Paragenesis and fluid evolution of the Halasu III porphyry Cu deposit, East Junggar (NW China): Implications for the Paleozoic multiphase superimposing mineralization in the Central Asian Orogenic Belt

The Halasu III deposit, an important Cu deposit in the southernmost part of the Halasu porphyry Cu belt, is situated in the East Junggar block in NW China. Copper and Mo sulfide mineralization commonly occurs as disseminations or veinlets, and is mainly associated with Devonian granodiorite porphyry. Our detailed field geological investigation identified late-stage high grade Cu sulfide-bearing veining superimposed on the earlier porphyry Cu-Mo mineralization. Four hydrothermal alteration and mineralization stages were identified, namely the early epidote alteration (Stage I), porphyry-style alterations (Stage II comprising II-A potassic, II-B propylitic and II-C phyllic alteration sub-stages), late veining (Stage III) and supergene processes (Stage IV) in the northern- and southern mineralization zones at Halasu III. Multiphase granodiorite- and alkali granite dykes intruded the Beitashan Formation volcanic rocks, generating the early epidote alteration. Potassic alteration (Stage II-A) occurred in and around the NNW-treading granodiorite dykes, while the propylitic alteration (Stage II-B) occurred in the intrusions or volcanic wall rocks around the potassic zone. These early alteration assemblages were overprinted by the subsequent, structurally-controlled phyllic alteration (Stage II-C) confined within the granodiorite porphyry. Late veins (Stage III) include sulfide-bearing (Stage III-A) and sulfide-barren (Stage III-B) ones. Supergene process (Stage IV), represented by hematite and jarosite replacing primary sulfides, extends tens of meters down depth and is commonly fracture-controlled. Three fluid inclusion (FI) types were recognized, namely Type A (single-phase), B (liquid-vapor two-phase) and C (liquid-vapor-solid three-phase). For Type B FIs, those of potassic alteration homogenized at 183-347 degrees C, with corresponding salinities of 6.2-17.8 wt.% NaCl equiv. The propylitic and phyllic Fls homogenized at 172-425 T and 231-352 degrees C, respectively, with the corresponding salinities of 0.9-14.0 wt.% NaCl equiv. and 0.4-10.5 wt.% NaCl equiv. The sulfide-bearing vein Fls homogenized at 243-410 degrees C (Stage III-A-1), 260-362 degrees C (Stage III-A-2) and 117-235 degrees C (Stage III-A-3), along with the corresponding salinities of 1.9-9.2 wt.% NaCl equiv., 1.1-6.7 wt.% NaClequiv. and 65-17.1 wt.% NaCl equiv., respectively. The sulfide-barren vein FIs yielded homogenization temperatures of 260-380 T (Stage III-B-1) and 114-297 T (Stage III-B-2), with corresponding salinities of 1.7-9.8 wt.% NaCl equiv. and 0.2-13.6 wt.% NaCl equiv., respectively. We suggest that hydrothermal veins at Halasu III may have undergone complex and superimposing alteration due to the episodic reopening of the preexisting veins, with Stage III-A-3 veining overprinting the phyllic alteration and Stage III-A-2 veining. Stage Ill-B-2 veining superimposed on the potassic alteration, as well as on Stages III-A-1 and III-B-1 veining. Paragenetic sequence and fluid evolution at Halasu III indicate that these complex hydrothermal alteration stages were formed in accordance with the regional tectonic evolution. These various alteration and mineralization stages at Halasu III deposit reveal a prolonged history of magmatic and hydrothermal processes extending episodically from the Middle Devonian to Middle Permian, wherein early mineralization was overprinted by late hydrothermal events. Such superimposed mineralization may occur commonly in the Paleozoic Central Asia Orogenic Belt. (C) 2016 Elsevier B.V. All rights reserved.