 2.83 ‰ (distal greisen), and 3.29 ‰ (quartz-calcite-fluorite vein). Scheelite grains formed in the retrograde skarn stage yielded a U–Pb isochron age of 164.4 ± 7.6 Ma, which is within the uncertainty of the emplacement age of the Qianlishan granite. Although scheelite grains formed in different stages have different trace elements and oxygen isotope compositions, they are all associated with the Qianlishan granite. We assume that the giant skarn-greisen W–Sn deposit has mainly resulted from multistage fluid activities derived from reduced intrusions and long-term fluid-rock interactions with thick marbleized limestone in an oxidizing setting.

石竹园氧化矽卡岩-云英岩W-Sn矿床（华南）广泛发育顺行矽卡岩期、逆行矽卡岩期、氧化物期、硫化物-石英脉期、云英岩期、石英-方解石-萤石脉期白钨矿与还原的A型千里山花岗岩有关。在本文中，我们使用微量元素、氧同位素组成和 U-Pb 同位素来追踪矽卡岩和云英岩中的 W 成矿过程，以及石竹园 W-Sn 矿床的成因。从顺行和逆行矽卡岩阶段到氧化物阶段，白钨矿颗粒的总稀土元素（∑REE）含量呈现出分馏下降的趋势（平均从1647到181 ppm）和硫化物石英脉阶段和云英岩的增加趋势（平均= 428 ppm 和 2074 ppm) 表示多级流体活动。_N /Yb _N值是指从 159 到 1.40)，这是由共生矿物沉淀（例如，石榴石和透辉石）和负或小正 Eu 异常引起的。相比之下，云英岩阶段的白钨矿颗粒具有平坦的 REE 模式和明显的负 Eu 异常，与反映岩浆热液的千里山花岗岩相同。白钨矿中的MoO ₃含量从顺行和逆行矽卡岩阶段通过氧化物阶段到硫化物-石英脉阶段降低（平均值= 27.4 wt％，1.97 wt％，0.51 wt％和0.12 wt％）。_{然而，MoO 3}略有上升在从云英岩到最新阶段的石英-方解石-萤石脉阶段的白钨矿颗粒中观察到含量（平均值分别为 0.28 wt% 和 0.52 wt%）。这被认为是流体f O ₂条件变化和从氧化到还原成矿环境周期性转变的结果。

δ ¹⁸ O白钨矿计算的不同成矿阶段成矿流体δ ₁₈ ^O H2O_平均值分别为 7.98 ‰（顺行矽卡岩）、6.20 ‰（逆行矽卡岩）、4.96 ‰（近端云英岩）、2.83 ‰（远端云英岩）和 3.29 ‰（石英-方解石-萤石脉）。逆行矽卡岩阶段形成的白钨矿颗粒产生的 U-Pb 等时线年龄为 164.4 ± 7.6 Ma，处于千里山花岗岩侵位年龄的不确定范围内。不同时期形成的白钨矿颗粒虽然微量元素和氧同位素组成不同，但都与千里山花岗岩伴生。我们假设巨大的矽卡岩-云英岩 W-Sn 矿床主要是由多阶段流体活动产生的，这些流体活动源于氧化环境中减少的侵入和与厚大理石化石灰岩的长期流体-岩石相互作用。