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The structure and stability of hybrid lipid vesicles containing bilayer-encapsulated hydrophobic nanoparticles is dependent upon lipid phase behavior. By embedding stearylamine-stabilized gold nanoparticles in dipalmitoylphosphatidylcholine/dipalmitoylphosphatidylglycerol vesicles, we show that encapsulation at lipid to nanoparticle ratios from 10,000:1 to 5000:1 leads to bilayer thickening and hydrophobic mismatch, favoring nanoparticle inclusion in gel phase vesicles. High loadings lead to large increases in the gel to fluid melting temperature upon heating and significant hysteresis on cooling, which cannot be attributed solely to excess free ligand. This behavior is due to a cooperative effect of excess free SA ligand and nanoparticle embedment. Nanoparticle clustering was observed during lipid melting and could be reversed upon lipid freezing owing to lateral capillary forces within the bilayer. The impact of nanoparticle embedment on vesicle structure and properties at such low concentrations is reminiscent of hydrophobic proteins, suggesting that the underlying lipid biophysics between proteins and nanoparticle are similar and may provide a predictive design tool for therapeutic applications.

From integrated textural and compositional studies of auriferous and barren pyrite/marcasite in the epithermal Axi gold deposit, China, we have identified a relationship between multiple gold mineralizing events, mafic magma recharge, and fluid-rock reactions. Three generations of pyrite (Py1–3) and four generations of marcasite (Mar1–4) record episodic gold mineralizing events, followed by silver-copper-lead-zinc-cadmium enrichment. The gold mineralizing events are recorded by high concentrations of subnanometer-sized gold in Py1, Py3, and Mar3 (max. = 147, 129, and 34 ppm, med. = 39, 34, and 12 ppm). Based on previous Re-Os age determinations of pyrite and U-Pb zircon ages of the andesitic wallrock, these gold events slightly postdate pulsed mafic magma recharge and represent the incursion of Au-As-S-rich magmatic volatiles into circulating meteoric water. Silver-Cu-Pb-Zn-Cd enrichment in Py2, Mar2, and Mar4 are consistent with quiescent degassing and gradual Ag-Cu-Pb-Zn-Cd enrichment in an evolved felsic magma. Barren Mar1 records the dominance of meteoric water and a limited magmatic fluid contribution. High-Co-Ni-V-Cr-Ti contents in porous cores of Py1 and Mar2 are attributed to wall rock alteration and dissolution-reprecipitation. The results provide convincing evidence that the metal budget (especially for Au, Ag, Cu, Pb, Zn, Sb) of the hydrothermal fluids and sulfides in epithermal systems are controlled by the influx of magmatic fluids and associated magma, whereas the enrichment of certain fluid-immobile elements, such as Co, Ni, V, Cr, and Ti, is caused in part by fluid-rock interaction. [ABSTRACT FROM AUTHOR]

The process and mechanism of gold mineralization are frontier issues. The Dunbasitao deposit is the most important gold deposit discovered along the Armantai suture zone, East Junggar, NW China, which indicates the potential for future ore exploration in this area. Orebodies are mainly hosted in Lower Carboniferous Jiangbasitao Formation volcano-sedimentary rocks, and the ores are characterized by multistage pyrites. Based on microscopy and backscattered electron imaging studies, pyrites are classified into five types: the pre-ore framboidal/colloidal Py0; the early-stage coarse-grained, cubic, and homogeneous Py1; and the middle-stage fine-grained, cubic/pyritohedron Py2 that includes Py2a (core), Py2b (mantle), and Py2c (rim). The results of the EPMA and in situ LA-ICP-MS analyses show that trace elements of pyrite mainly occur in two forms: solid solutions and invisible or visible inclusions. Mn, Co, Ni, and As enter the pyrite lattice, whereas Ti occurs as mineral inclusions, and Au, Cu, Zn, Sb, and Pb can occur in both forms. Au and As show a positive linear relationship with r = 0.850. Py2b has much higher Au contents (20.1 to 201 ppm) than other pyrite types (Py0: 0.01 to 0.36 ppm; Py1: 0.01 to 0.02 ppm; Py2a: 0.31 to 2.48 ppm; and Py2c: 0.18 to 18.0 ppm). The Dunbasitao deposit is classified as an orogenic gold deposit using the two latest machine learning classifiers based on pyrite trace element data. Fluid immiscibility, sudden cooling, and the substitution of S1− with As1− might be crucial mechanisms leading to Au precipitation. Initial ore-forming fluids brought major amounts of As, Au, Co, Ni, Se, Zn, Ag, Cd, Sn, and other elements, and the Jiangbasitao Formation host rocks contributed a certain amount of As, Ni, Cu, Sb, Pb, and Bi, at least. [ABSTRACT FROM AUTHOR]

The Central Asian Orogenic Belt experienced a complex subduction accretion–collision history, forming the Irtysh gold belt. The Doranasai deposit is a typical gold deposit in the Irtysh gold belt, but its genesis is still unclear. The Doranasai gold deposit occurs in the east wing of the Aksay syncline. The orebodies are controlled by the NS-trending fault. The main ore types are quartz vein type and altered rock type. Wall rock alteration is represented by albitization, pyritization, sericitization, silicification, chloritization and carbonation. The ore-forming process includes three stages: albite–quartz–pyrite stage, quartz–polymetallic sulfide stage and barren quartz–carbonate stage. The fluid inclusions in the early- and middle-stage quartz are mainly aqueous inclusions and CO2–H2O inclusions, while only aqueous inclusions are developed in the late-stage quartz. The homogenization temperature of fluid inclusions has evolved from up to 300 °C in the early stage, 180–280 °C in the middle stage to lower than 200 °C in the late-stage, and the salinities have evolved from 4.2–9.6 wt% NaClequiv. in the early stage and 4.3–10.9 wt% NaClequiv. in the middle stage to 2.1–6.9 wt% NaClequiv. in the late stage. The coexistence of different types of inclusions in middle-stage quartz indicates that the fluid is not uniformly trapped, and fluid phase separation is the main mechanism of gold precipitation. The isotopic compositions of quartz from the Doranasai gold deposit show some variation but are generally comparable to those of other orogenic gold deposits. Fluids trapped in early-stage quartz have a δ18Owater range of 12.5–7.6‰, δD of − 101‰ and δ 13 C CO 2 of − 12.9‰, and the isotopic compositions of fluids trapped in middle-stage quartz have δ18Owater values of 11.4‰ to 4.4‰, δD of − 112‰ to − 102‰ and δ 13 C CO 2 of − 11.7‰ to − 9.5‰. In contrast, isotopic compositions of fluids trapped in late-stage quartz have δ18Owater values of 7.6‰ to 1.8‰, δD of − 108‰ to − 90‰ and δ 13 C CO 2 of − 12.4‰ to − 11.1‰. The early-stage fluids are probably derived from metamorphic decarbonation of the sedimentary host rock at depth, leading to the precipitation of barren quartz veins. In the middle stage, a decrease of the regional pressure and temperature may lead to the incorporation of meteoric water into the ore-forming system. Late-stage fluids trapped by calcite veins show isotopic compositions similar to meteoric water, indicating the cessation of hydrothermal fluid circulation. The geological and fluid inclusion characteristics of the Doranasai gold deposit are consistent with those of the orogenic gold deposit, indicating that it is an orogenic gold deposit formed in the collisional setting. [ABSTRACT FROM AUTHOR]

Scheelite, as a common accessory mineral found in hydrothermal deposits, is an indicator that allows the study of the ore-forming hydrothermal process and the tracing of fluid sources. The Doranasai gold deposit is a large-sized orogenic gold deposit in the South Altai, and orebodies occur as veins in the Devonian Tuokesalei Formation and Permian albite granite dykes. The ores are quartz veins and altered tectonites (rocks). Here, scheelite can be observed in the early-stage milky quartz veins, the middle-stage smoky quartz-polymetallic sulfide veins, and the altered albite granite dykes. In this study, the scheelites of these three types were carefully investigated in terms of texture, element, and isotope geochemistry to understand their ore-forming processes and fluid sources. The results showed that all types of scheelite were rich in Sr and poor in Mo, indicating that their ore-forming fluids had no genetic relation to magmatic–hydrothermal activities. The scheelites were characterized by the enrichment of medium rare earth element (MREE) and positive Eu anomaly in the chondrite-standardized REE patterns. This indicated the REE differentiation between scheelite and fluid, i.e., REE3+ and Na+ were in the form of valence compensation, preferentially replacing Ca2+ and selectively entering the scheelite lattice. The trace element composition of scheelite showed that the ore-forming fluid system was relatively closed, mesothermal, Na-rich, and reductive. The Sr isotope ratio of the scheelite (0.704819–0.70860, average 0.706372) was higher than that of the ore-bearing albite granite dyke (0.704654–0.704735), indicating that the Tuokesalei Formation is the main source for the fluids forming the Doranasai deposit. [ABSTRACT FROM AUTHOR]

Abstract: The Sawayaerdun gold deposit was discovered in the early 1990s and is the largest orogenic-gold deposit in the Chinese Tianshan. Gold mineralization occurs in quartz veins, which are hosted in carbonaceous metasediments and controlled by faults and fractures. Three major hydrothermal events can be identified at Sawayaerdun: An early barren quartz vein stage, middle stage quartz veins with pyrite and gold mineralization and late carbonate (–quartz) veins. Fluid inclusion studies of quartz, pyrite and carbonate formed during the major hydrothermal stages show distinct changes in fluid, temperature, composition and redox conditions occurred during fluid evolution. Three types of fluid inclusions have been identified at Sawayaerdun: H2O+NaCl (L+V), H2O+NaCl+CO2 (L+V) and CO2 (L+V). Fluids trapped in early barren quartz have high temperatures (280–420°C), low salinities (<3wt.% NaCl equiv.), high Cl− and are CO2-rich. Middle-stage quartz contains fluids with lower temperatures (210–310°C) and variable salinities (0.8–17.5wt.% NaCl equiv.). They are commonly S-rich, CO2-containing and relatively reduced compared with early stage fluids. In contrast, hydrothermal pyrite hosted in middle-stage quartz veins trapped fluids formed over a narrower temperature range (220–270°C), more oxidized (high CO2/CH4 ratio) and have higher Ca, K and Mg than fluids in quartz. Late stage carbonate is dominated by fluids with low temperatures (<200°C) and low contents of Cl, S and K. Fluid immiscibility probably commenced at the onset of mineralization along with middle-stage quartz formation, resulting in the generation of coexisting fluid inclusions with distinguishable vapor/liquid ratios and salinities. The compositional difference between fluids trapped in pyrite and quartz indicate fluid mixing may have occurred during the mineralization stage. The oxidized fluids, probably a mixture of meteoric water and fluids generated during water–host rock interaction, emerged into the ore-forming system to generate extensive metals precipitation. The fluid immiscibility and fluid mixing are most likely caused by pressure decrease during Late Paleozoic uplift and erosion in the Chinese Southern Tianshan area. Comparison of fluids between four major mineralization zones at Sawayaerdun indicate that zone II is similar to the most important zone IV and the order of similarity is probably zone II>XI>I, which could be applied to the future mineral exploration in this area. [Copyright &y& Elsevier]

In the light of field investigation, microscopic study, X-ray phase analysis and mineral infrared spectral analysis, it is considered that laumontitization is of extensive occurrence in the Axi gold orefield. The development of laumontilization and its relationship to mineralization show that the laumontitization appeared mainly at the lop of and in the periphery of orebodies, and occurred at the edge of the epithermal system or at the late stage of epithermal system evolution. Therefore, laumontitization can be used as an exploration indicator of epithermal gold deposits. The fluids responsible for laumomitization in the Axi gold orefield are similar to those producing hot spring-type gold deposits or those from modern geothermal fields. Epithermal mineralization of the Axi gold deposit was dated at Carboniferous, indicating that the West Tianshan of China is a region favorable to epithermal-type gold mineralization and preservation. Hence the West Tianshan of China is a target area for exploring epithermal gold deposits. [ABSTRACT FROM AUTHOR]

[Display omitted] • CL images of quartz are dark in Tokuzbay orogenic gold deposit. • PC, C-type FIs are trapped from initially carbon-rich metamorphic fluids. • Organic carbon in the sediments significantly contributed to the carbon in the fluids. • Carbon isotopes of carbon-rich water-poor fluids are light in orogenic gold deposits. Carbon-rich or carbonic fluids are identified in some orogenic-type gold deposits worldwide. Their nature, origin, evolution, and relations with gold mineralization are still poorly understood. The Tokuzbay large-size orogenic-type gold deposit in Chinese Altai is characterized by enormous CO 2 -rich fluid inclusions (FIs), providing an ideal case to investigate the genetic relationship between carbon-rich hydrothermal systems and orogenic-type gold mineralization. The mineralization process in the Tokuzbay includes four stages: (1) stage I quartz-magnetite veins; (2) stage II quartz-pyrite veins; (3) stage III quartz-polymetallic sulfide veins; and (4) stage IV quartz-carbonate veins. Based on the microscopic investigation, cathodoluminescence (CL) imaging, Raman spectrum analysis, and mircothermometric measurements, three types of FIs are identified in the veins, including the N 2 -bearing carbonic or CO 2 -rich inclusions (PC-type), the CO 2 -H 2 O inclusions (C-type), and the H 2 O-dominated or aqueous inclusions (W-type). The FIs in the stage I minerals are dominated by PC- and C-types, with minor amount of W-type, and occur as primary and pseudosecondary within quartz grains. These inclusions show a salinity of 5.0—9.5 wt% NaCl eqv. and homogenize to liquid phase during 272℃ to 399℃, indicating their entrapment from an initially homogeneous carbon-rich CO 2 -H 2 O-NaCl metamorphic fluid system. From early to late stages, the PC- and C-type FIs are getting infertile, while the W-type FIs become more abundant, indicating the escapes of CO 2 and compositional transition from CO 2 -rich to H 2 O-rich system. Moreover, the decreasing in temperature (272–399 ℃, 238—326 ℃, 173—267 ℃ and 135—182 ℃ from stages I to IV, respectively) and salinity (5.0—9.5, 2.6—9.2, 2.3—7.8 and 1.4—4.3 wt% NaCl eqv. from stages I to IV, respectively), together with the decrease of the δ18O values, suggests an input of meteoric water during mineralization. In the main mineralization stages (II and III), some FIs show divergent homogenization direction (liquid vs vapor) at similar homogeneous temperatures, yielding quite different salinities. For example, the coexisting W-type and C-type FIs yield similar homogenization temperatures, and the liquid-rich and vapor-rich FIs divergently homogenize to liquid and vapor at similar temperatures with different salinities. This indicates that the fluid effervescence drove phase separation and caused the CO 2 escape from the fluid system which promoted the gold precipitation at the ductile-to-brittle transition zone that revealed by the depth (8—11 km) calculated by the C-type FIs of the immiscible inclusion assemblages. The δ13C values of the CO 2 extracted from fluid inclusions range from –7.6 to –22.8‰, suggesting that the CO 2 might be derived from the hydrolysis of organic matter in the source sediments during metamorphism, rather than simply sourced from magma or the mantle. This understanding is supported by the widespread observation of the low δ13C values from most of orogenic-type gold deposits hosted in sedimentary rocks worldwide. [ABSTRACT FROM AUTHOR]

[Display omitted] • Fluid immiscibility plays an important role in gold precipitation. • Magma was likely a major source of ore-forming fluid and material. • High Co/Ni ratios of pyrite are consistent with a magmatic–hydrothermal origin. • The Xiaobeigou is a mesothermal magmatic–hydrothermal lode gold deposit. The Xiaobeigou gold deposit (>20 t @ 17.36 g/t) is located in the Jiapigou gold district (JGD), Northeast China, representing a large-sized quartz vein-type gold deposit hosted by Neoarchean basement gneiss and is related to Mesozoic intrusions in space and time. Four hydrothermal stages were identified from early to late, namely, (1) barren quartz stage, (2) quartz–pyrite stage, (3) gold–quartz–polymetallic sulfide stage, and (4) quartz–carbonate stage. Three main types of fluid inclusions (FIs) have been identified: water-rich (H 2 O–NaCl; W-type), mixed aqueous-carbonic (CO 2 –H 2 O–NaCl; C-type) and pure carbonic (CO 2 ; PC-type) FIs. The early-stage quartz contains W- and C-type FIs that yield moderate homogenization temperatures (270–379 °C) and moderate-low salinities (4.82–17.87 wt% NaCl equivalent). The main-stage quartz grains contain all three types of FIs that yield medium–low temperature (179–263 °C) and moderate-low salinity (2.82–9.86 wt% NaCl equivalent). Only W-type FIs are recognized in late-stage quartz grains, which have low temperatures (133–183 °C) and low salinities (1.91–7.73 wt% NaCl equivalent). The initial ore-forming fluid of the Xiaobeigou gold deposit was a moderate homogenization temperature and moderate-low salinity CO 2 –H 2 O–NaCl ± CH 4 ± N 2 hydrothermal fluid system. Fluid immiscibility is the main mechanism leading to the precipitation of gold and other metal sulfides. The H–O isotopic values (δ18O H2O = −6.87 to 5.90‰; δD = −102 to −78‰) and composition of the quartz suggest that the initial ore-forming fluids consisted mainly of magmatic water mixed with meteoric water during the late stage of the mineralization process. The S isotope data (δ34S = 3.2 to 4.4‰, avg. 3.6‰) indicate that the ore-forming materials are magmatic sources. EPMA and LA–ICP–MS data show that a large amount of gold mineralization mainly occurs in the main ore-forming stage. The high Co/Ni ratio indicates that the pyrite may be a magmatic–hydrothermal source. Taking into account all available data and regional geological history, we suggest that a magmatic–hydrothermal source for the Xiaobeigou gold deposit in the JGD and the ore formation is related to the subduction of the Paleo-Pacific Plate beneath Eurasia. [ABSTRACT FROM AUTHOR]

The Tokuzbay gold deposit is one of the represented gold deposits in Altai Orogen and the ores hosted in metamorphic rocks and magmatic dikes in a shear zone. Ore hosting magmatic dikes are intruded at Devonian, representing the product of the subduction-accretion process of the Altai Orogen. However, the ores are mineralized at Early Permian and is closely related to the sinistral shearing of Ma'erkakuli Fault. Gold mineralization in this deposit is related to the collision between the Junggar Plate and Altai Orogen. The orogenic gold deposits represented by the Tokuzbay deposit indicate that the Altai Orogen is characterized by orogenic gold mineralization related to the late Paleozoic collision. [Display omitted] • Tokuzbay gold deposit is an orogenic system controlled by shear zones. • Tokuzbay gold deposit was generated in the Permian collisional orogenesis. • The ore-hosting magmatic dikes originated from the Devonian plate subduction. • Orogenic gold mineralization in Altai Orogen resulted from late Paleozoic collision. Orogenic gold deposits are one of the most important gold deposits in the world. However, it is controversial that orogenic gold deposits are only generated at subduction-accretion or both in collisional setting. The Altai Orogen experienced a complex subduction accretion–collision history, including magmatism and metamorphism, and forming giant gold deposits. The Tokuzbay gold deposit consists of quartz vein ores and disseminated ores hosted in dikes. The ore bodies are controlled by secondary shear zone of the NW-, NNW-trending Ma'erkakuli Fault and occurred in meta -sediments, i.e., meta -sandstone and phyllite of Devonian Altai Formation, and diorite dikes and granite porphyritic dikes. Wall rock alteration is represented by silicification, pyritization, and muscovite alteration. The ores are restricted by ductile and brittle deformation in the shear zone. Large amounts of native gold and auriferous tellurium were precipitated during a transition from ductile to brittle regime. These characteristics indicate that the Tokuzbay gold deposit is an orogenic gold deposit in the Altai Orogen. The zircon LA-ICP-MS U-Pb ages of the ore-bearing granite porphyritic dikes and diorite dikes are 390 ± 2.5 Ma (MSWD = 0.87) and 378 ± 4 Ma (MSWD = 0.21), respectively, indicating that the magmatic rocks were emplaced during subduction of the Paleo Asian Ocean beneath Altai Orogen. Muscovite samples associated with gold from the auriferous quartz vein and disseminated ores hosted in diorite dikes returned Ar-Ar ages of 292.7 ± 1 Ma (MSWD = 1.3) and 293.9 ± 1.2 Ma (MSWD = 0.7), indicating that gold mineralization in quartz vein is synchronized with disseminated ores. The gold mineralization is restricted to the Early Permian and overlaps with the collision between Altai Orogen and Junggar Plate. The ore-hosting magmatic rocks related to subduction are more than 100 million years earlier than the ore-forming events. Combined with the regional tectonic evolution and the shear characteristics of the gold district, it is well proved that sinistral shearing trigged by the collision of Junggar Plate and Altai Orogen contributed to gold mineralization of the Tokuzbay deposit. Considering the Altai gold deposits in Kazakhstan, it is revealed that Permian collision between Junggar Plate and Altai Orogen triggered a large number of orogenic gold mineralization. [ABSTRACT FROM AUTHOR]

[Display omitted] • A low I Sr (t) fluid system is required for formation of Tokuzbay gold deposit. • Pb isotopes of sulfides are similar with the ore hosting Altai Formation. • The gold mineralization may have originated from the metamorphic dehydration of sediments of Altai Formation. Orogenic gold deposits are the most important gold resource in the world. It is controversial whether their ore-forming fluids were sourced from metamorphic dehydration of the crust or the mantle. The Tokuzbay gold deposit is a typical orogenic-type gold deposit in the Central Asian Orogenic Belt, providing a case for discussing the source of ore-forming fluids. The auriferous quartz veins are fault-controlled and occur mainly in metamorphic sediments of Devonian Altai Formation and minor in diorite dikes, forming three ore types, i.e., quartz vein, altered metamorphic sediments and altered diorite dikes. We studied the Sr–Nd–Pb isotope characteristics of the ore sulfides, and magmatic and metamorphic rocks from the Tokuzbay gold deposit, and thereby discuss the source of the ore-forming fluids. The 87Sr/86Sr ratios of meta -sediment hosted ores scatter between 0.709474 and 0.715238, and I Sr (292 Ma) values range from 0.706570 to 0.714045. The diorite dikes hosted ores show more restricted 87Sr/86Sr ratios ranging from 0.706963 to 0.711519, and I Sr (292 Ma) values ranging from 0.706777 to 0.710612. The wall rocks of the Altai Formation have I Sr (292 Ma) values of 0.711778 and 0.714409, which are higher than ore sulfides. This indicates that the I Sr (292 Ma) values of initial ore-forming fluids that interacted with the Altai Formation are no higher than 0.706777, which is the lowest I Sr (292 Ma) value for disseminated ores. The calculated (143Nd/144Nd) i ratios and ε Nd (292 Ma) values for meta -sediment hosted ores range from 0.511882 to 0.512464, and −7.4 to 4.0, respectively. The calculated (143Nd/144Nd) i ratios and ε Nd (292 Ma) values for diorite dike hosted ores vary from 0.512293 to 0.512562, and from 0.6 to 5.9, respectively. The meta -sediments of Altai Formation show ε Nd (292 Ma) values ranging from −6.8 to −4.4 with an average of −5.8, which are lower than those of ore sulfides. This indicates that the ε Nd (292 Ma) values for the fluids that interacted with the wall rocks cannot be lower than 4.5, which is the average value for disseminated ores. The calculated (208Pb/204Pb) i , (207Pb/204Pb) i , and (206Pb/204Pb) i values of ore sulfides are 37.796–38.989, 15.512–15.707, 17.988–18.100, respectively. The wall rocks of the Altai Formation show relatively higher (206Pb/204Pb) i ratios, indicating that the ore-forming fluid that interacted with the Altai Formation are not higher than 17.988, which is the lowest values of sulfides from disseminated ores. Based on the Sr–Nd–Pb isotope data, we suggest the possible ore-forming fluids should have lower I Sr (292 Ma) values, higher ε Nd (292 Ma) values, and lower (206Pb/204Pb) i values compared to the those of ore sulfides and were possibly sourced from a source compositionally similar to the diorite dikes in addition to wall rocks of Altai Formation. Combining with the regional metamorphism and tectonic evolution, we suggest that the ore fluids have originated from the metamorphic dehydration of sediments of Altai Formation in the South Altai during the collision between Altai Orogen and Junggar Plate. [ABSTRACT FROM AUTHOR]

A total of 334 sets of age data were obtained from the three sandstone samples, which range from 2598 to 330 Ma. Ages of the zircon grains fall into three major groups: Paleozoic (<540 Ma) (Fig. A), Neoproterozoic to late Precambrian (540–1800 Ma), and early Precambrian (>1800 Ma) (Fig. B). The Hf isotope data show that the detrital zircon source probably shares similar origin with the Jinwozi granite (Fig. C). These rocks may have formed in the early Paleozoic Caledonian Orogeny, during which the supercontinents of Gondwana and Laurasia assembled. This mountain building process may have provided the detritus for the clastic rocks of the Jinwozi Formation. • Au veins or lodes in Jinwozi deposit occur in Jinwozi Formation or Jinwozi granite. • Jinwozi Formation deposited after 330 Ma, postdates the Silurian Jinwozi granite. • The debris of Jinwozi Formation were mainly sourced from mid-Paleozoic granites. • The strongest crustal growth occurred in mid-Paleozoic (420 ± 50 Ma) in Beishan area. The Jinwozi deposit is the most economically important gold (Au) deposit in the Beishan Orogen (Eastern Xinjiang, NW China). The Au orebodies occur as quartz veins or altered lodes in the Jinwozi Formation clastic rocks and the Jinwozi granite. The age, detrital source and tectonic setting of the Jinwozi Formation, however, have not been well understood. In this paper, we reported new LA–ICP MS detrital zircon U–Pb ages and Lu–Hf isotopes of ore-hosted clastic rock of the Jinwozi Formation. Detrital zircons from three samples yield 334 U–Pb ages varied from 330 to 2598 Ma, showing complex detrital sources. The youngest detrital zircon population suggests that the Jinwozi Formation deposited no earlier than 330 Ma in the Late Carboniferous or Permian. The majority of the detrital zircons (291 out of 334) have ages between 330 and 533 Ma, suggesting a dominant Paleozoic detrital source. Much of these age data (282 out of 334) range from 470 to 370 Ma, broadly coeval with the zircon U–Pb ages of the Jinwozi granite. Zircon Hf isotope data also implicate their similar origin to the Jinwozi granite. The source rocks, as well as the Jinwozi granite, may have formed in the Early Paleozoic Caledonian Orogeny, during which the supercontinents of Gondwana and Laurasia assembled. This orogeny process may have provided plenty of detritus for the clastic rocks of the Jinwozi Formation. Precambrian detrital zircon ages from the Jinwozi Formation cluster around 2400–2600 Ma, 1800–2100 Ma, 800–1300 Ma, which corresponds to the supercontinent assembly events of Kenor, Columbia and Rodinia, respectively. The age populations of 2200–2300 Ma and 600–660 Ma are possibly related to the breakup of Kenor and Rodinia supercontinents. This understangding is supported by zircon Hf isotope data. [ABSTRACT FROM AUTHOR]