The Ming deposit has a complex ore mineralogy that is shown in Table 3, along with mineral formulas and occurrences. Microscopically, recrystallized pyrite, galena, and especially in the 1806 Zone tennantite – tetrahedrite occur as minor (5 – 10 vol.%) to trace ( b 5 vol.%) phases within sphalerite bands. In the 1806 Zone thick sphalerite bands are common, whereas thin, mm-scale schlieren occur in other orebodies. Sphalerite bands (0.5 – 30 cm) and schlieren (1 – 5 mm) of varying thickness commonly occur within a pyritic – chalcopyritic matrix in the upper parts of the 1807, 1806, and Ming South orebodies (Table 2). Semi-massive to massive sul fi des occur in the 1807, 1806, and Ming South orebodies and consist predominantly of pyrite ± chalcopyrite with minor sphalerite ± pyrhhotite. The several hundred meter thick LFWZ orebody is made up entirely of this sul fi de mineralization style therefore, the term LFWZ is used synonymously for both the orebody and the mineralization style herein. In contrast, discordant stringers in the Lower Footwall Zone (LFWZ) consist of chalcopyrite – pyrrhotite ± pyrite ± cubanite in an in- tensely chlorite altered footwall, and are transposed into the main foliation. Sul fi de stringers in the rhyodacitic footwall are made of pyrite – chalcopyrite ± sphalerite ± pyrrhotite, run predominantly parallel to foliation within a sericite footwall and occur as a horizon, up to 100 m thick, immediately below the 1806 Zone and Ming South orebodies. thin quartz altered horizon immediately above semi-massive and massive sul fi des (i.e., silici fi ed horizon) in the 1806 Zone. (C) – (D) Simple textures of tellurides: (C) Very small crystal of Bi-telluride with altaite in chalcopyrite and (D) Hessite with inclusions of Bi-telluride and clausthalite (E) – (J) Occurrences of electrum in the LFWZ: (E) Re fl ected light (RL) image of submicroscopic electrum between recrystallized pyrite that are partly replaced and surrounded by pyrrhotite (F) Back-scattered electron (BSE) image of (E) showing submicroscopic electrum and galena between recrystallized and partly replaced pyrite (G) RL image of coarse-grained, recrystallized pyrite that is partly replaced by pyrrhotite submicroscopic electrum occurs in pyrrhotite replacing pyrite (H) BSE image of (G) showing submicroscopic electrum in pyrrhotite that replaces coarse-grained, recrystallized pyrite along fractures (I) RL image of recrystallized arsenopyrite on pyrrhotite submicroscopic electrum occurs between and along fi ne fractures in arsenopyrite and (J) BSE image of (I) showing submicroscopic electrum and galena between and along thin fractures in recrystallized arsenopyrite. (A) – (B) Textural relationships between pyrrhotite – chalcopyrite – cubanite – pyrite: (A) Replacement of pyrite by pyrrhotite and (B) High temperature cubanite laths in chalcopyrite partly overgrown by pyrrhotite. Solid trajectory lines indicate that a mineral texture is abundant, whereas dashed trajectory lines indicate a rare abundance of a texture. Minerals forming ore textures are connected to the different textures by trajectories. Textures of metal sul fi des, tellurides, and electrum in the LFWZ.

Metallic texture cd