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Although China is well-endowed with tungsten deposits, while the tungsten resources in the Central Asian Orogen Belt (CAOB) are rarely reported. Recently, many W-skarn deposits have been discovered in the East Tianshan, but the source and evolution of the mineralising fluids are poorly understood. The Xiaobaishitou W(–Mo) deposits are hosted by carbonaceous limestone or banded crystalline limestone in the Mesoproterozoic Jianshanzi Formation, which is intruded by Triassic biotite monzogranite. The deposit comprises garnet-dominated prograde skarn and retrograde skarns followed by oxides (scheelite–cassiterite–magnetite), sulphides (quartz–molybdenite–bismuthinite–pyrite–chalcopyrite–sphalerite–galena), and carbonate stages. The types of fluid inclusions are composed of liquid-rich aqueous, vapour-rich aqueous, aqueous carbon-dioxide, and daughter mineral-bearing inclusions. The homogenization temperatures of fluid inclusions change from > 400 °C in garnet, through > 380 °C in epidote and 310–280 °C in scheelite, to 280 °C in quartz and 220 °C in calcite indicating a complex magmatic-hydrothermal process. The δ18Owater values varied from + 6.1 to + 8.4‰ in garnet, + 5.2 to + 7.4‰ in epidote, + 2.0 to + 3.0‰ in quartz, to − 0.7 to − 0.1‰ in calcite. The corresponding δD values are − 95 to − 71‰ in garnet, − 84 to − 80‰ in epidote, − 115 to − 90‰ in quartz and − 101 to − 89‰ in calcite. Both O and H isotopic compositions show the mineralisation fluids are originated from deep-sourced magmatic fluids. The δ13CCO2 values in the calcite range from − 7.8 to − 7.7‰, which is characteristic of magmatic fluids interacting with reduced carbon from metamorphic rocks. The δ34S values of hydrothermal fluids range from + 4.5 to + 5.1‰, and 206Pb/204Pb, 207Pb/204Pb and 208Pb/204Pb ratios of sulphide are 18.072–18.664, 15.566–15.708, and 38.245–38.658, respectively, representing a mixed characteristic of magmatic and sedimentary sulphur. Considering the coexisting of L-type and V-type inclusions in the scheelite, we proposed that pH increase caused by fluid boiling may be the major cause for the precipitation of scheelite at the Xiaobaishitou deposit.

Buchwaldoboletus xylophilus and Phlebopus portentosus (Boletales) are two non-ectomycorrhizal boletes, which are widely reported in tropical Asia. However, there is little information available about the taxonomy of these two boletes. Here, B. xylophilus and P. portentosus are redescribed based on morphology and molecular phylogenetic analyses of DNA sequences from nuclear 28S rDNA (28S), nuc rDNA internal transcribed spacer region ITS1-5.8S-ITS2 (ITS), translation elongation factor 1-α gene (TEF1) and the RNA polymerase II second largest subunit gene (RPB2). Detailed descriptions, color photos of fresh basidiomata, and line-drawings of microscopic features of the two taxa are presented.

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 $$\delta^{13} {\text{C}}_{{{\text{CO}}_{2} }}$$ 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 $$\delta^{13} {\text{C}}_{{{\text{CO}}_{2} }}$$ 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 $$\delta^{13} {\text{C}}_{{{\text{CO}}_{2} }}$$ 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.

Formation of a large igneous province, an explosive magmatic event in earth, is intimately related to geodynamic processes. The Tarim large igneous province, a famous representative in China, conta...

The volcanic rocks hosting the iron deposits in the Aqishan–Yamansu metallogenic belt are sodium-rich. The geochronology, petrography, and geochemistry of minerals and sodium-rich rocks as well as the relationship between these rocks and the iron deposits are studied. Geochemically, the ore-hosting volcanic rocks are sodium-rich (the averages of Na2O and Na2O/K2O are 4.31 ​wt.% and 8.56, respectively) and belong to the calc-alkaline series. They are enriched in LREEs and LILEs (Ba, U, K, and Sr), but depleted in HFSEs (Nb, Ta, and Ti). SHRIMP zircon U–Pb dating of the crystal tuff in the Aqishan Formation and the dacite in the Tugutu Bulak Formation yields ages of 337.5 ​± ​2.3 ​Ma (n ​= ​15, MSWD ​= ​0.85) and 313.0 ​± ​3.3 ​Ma (n ​= ​13, MSWD ​= ​0.74), respectively, indicating that the sodium-rich volcanic rocks formed from the early–late Carboniferous. Electron microprobe data from plagioclases demonstrate that albites and/or oligoclases were formed in the basic–intermediate–acid volcanic rocks. Two stages of albitization are identified, and the latter is likely attributed to the dissolution of iron in the Aqishan–Yamansu belt. The sodium-rich volcanic rocks probably formed by the interaction between volcanic lava and seawater after volcanoes erupted on the seafloor; meanwhile, the albites formed by element substitution in a low-metamorphic environment. The spatiotemporal coupling relationship between sodium-rich volcanic rocks and iron deposits in the Aqishan–Yamansu belt is favorable. Iron dissolved from the dark minerals of basic–intermediate volcanic rocks through sodium metasomatism is one of the material sources for the iron deposits. Keywords: Sodium-rich volcanic rock, Geochronology, Rock geochemistry, Yamansu metallogenic belt, Eastern tianshan orogenic belt

Topological systems are inherently robust to disorder and continuous perturbations, resulting in dissipation-free edge transport of electrons in quantum solids, or reflectionless guiding of photons and phonons in classical wave systems characterized by topological invariants. Realization of robust, lossless topological insulators in the technologically important terahertz (THz) frequency range has drawn immense attention. In this paper, we propose a Kagome lattice structure that supports topological edge states with valley-dependent transport. Optical topological insulators are subsequently fabricated, in which mirror symmetry is broken and degenerate states are lifted at K(K′) valleys in the band structure. Theoretical and numerical analyses show that four types of edge states can be obtained. The performance of the fabricated topological waveguides is characterized with THz time-domain spectroscopy (TDS). Nearly identical THz wave transmission in the 0.437-0.453-THz range is verified with a straight-line topological waveguide and Z-shaped waveguides with multiple sharp turning corners, which quantitatively illustrate the strong backscattering suppression effects from the nontrivial topology edge states of the structures. Particularly, the THz TDS measurements provide important extra time-domain information about the topological waveguiding mode, which is generally unavailable from previous topological insulator investigations solely replying on power spectrum measurements.

The culturally unique Sanya Hui (SYH) people are regarded as the descendants of ancient Cham people in Central Vietnam (CV) and exhibit a scenario of complex migration and admixture history, who were likely to first migrate from Central and South Asia (CSA) to CV and then to South Hainan and finally assimilated with indigenous populations and resided in the tropical island environments since then. A long-standing hypothesis posits that SYH derives from different genetic and cultural origins, which hypothesizes that SYH people are different from the genetically attested admixture history of northern Hui people possessing major Han-related ancestry and minor western Eurasian ancestry. However, the effect of the cultural admixture from CSA and East Asia (EA) on the genetic admixture of SYH people remains unclear. Here, we reported the first batch of genome-wide SNP data from 94 SYH people from Hainan and comprehensively characterized their genetic structure, origin, and admixture history. Our results found that SYH people were genetically different from the northern Chinese Hui people and harbored a close genomic affinity with indigenous Vietnamese but a distinct relationship with Cham, which confirmed the hypothesis of documented recent historical migration from CV and assimilation with Hainan indigenous people. The fitted admixture models and reconstructed demographic frameworks revealed an additional influx of CSA and EA ancestries during the historical period, consisting of the frequent cultural communication along the Southern Maritime Silk Road and extensive interaction with EA. Analyses focused on natural-selected signatures of SYH people revealed a similar pattern with mainland East Asians, which further confirmed the possibility of admixture-induced biological adaptation of island environments. Generally, three genetically attested ancestries from CV, EA, and CSA in modern SYH people supported their tripartite model of genomic origins.

Background: Previous studies have suggested that the human Y-chromosome haplogroup Q1a1a-M120, a widespread paternal lineage in East Asian populations, originated in South Siberia. However,...

Yunnan province harbours substantial genetic, cultural and linguistic diversity, with the largest number of Aborigines in China, but the relationship among these Aborigines remains enigmatic. This study genotyped 45 Y chromosomal single nucleotide polymorphisms (SNPs) of 500 males from two aboriginal cross-border populations, Jingpo and Dai, from Dehong, Yunnan. It is reported that Haplogroup O2a2b1a1-M117 is the dominant lineage in both Jingpo and Dai. The Jingpo people show affinity with Tibeto-Burman speaking populations with a relatively high frequency of Haplogroup D-M174, and the Dai people are generally genetically similar with Tai-Kadai speaking populations with high frequencies of Haplogroup O1a-M119 and O1b1a1a-M95, which is consistent with their language classification.

The Kalatage area, located in the middle of the Dananhu arc in the Eastern Tianshan, NW China, contains abundant and different types of mineralization , e.g. volcanogenic massive sulfide (VMS) Cu-Zn deposits, porphyry Cu (-Au) deposits and volcanic hydrothermal vein Cu (-Au) deposits, represents an integral component of the Central Asian Orogenic Belt (CAOB). The Meiling hydrothermal Cu-Zn (-Au) deposit is located in the core of the Kalatage area and can be studied to better understand the processes of Paleozoic Cu mineralization in the Kalatage area. This deposit hosted in the intermediate-felsic volcanic, volcanoclastic and subvolcanic rocks. The subvolcanic rocks controlled the Cu mineralization and the distributions of the orebodies. The alteration developed along the volcanic structures, where the NW-SE, NNW-SSE, NE-SW and E-W-trending faults controlled the distribution of ores. The ores mainly occur as quartz sulfide veins and stockwork quartz sulfide veins, which contain pyrite , chalcocite, chalcopyrite , sphalerite , quartz, sericite, and/or minor calcite/gypsum/barite. Here, we report new zircon U-Pb, sericite Ar-Ar and sulfide Rb-Sr ages to constrain the geochronological framework of the Meiling deposit. The mineralization-related quartz porphyry yields a weighted mean age of 298.7 ± 2.9 Ma; the sericite from the phyllic alteration zone of the M2 orebody yields a plateau age of 265 ± 17 Ma and a consistent inverted isochron age of 261 ± 10 Ma; and the syngenetic sulfides of the M1 and M12 orebodies yield Rb-Sr isochron ages of 299 ± 3 Ma and 301 ± 4 Ma, respectively. All of these ages indicate that the metallogenic epoch of the Meiling deposit occurred in the late Carboniferous (300 Ma). Furthermore, combined with the mineralization ages of the early Silurian Honghai VMS deposit and the middle Devonian Yudai porphyry deposit, our data suggest that the the Kalatage island arc is a long-lived arcs and controls to formed the VMS-type deposit in the immature arc during the Early Silurian, the adakitic intrusions related porphyry-type deposit in the mature arc during the Middle Devonian, and the subvolcanic intrusions related volcanic hydrothermal vein-type Cu(Zn/Au) deposits in the shallow crust of the mature arc during the late Carboniferous.

The Qiman Tagh W–Sn belt lies in the westernmost section of the East Kunlun Orogen, NW China, and is associated with early Paleozoic monzogranites, tourmaline is present throughout this belt. In this paper we report chemical and boron isotopic compositions of tourmaline from wall rocks, monzogranites, and quartz veins within the belt, for studying the evolution of ore-forming fluids. Tourmaline crystals hosted in the monzogranite and wall rocks belong to the alkali group, while those hosted in quartz veins belong to both the alkali and X-site vacancy groups. Tourmaline in the walk rocks lies within the schorl–dravite series and becomes increasingly schorlitic in the monzogranite and quartz veins. Detrital tourmaline in the wall rocks is commonly both optically and chemically zoned, with cores being enriched in Mg compared with the rims. In the Al–Fe–Mg and Ca–Fe–Mg diagrams, tourmaline from the wall rocks plots in the fields of Al-saturated and Ca-poor metapelite, and extends into the field of Li-poor granites, while those from the monzogranite and quartz veins lie within the field of Li-poor granites. Compositional substitution is best represented by the MgFe−1, Al(NaR)−1, and AlO(Fe(OH))−1 exchange vectors. A wider range of δ11B values from −11.1‰ to −7.1‰ is observed in the wall-rock tourmaline crystals, the B isotopic values combining with elemental diagrams indicate a source of metasediments without marine evaporates for the wall rocks in the Qiman Tagh belt. The δ11B values of monzogranite-hosted tourmaline range from −10.7‰ and −9.2‰, corresponding to the continental crust sediments, and indicate a possible connection between the wall rocks and the monzogranite. The overlap in δ11B values between wall rocks and monzogranite implies that a transfer of δ11B values by anataxis with little isotopic fractionation between tourmaline and melts. Tourmaline crystals from quartz veins have δ11B values between −11.0‰ and −9.6‰, combining with the elemental diagrams and geological features, thus indicating a common granite-derived source for the quartz veins and little B isotopic fractionation occurred. Tourmalinite in the wall rocks was formed by metasomatism by a granite-derived hydrothermal fluid, as confirmed by the compositional and geological features. Therefore, we propose a single B-rich sedimentary source in the Qiman Tagh belt, and little boron isotopic fractionation occurred during systematic fluid evolution from the wall rocks, through monzogranite, to quartz veins and tourmalinite. Keywords: Tourmaline, Chemical composition, Boron isotope, Qiman Tagh W–Sn belt, Fluid evolution

OBJECTIVES The aim of this research was to explore the origin, diversification, and demographic history of O1a-M119 over the past 10,000 years, as well as its role during the formation of East Asian and Southeast Asian populations, particularly the Han, Tai-Kadai-speaking, and Austronesian-speaking populations. MATERIALS AND METHODS Y-chromosome sequences (n = 141) of the O1a-M119 lineage, including 17 newly generated in this study, were used to reconstruct a revised phylogenetic tree with age estimates, and identify sub-lineages. The geographic distribution of 12 O1a-M119 sub-lineages was summarized, based on 7325 O1a-M119 individuals identified among 60,009 Chinese males. RESULTS A revised phylogenetic tree, age estimation, and distribution maps indicated continuous expansion of haplogroup O1a-M119 over the past 10,000 years, and differences in demographic history across geographic regions. We propose several sub-lineages of O1a-M119 as founding paternal lineages of Han, Tai-Kadai-speaking, and Austronesian-speaking populations. The sharing of several young O1a-M119 sub-lineages with expansion times less than 6000 years between these three population groups supports a partial common ancestry for them in the Neolithic Age; however, the paternal genetic divergence pattern is much more complex than previous hypotheses based on ethnology, archeology, and linguistics. DISCUSSION Our analyses contribute to a better understanding of the demographic history of O1a-M119 sub-lineages over the past 10,000 years during the emergence of Han, Austronesians, Tai-Kadai-speaking populations. The data described in this study will assist in understanding of the history of Han, Tai-Kadai-speaking, and Austronesian-speaking populations from ethnology, archeology, and linguistic perspectives in the future.

Objectives The origin and differentiation of Austronesian populations and their languages have long fascinated linguists, archeologists, and geneticists. However, the founding process of Austronesians and when they separated from their close relatives, such as the Daic and Austro-Asiatic populations in the mainland of Asia, remain unclear. In this study, we explored the paternal origin of Malays in Southeast Asia and the early differentiation of Austronesians. Materials and methods We generated whole Y-chromosome sequences of 50 Malays and co-analyzed 200 sequences from other Austronesians and related populations. We generated a revised phylogenetic tree with time estimation. Results We identified six founding paternal lineages among the studied Malays samples. These founding lineages showed a surprisingly coincident expansion age at 5000 to 6000 years ago. We also found numerous mostly close related samples of the founding lineages of Malays among populations from Mainland of Asia. Conclusion Our analyses provided a refined phylogenetic resolution for the dominant paternal lineages of Austronesians found by previous studies. We suggested that the co-expansion of numerous founding paternal lineages corresponds to the initial differentiation of the most recent common ancestor of modern Austronesians. The splitting time and divergence pattern in perspective of paternal Y-chromosome evidence are highly consistent with the previous theories of ethnologists, linguists, and archeologists.

Previous studies have shown that the genus Tagiades Hübner, 1819 is paraphyletic with regard to Daimio Murray, 1875 and/or Darpa Moore, 1866. In this study, we attempt to disentangle the relationships among these three genera based on an integrative approach including molecular data, morphological characters, and biological data from available sources. All evidence shows that Daimio and Tagiades are congeneric, isolated from Darpa. According to the rule of priority, Daimio (syn. n.) is a junior synonym of Tagiades. Therefore, we subsume tethys under Tagiades as Tagiades tethys (Ménétriés, 1875), comb. n.

The Baiganhu W-Sn ore field in the northwestern area of the East Kunlun Orogen, NW China, contains three economically important W-Sn deposits, namely Kekekaerde, Baiganhu and Bashierxi. Timing of the W-Sn mineralization remains under debates due to lack of precise isotope dating directly conducted on ore minerals. We herewith report LA-MC-ICP-MS (laser ablation (multi-collector) inductively coupled plasma mass spectrometry) and ID-TIMS (isotope dilution thermal ionization mass spectrometry) cassiterite U−Pb ages for the Kekekaerde W-Sn deposit in the Baiganhu W-Sn ore field. The ID-TIMS cassiterite 206 Pb/ 238 U results yield a weighted mean age of 416 ± 1 Ma (95% confidence, MSWD = 0.8), and the LA-MC-ICP-MS analytical data give a 206 Pb/ 207 Pb– 238 U/ 207 Pb isochron age of 426 ± 13 Ma (95% confidence, MSWD = 0.1). These two ages are same within errors, suggesting that the mineralization in the Baiganhu W-Sn ore field occurred at ca. 416 Ma. These new ages and understandings are consistent with the previously reported zircon U−Pb ages of 430–420 Ma for the ore-bearing granites in the ore-field, and with the 40 Ar/ 39 Ar plateau ages of ca. 412 Ma for the hydrothermal muscovite from ore-bearing quartz veins and greinsenized granite. It shows that the granite magmatism and its associated hydrothermal mineralization resulted from the Caledonian Orogeny that accommodated the closure of the Proto-Tethys, followed by the continental collision between the Central Kunlun, Northern Kunlun terranes and the Qaidam Block.

The Qiman Tagh W-Sn ore belt is located in the westernmost sector of the East Kunlun Orogen, NW China. It has been recognized as a unique W-Sn belt that formed in the early Paleozoic and related to closure of the Proto-Tethys. To understand the evolution of ore-forming fluids and its relationship with the tectonic setting of East Kunlun Orogen, we report the results obtained from fluid inclusion and H-O isotopic studies of ores and quartz veins for the Qiman Tagh W-Sn ore belt. Mineralization in Qiman Tagh includes four stages characterized by quartz-cassiterite-wolframite assemblage stage 1, quartz ± scheelite assemblage stage 2, quartz-polymetallic sulfides stage 3, and ore-barren veins stage 4. The former two stages are conducive to mineralization, while the latter two stages are less important. The fluid inclusions are distinguished between CO2-H2O (C-type) and NaCl-H2O (W-type) in composition, containing a trace of CH4, N2, C2H6, SO2, and CO32–. Cassiterite and quartz in stage 1, instead of wolframite, contain a great deal of C-type inclusions. All inclusions in minerals of stage 1 yield homogenization temperatures of 230.1–384.1 °C (peaking at 310–320 °C), with salinities lower than 14.76 wt% NaCl equiv. and bulk densities of 0.63–0.89 g/cm3. The stage 2 minerals contain both two types of inclusions, yielding homogenization temperatures of 183.4–335.9 °C (peaking at 280–290 °C), with salinities lower than 14.53 wt% NaCl equiv. and bulk densities of 0.66–0.97 g/cm3. Fluid inclusions in minerals of stages 3 and 4 are mainly W-type and homogenized at temperatures of 140.6–277.6 °C (peaking 210–220 °C), and 116.9–255.1 °C (peaking 160–170 °C), respectively. The H-O isotopic systematics shows that the fluids were dominated by magmatic water in stages 1 and 2, but by meteoric water in stages 3 and 4. Integrating all the geological and geochemical data, we conclude that the fluids forming the Qiman Tagh W-Sn ore belt evolved from granite-derived, CO2-rich and reducing, to meteoric water-dominated, CO2-poor and oxidizing. Fluid immiscibility, cooling and interaction with rocks are main mechanisms for metallic deposition.

As an attractive supercapacitor material, MnO2 greatly suffers poor conductivity and unsatisfied stability. In this work, double-shelled poly(3,4-ethylenedioxythiophene) (PEDOT) and MnO2 decorated Ni nanotube arrays (NTAs) are successfully synthesized by a simple electrodeposition strategy, endowing the hybrid with remarkably improved conductivity and prolonged durability. As a self-supported electrode, the resulting PEDOT@MnO2@NiNTAs exhibits outstanding electrochemical properties, including high mass capacitance (based on MnO2 mass, 442.85 F g−1 at 2.5 A g−1) and excellent cycling stability (80.37% capacitance retention after 15000 cycles). Furthermore, when assembling an asymmetric supercapacitor with the PEDOT@MnO2@NiNTAs and activated carbon (AC), the device affords a voltage window up to 1.7 V and delivers a large volumetric capacitance (1.47 F cm−3 at 4 mA cm−3) and high energy density (0.59 mWh cm−3 at power density of 84.96 mW cm−3), indicating its great potential in practical supercapacitor applications.

The Qiman Tagh of the East Kunlun Orogen, NW China, lies within the Tethysides and hosts a large W–Sn belt associated with the Bashierxi monzogranite. To constrain the origin of the granitic magmatism and its relationship with W–Sn mineralization and the tectonic evolution of the East Kunlun Orogen and the Tethys, we present zircon U–Pb ages and Hf isotopic data, and whole-rock compositional and Sr–Nd–Pb isotopic data of the Bashierxi monzogranite. The granite comprises quartz, K-feldspar, plagioclase, and minor muscovite, tourmaline, biotite, and garnet. It contains high concentrations of SiO2, K2O, and Al2O3, and low concentrations of TiO2 and MgO, indicating a peraluminous high-K calc-alkaline affinity. The rocks are enriched in Rb, U, Pb, and light rare earth elements, and relatively depleted in Eu, Ba, Nb, Sr, P, and Ti, and are classified as S-type granites. Twenty zircon grains yield a weighted mean 238U/206Pb age of 432 ± 2.6 Ma (mean square weighted deviation = 1.3), indicating the occurrence of a middle Silurian magmatic event in the region. Magmatic zircons yield eHf(t) values of −6.7 to 0.7 and corresponding two-stage Hf model ages of 1663–1250 Ma, suggesting that the granite was derived from Mesoproterozoic crust, as also indicated by 207Pb/206Pb ages of 1621–1609 Ma obtained from inherited zircon cores. The inherited zircon cores yield eHf(t) values of 8.3–9.6, which indicate the generation of juvenile crust in the late Paleoproterozoic. Samples of the Bashierxi granite yield high initial 87Sr/86Sr ratios and radiogenic Pb concentrations, and negative eNd(t) values. Isotopic data from the Bashierxi granite indicate that it was derived from partial melting of ancient (early Paleozoic to Mesoproterozoic) sediments, possibly representing recycled Proterozoic juvenile crust. Middle Silurian granitic magmatism resulted from continental collision following closure of the Proto-Tethys Ocean. The Qiman Tagh represents a Caledonian orogenic belt containing S-type granites and associated W–Sn deposits.

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.

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 ISr (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 ISr (292 Ma) values ranging from 0.706777 to 0.710612. The wall rocks of the Altai Formation have ISr (292 Ma) values of 0.711778 and 0.714409, which are higher than ore sulfides. This indicates that the ISr (292 Ma) values of initial ore-forming fluids that interacted with the Altai Formation are no higher than 0.706777, which is the lowest ISr (292 Ma) value for disseminated ores. The calculated (143Nd/144Nd)i ratios and eNd (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 eNd (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 eNd (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 eNd (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 ISr (292 Ma) values, higher eNd (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.

Xiao‐Hua Deng, Jing‐Bin Wang, M. Santosh, Yu‐Wang Wang, Ling‐Li Long, Hui‐Qiong Zhang, Li‐Ya Yang, Jun Xu, Xi Chen, Lei Chen

Background Neonatal inflammation may affect brain development and lead to cognitive and emotional deficits at adolescence and adulthood. The nucleotide binding and oligomerization domain-like receptor family pyrin domain-containing 3 (NLRP3) is the core component of NLRP3 inflammasome, which may involve in neuroinflammation. We explored if early-life exposure to the bacterial endotoxin lipopolysaccharide (LPS) could promote the expression of proteins related to NLRP3 inflammasome, including NLRP3, the apoptosis-associated speck-like protein (ASC) and cysteiny aspartate-specific protease (Caspase-1) in the forebrain, and behavioral alteration in adolescent rats. Methods Two-week old Sprague Dawley rats were divided into naive control, vehicle (phosphate buffered saline, PBS) control and LPS (100 μg/kg, i.p.) treatment groups. Anxiety and depression-like behaviors were examined around 1 month age, with the expression of NLRP3, ASC and Caspase-1 in the prefrontal cortex (PFC) and hippocampus analyzed by means of immunohistochemistry and western blot. Results LPS-treated rats exhibited anxiety but not depressive-like behavior as indicated by results of open field, elevated plus maze, dark-light box, sucrose preference and forced swimming tests. Increased immunolabeling of NLRP3, ASC and Caspase-1 in neurons and/or microglia occurred in the PFC and hippocampus in LPS-treated adolescents relative to controls, with immunoblot shown elevated levels of these proteins. Conclusion Early-life inflammatory stress promotes the expression of NLRP3 inflammasome proteins in the brain and the occurrence of anxiety-like behavior in adolescent rats.

The Xingdi II mafic–ultramafic complex is located in the northern rim of the Tarim Craton, Northern Xinjiang, NW China. This complex is mainly composed of gabbro, gabbronorite, websterite and lherzolite, plus minor granodiorites and granites. The geodynamic setting of this complex and other Neoproterozoic mafic–ultramafic complexes in the region is debated, with opinions varying from mantle plume to a continental arc. A new zircon U–Pb age from this study reveals > 7-myr difference for two gabbroic intrusive phases in the Xingdi II mafic–ultramafic complex and up to a 21-myr difference between this complex and the nearby mafic–ultramafic complexes that occur

Neurodegenerative disorders have attracted attention in last decades due to their high incidence in the world. The p53/miR-34a axis triggers apoptosis and suppresses viability in multiple types of cells, but little is known about its role in neurodegenerative diseases. In this study, we showed that presenilin (PS)-2, a major gene associated with familial Alzheimer's disease (AD) could trigger the apoptosis through the p53/miR-34a axis in PC12 cells. First we found that PC12 cell viability was downregulated by PS-2 and mutant PS-2 overexpression, especially by mutant PS-2 overexpression. Then, we established a mutant PS-2-overexpressing PC12 cell line and confirmed that mutant PS-2 induced not only p53 but also miR-34a expression. The transfection of miR-34a inhibitor reversed PS-2-induced effects on cellular viability and apoptosis. Mutant PS-2 overexpression promoted caspase-3 expression, reduced Sirt1 and Bcl-2 expression, all of which were miR-34a downstream genes related with cell apoptosis. Moreover, mutant PS-2 also activated the p53/miR-34a axis and induced apoptosis in AD transgenic mice brain. These results implied that mutant PS-2 might promote the apoptosis of neuronal cells through triggering the p53/miR-34a axis. Altogether our results provide a novel insight into neurodegenerative disease and deepen our understandings of AD pathogenic processes.

The Waifangshan Mo-quartz vein cluster occurs at the northernmost margin of the Qinling Orogen. The orebodies occur as quartz veins and are controlled by low-angle faults. We identify three hydrothermal stages, characterized by veinlets of quartz–pyrite, quartz–molybdenite–pyrite–chalcopyrite–galena–sphalerite, and quartz–carbonate assemblages, respectively. The early-stage quartz veins were structurally-deformed, brecciated, and filled by non-deformed middle- or late-stage veinlets, suggesting that the mineralization is associated with a tectonic transition from compression to extension. Five molybdenite separates from the Zhifang Mo deposit yield individual Re–Os ages from 241.2 ± 1.6 to 247.4 ± 2.5 Ma, with a weighted mean age of 243.8 ± 2.8 Ma. Individual Re–Os isotope ages of four molybdenite samples from the Badaogou Mo deposit range from 238.9 ± 2.1 to 255.8 ± 2.2 Ma, with a weighted mean age of 246 ± 10 Ma. Four analyses of molybdenite separates from the Xiangchungou Mo deposit yield individual Re–Os isotope ages of 243.8 ± 8.8 to 247.7 ± 4.4 Ma, with a weighted mean age of 246.0 ± 1.1 Ma. All of these data yield a weighted mean age of 241.9 ± 1.9 Ma, coeval with the accretionary orogeny. We thus conclude that the Waifangshan Mo-quartz veins formed during a transition from continental arc to back-arc setting. The Waifangshan Mo-quartz veins share similar geological, geochemical and geochronological features with the orogenic-type systems. We propose that the Waifangshan Mo-quartz veins are an orogenic-type Mo mineralization, and possibly represent the deepest member in the crustal continuum model of the orogenic-type mineral systems. The molybdenite samples from the Mo-quartz veins in the Waifangshan area have low Re contents (1.457 to 39.16 ppm), suggesting a continental crust-dominated source.

The giant Shangfanggou skarn-porphyry Mo–Fe deposit, one of the largest Mo deposits in the East Qinling Orogen, is hosted by the Neoproterozoic Luanchuan Group on the southern margin of the North China Craton. The mineralization occurs mainly as veinlets and in veinlet-disseminated form within altered schists, skarns, hornfelses, and/or marbles. The hydrothermal alteration and mineralization at Shangfanggou took place over four stages. Stage 1 involved potassic alteration and silicification in the porphyry, skarnization and magnetization in carbonate strata, and hornfelsization in schists. Quartz–molybdenite veins associated with phyllic alteration were produced in the porphyry during stage 2, along with sericitization, chloritization, serpentinization, and silicification in the skarns, hornfelses and/or marbles. Quartz–polymetallic sulfide veins related to phyllic alteration were produced during stage 3, and ore-barren quartz ± calcite ± pyrite veins associated with weak carbonatation were produced during stage 4. C, O, and D isotope compositions of hydrothermal calcite, dolomite, magnetite, phlogopite, and quartz from different stages of mineralization during the formation of the Shangfanggou deposit range from − 12.9‰ to + 8.8‰, − 3.2‰ to + 22.7‰, and − 100‰ to − 80‰, respectively. Sulfur isotope compositions of sulfides from the ores of the Shanfanggou deposit range from 3.6‰ to 4.4‰. 206 Pb/ 204 Pb, 207 Pb/ 204 Pb, and 208 Pb/ 204 Pb ratios of 17.648 to 18.742 (apart from one magnetite with a value of 20.78), 15.526 to 15.690, and 38.197 to 39.823 in the Shanfanggou deposit. The evolution of the ore-forming fluids in the Shangfanggou deposit, as revealed by δ 18 O, δD, and δ 13 C isotope studies, was one of progressive modification of the magmatic fluids through fluid–wall rock interactions along conduits during fluid ascent, and this signifies the involvement of formation/strata water during the earlier stages of mineralization, and the predominance of meteoric waters over magmatic fluids in the later stages. The carbon, sulfur, and lead isotope compositions suggest mixing took place between the magmas and the host rocks within the region. Integrating the data obtained from studies of the regional geology, ore geology, fluid inclusions, and C–H–O–S–Pb isotope geochemistry, we conclude that the Shangfanggou Mo–Fe deposit is a porphyry-skarn type system that formed during a transition from compressional to extensional tectonics during the Jurassic–Early Cretaceous continental collision between the North China Craton and Yangtze Craton. The ore materials were sourced from magmatic ore-forming fluids that mixed with components derived from carbonaceous wall rocks during their ascent, and which were gradually mixed with meteoric waters, especially in the later stages.

The Xiaobaishitou W (–Mo) deposit is located in the eastern segment of the Central Tianshan, northwestern China. The deposit represents a skarn system distributed in the contact zones of biotite granite and crystalline limestone of the Mesoproterozoic Kawabulag Group. The Xiaobaishitou deposit is characterized by a typical calc-silicate mineralogy dominated by garnet, diopside and wollastonite, with minor epidote, tremolite, actinolite, chlorite, quartz, fluorite and calcite. The prograde and retrograde skarns are characterized by garnet–clinopyroxene–wollastonite and epidote–tremolite–actinolite–chlorite, respectively, intruded and replaced by mineral assemblages of scheelite–cassiterite–magnetite, quartz–sulfides and calcite–quartz–fluorite in younger order. Six molybdenite samples from the deposit yielded Re − Os isotope model ages ranging from 239.7 ± 3.6 Ma to 251.4 ± 3.6 Ma. The zircon crystals from biotite granite and Mo-mineralized granite yield weighted 206Pb/238U age of 242 ± 1.7 and 240.5 ± 2.1 Ma, respectively. Both the zircon U − Pb and the molybdenite Re − Os ages obtained in this study fall in a narrow span of 242–240 Ma, which suggest that the Xiaobaishitou W (–Mo) system was formed in the Triassic. The Re contents of the molybdenites range from 40.33 to 64.67 ppm, suggesting that the ore-forming materials were derived mainly from continental crust together with the involvement of minor mantle components. Combined with the 87Sr/86Sr ratios of tungsten-bearing quartz veins from other studies, which scatter between 0.707153 and 0.709877, demonstrating mixing between two end-member isotopic compositions of crust and mantle. It can be concluded that the Indosinian Xiaobaishitou deposit was formed in a tectonic transition from collisional crust shortening and thickening to post-collisional extension and thinning.

Isotope dilution thermal ionization mass spectrometry (ID-TIMS) and laser ablation inductively coupled plasma mass spectrometry (LA–ICP-MS) are two popular analytical methods used to constrain the age of minerals, including cassiterite. Compared to ID-TIMS, the LA–ICP-MS analytical method is often favoured due to its simple analytical procedure and sample preparation, although the methodology constantly needs modification. Our recent paper on dating cassiterite from the Baiganhu W-Sn ore field in NW China based on LA–MC-ICP-MS and ID-TIMS methods has received a response from Dr. Leonid A. Neymark (2017). Definitely, Neymark is appreciated, and his suggestions are helpful to improve the methodology of cassiterite U–Pb geochronology. Based on a discussion on the cassiterite U–Pb dating method, we re-confirm the validity of the cassiterite U-Pb ages for the Baiganhu W-Sn ore field. The initial non-radiogenic 204Pb used in the U-Pb isochron approach can be replaced by the non-radiogenic 207Pb, because the radiogenic 207Pb decayed from 235U can be ignored in cassiterite with a high Pb content. Therefore, the cassiterite U-Pb isochron yields an age similar to that obtained from T-W concordia for the same sample, testifying the validity of the cassiterite 238U/207Pb–206Pb/207Pb isochron method.

Located in the north of Anatolia, the Pontide Orogenic Belt hosts Turkey's most important volcanogenic massive sulfide (VMS) deposits. Studies completed in the last ten years have discovered new massive sulfide deposits in the Central Pontide zone. The Zeybek VMS deposit is one of these newly-discovered deposits found in the Central Pontides. This deposit is associated with the Çangaldağ Metamorphic Complex occurring as east-west-striking tectonic slices. The Çangaldağ Metamorphic Complex is an allochthonous mass of metavolcanic, metavolcaniclastic and metaclastic rocks in the form of imbricated tectonic slices. Zeybek massive sulfide deposit is located within metaclastic rocks intercalated with mafic sills or lava flows in this complex. The major ore mineral paragenesis in the Zeybek VMS deposit comprises pyrite, chalcopyrite and sphalerite, with lower amounts of bornite, covelline, chalcocite and magnetite. With thirty thousand meters of drilling in the mineralized area, 20 million ton resources with 0.32 wt% Cu were determined. According to the wall-rock mineralization relationships, mineralization style and ore geochemistry of the Zeybek VMS mineralization, it is similar to a mafic-siliciclastic type volcanogenic massive sulfide formation. Re-Os geochronologic studies of chalcopyrites from the Cu-rich massive ore samples obtained a 178 ± 2.2 Ma (MSWD: 4.1) 187Re/188Os against 187Os/188Os isochron. Geochemical and isotopical age data associated with the Zeybek VMS deposit indicate that the mineralization occurred in an arc-back arc tectonic environment, which developed in Middle Jurassic age intra-ocean as a result of the closure of north-ward subduction that resulted the closure of the Tethys ocean. © 2019 Elsevier B.V. National Basic Research Program of China (973 Program): 2018YFC0604006 National Natural Science Foundation of China: 41572077 We would like to thank to all MTA staff who assigned in this project. We would like to thank to editor Franco Pirajno and reviewers for their constructive criticism contributions. This study has been prepared based on the project of ‘Polimetal ore exploration of Kastamonu province surounding in General Directorate of Mineral Resource and Exploration (MTA); with the project number (2013/2019)-32-13-05. Within the scope of this project we thank geological engineers Kenan ÇOŞKUN, Aysun SÖZCÜ, Aydın Olcay ÇOLAKOĞLU, Serdar KESKİN, Furkan ERDEM, Özkan YILDIRIM, Buğra GÖKÇEOĞLU, Ercüment AYSERT and Mehmet KÖKSAL, Onur TİRYAKİ for field and laboratory studies. We are grateful to geological engineers Füsun NİĞDELİ, Mustafa TOKOĞLU, and Yusuf Mehmet ERDEM and mining engineer İsmail ÖKSÜZ for completing solid model and feasibility studies related to mineralization. The National Key Research and Development Program of China ( 2018YFC0604006 ) and National Natural Science Foundation of China ( 41572077 ) have supported this study Re/Os age analizes. Appendix A

The Kalatag Cu–Zn–Au district contains a number of economically important Cu deposits in eastern Tianshan in Xinjiang, NW China. Due to the lack of precise mineralization ages, the metallogenesis of this area has long been a matter of debate. In this study, chalcopyrite Re–Os isotope methods are used to date the South Meiling Cu–Zn and Hongshi Cu deposits in the eastern part of Kalatag area. The South Meiling Cu–Zn deposit is hosted in volcanic-sedimentary rocks of the Late Ordovician to Early Silurian Daliugou Formation. The deposit consists of two parts: a concordant massive sulfide ores and discordant vein-type ores located in the footwall strata. The principal ore minerals are pyrite, chalcopyrite, sphalerite, minor tetrahedrite, galena and pyrrhotite. Gangue minerals include quartz, sericite and barite, and minor chlorite, plagioclase and carbonate minerals. The Hongshi Cu deposit represents a hydrothermal vein system hosted in the mafic volcanic rocks of Daliugou Formation. The orebodies are associated with quartz veins and controlled by subsidiary faults of the Kalatag fault. The ore-forming process can be divided into the early, middle and late stages and is characterized by quartz–pyrite, quartz–chalcopyrite–pyrite and quartz–carbonate–gypsum veins, respectively. Re–Os analyses of chalcopyrite from the South Meiling Cu–Zn deposit yield an isochron age of 434.2 ± 3.9 Ma and initial 187Os/188Os ratio of 0.647 ± 0.098 (MSWD = 0.59). Re–Os analyses of chalcopyrite from the Hongshi Cu deposit yield an isochron age of 431.8 ± 2.7 Ma and initial 187Os/188Os ratio of − 0.165 ± 0.075 (MSWD = 0.77). Since chalcopyrite is the primary copper mineral, we interpret these isochron ages as the timing of Cu mineralization, based on field geology and petrographic evidence. These results suggest that the Re–Os ages presented here provide, for the first time, a direct constraint on an early Paleozoic Cu mineralization event of the eastern Tianshan Orogen. The high initial 187Os/188Os ratios (0.647 ± 0.098) ratio of ~ 434 Ma chalcopyrite from the South Meiling deposit suggest that the metal was sourced from a two end-member mixing of crust and mantle materials. Moreover, we propose that the VMS mineral system and hydrothermal vein system of the Kalatag district were related to the south-dipping subduction of the Kalamaili oceanic plate during the Late Ordovician–Silurian.

The Zhifang Mo deposit is located in the northeastern Qinling Orogen along the southern margin of the North China Craton. The deposit represents a quartz-vein system hosted in the Mesoproterozoic Xiong'er Group volcanic rocks. We identify three hydrothermal stages (early, middle and late), characterized by veinlets of quartz–pyrite, quartz–molybdenite–pyrite–chalcopyrite–galena–sphalerite, and quartz–carbonate assemblages, respectively. Five molybdenite samples from the Zhifang deposit yield Re–Os ages ranging from 241.2 ± 1.6 Ma to 247.4 ± 2.5 Ma, with an isochron age of 246.0 ± 5.2 Ma (2σ, MSWD = 7.4), and a weighted mean age of 243.8 ± 2.8 Ma (2σ, MSWD = 5.5). The Re–Os age shows that the Mo mineralization occurred during the Indosinian Orogeny, and suggests that the mineralization is unrelated to the Yanshanian magmatism or the Paleo-Mesoproterozoic volcanic–hydrothermal event. This study also reports a new Sr–Nd–Pb isotope dataset from ore sulfides in an attempt to constrain the source of the ore-forming fluids. Ten sulfide samples from middle stage of the Zhifang Mo deposit yield I Sr (t) ratios of 0.710286–0.711943, with an average of 0.711004; e Nd (t) values between − 19.5 and − 14.8, with an average of − 16.7; and ( 206 Pb/ 204 Pb) i , ( 207 Pb/ 204 Pb) i and ( 208 Pb/ 204 Pb) i ratios of 17.126–17.535, 15.374–15.466 and 37.485–37.848, with averages of 17.380, 15.410 and 37.631, respectively. One pyrite from the early stage yield I Sr (t) of 0.722711–0.722855, with an average of 0.722783, which is higher than those of the middle stage sulfides and suggests equilibration with wallrocks. The e Nd (t) values are in the range of − 17.3 to − 16.6 with a mean at − 17.0; and ( 206 Pb/ 204 Pb) i , ( 207 Pb/ 204 Pb) i and ( 208 Pb/ 204 Pb) i ratios are 17.386, 15.405 and 37.622, respectively. The ore sulfides show higher Pb-isotope ratios, higher e Nd (t) and lower I Sr (t) values than the host rocks. The results suggest that the ore-forming fluids had lower I Sr (t), and higher e Nd (t) values than the ore sulfides, and were possibly sourced from the Dengfeng Complex. The southward subduction of the North China Craton beneath the Huaxiong Block during the Triassic was possibly responsible for the formation of the Waifangshan orogenic Mo system.

Tourmaline is widespread in the Baiganhu W–Sn deposit, Xinjiang Province, NW China. In this study, electron microprobe analysis reveals that tourmaline in the Baiganhu deposit belongs to the alkali and X-site group with low Ca and moderate X site vacancy, all beyond the confines of schorl–dravite series, with Na/(Na + Ca) and Fe/(Fe + Mg) ratios ranging from 0.769 to 0.965 and 0.518 to 0.822, respectively. In chemical discrimination diagrams, the tourmaline samples plot in the fields of Li-poor granite, associated with Al-saturated metapelites and metapsammites. The tourmaline cores are depleted in Mg, Ca, Ti, but enriched in Al and Fe compared to the rims. Substitution mechanisms for the compositional variations are dominantly due to MgFe− 1, □Al(NaFe)− 1, □Al(NaMg)− 1, and AlO(Fe− 1(OH))− 1 exchange vectors. The δ11B values of the tourmalines range from − 12.9 to − 7.9‰, with a slight variation between cores and rims, which reflect a common boron source, and also indicate that the tourmaline crystallized during a single magmatic-hydrothermal event related to monzogranite. Tourmaline is a valuable prospecting indicator of W–Sn mineralization.

Introduction Granulocytic sarcoma (GS) is a commonly occurring tumor comprising immature myeloid cells, which are usually related to acute or chronic myelocytic leukemia. The tumor rarely precedes leukemia without bone marrow involvement and is called primary GS. Although primary GS can occur in any body part, the involvement of the oral cavity is uncommon. Patient concerns A 49-year-old woman hospitalized at the Department of Plastic and Maxillofacial Surgery presented with a growing mass in her left maxillary hard palate dating two months back. No obvious physical findings were noted during general examination. She was diagnosed with an oral ulcer at a local clinic, and received antibiotics. However, the symptoms did not improve; the mass became bigger and painful. Diagnosis An incisional biopsy of the oral mass was performed, the immunohistochemistry showed that the tumor cells tested positive for myeloperoxidase, CD4, BCL-2, KI-67. Bone marrow aspiration was negative for malignant cells, and the laboratory test results revealed only monocytosis. Standard bone marrow cytogenetic analysis showed a normal karyotype and leukemia-related fusion gene detection was normal. Therefore, the final diagnosis was intraoral primary GS. Interventions The patient was treated with a chemotherapy regimen based on idarubicin and cytarabine arabinoside. Outcomes After 2 cycles of idarubicin and cytarabine arabinoside regimen chemotherapy, the patient achieved complete remission. The tumor was barely visible in the left maxillary hard palate. There has been no evidence of disease spread and progression after 1 year of follow-up. Conclusions Careful morphological and immunohistochemical analyses, correlating with clinical data are necessary to establish the diagnosis of oral primary GS. Early aggressive systemic chemotherapy can effectively relieve symptoms, significantly reducing primary GS conversion into acute myelocytic leukemia and prolonging overall survival.

The Xiaoriquanzi volcanogenic massive sulfide (VMS) Cu-Zn deposit occurs at the western part of the Paleozoic Dananhu-Haerlik arc in the eastern Tianshan, Xinjiang, China. Due to a lack of precise mineralization ages, the metallogenesis of the deposit has long been debated. In this study, systematic geochronological methods are used to constrain the mineralization age of the deposit. The deposit is hosted in the Xiaorequanzi Formation volcanic-sedimentary rocks. The orebodies occur as clusters of lenticular bodies with or without banding, and they are controlled by the NW-trending acticline. The ore types contain massive, banded, laminated and chlorite-enriched ores as well as vein-type, veinlet-dissemination and dissemination ores. In this study, Re-Os dating of the chalcopyrite from the Xiaorequanzi deposit yields an isochron age of 354 ± 11 Ma and initial 187Os/188Os ratios of 0.39 ± 0.14, which is consistent with the zircon U-Pb ages of ore-hosted tuff sandstone and dacite at 357.3 ± 2.4 Ma and 359.5 ± 3.4 Ma, respectively. Zircon U-Pb dating reveals that the mineralized granite porphyry formed at 354.7 ± 3.2 Ma, and this age is similar to the exhalative syn-sedimentary mineralization age (354 ± 11 Ma). Thus, precise geochronologic studies reveal that the seafloor volcanic hydrothermal system formed exhalative syn-sedimentary mineralization in the local extensional basin of the Dananhu-Haerlik arc during the Early Carboniferous (354–357 Ma). From Early Silurian to Carboniferous, two epochs VMS and porphyry deposits alternately formed in Dananhu-Haerlik long-lived arc. This reveals complicated arcs-basins tectonic transformation at the island arc setting.

The Chinese East Tianshan is the easternmost sector of the Tianshan Mountain Range in the Central Asian Orogenic Belt (CAOB), and accommodates several events of magmatism, crustal growth and mineralization. The Kalatag arc is unique in the East Tianshan due to its widespread Early Paleozoic volcanic rocks, which offers a special opportunity to study the Early Paleozoic Cu-dominant mineral systems in island arc setting. In this region nine deposits have been discovered in recent years. These deposits occur in Paleozoic volcanic rocks between the Kalatag Fault and Kabei Fault, and can be divided into six mineral systems, i.e., VMS Cu-Zn, epithermal Cu, porphyry Cu-Au, skarn Fe-Cu, magmatic Cu-Ni sulfide and hydrothermally overprinted deposits. Among them, VMS, epithermal, porphyry-skarn and magmatic Cu–Ni sulfide mineralization are distributed in the southeastern, central, northwestern and westernmost Kalatag, respectively. The mineralization and associated intrusive rock ages can be clustered into four episodes in the Kalatag arc, i.e., Late Ordovician–Silurian (ca. 450–430 Ma), Middle Devonian (ca. 390–380 Ma), Late Carboniferous (ca. 320–300 Ma) and Permian (ca. 280 Ma). Here, Paleozoic granitoids show similar geochemistry and isotopic features. All Paleozoic granitoids plot in the subalkaline field, and predominantly tholeiitic to calc-alkaline series, with enrichment of large-ion lithophile elements and depletion of high-field-strength elements. These granitoids plot in a volcanic arc fields in tectonic discrimination diagrams, which are characteristic of an island arc setting. The fluid inclusions in porphyry and skarn system are characterized by high-temperature, high-salinity, low-content of CO2, whereas epithermal system represented by low-temperature, low-salinity, low-content of CO2, and the VMS system can be described as medium-temperature, medium low-salinity, CO2-bearing fluid. H-O isotopic data suggest that ore-fluids were sourced from a mixing fluid between magmatic and meteoric water. S-Pb isotopic data show that the sulfur mainly came from magma or ore-hosting igneous rocks. The Yudai porphyry Cu-Au deposit, the Hongshi epithermal Cu deposit and the Honghai Au-rich VMS Cu-Zn deposit formed at the same time related to a subduction environment. The Early Paleozoic VMS mineralization is generally overprinted by late magmatic hydrothermal fluids, which may be due to multiple accretionary orogeny in Kalatag island arc. We propose that the north-dipping subduction of the Paleo-Tianshan Ocean or south-dipping subduction of the Junggar Ocean during Late Ordovician–Silurian, which may led to the development of Yudai porphyry copper, Hongshi epithermal copper and Honghai VMS copper-zinc deposits in the Kalatag arc. After that, north-dipping subduction of the Paleo-Tianshan Ocean resulted to the formation of the Middle Devonian (ca. 390–380 Ma) and Late Carboniferous (ca. 320–300 Ma) Cu mineralization. Finally, the Permian (ca. 280 Ma) magmatic copper–nickel sulfide deposits associated with ultramafic–mafic complexes developed in post-collisional-extension setting, part of a Large Igneous Province (LIP) event associated with mantle plume upwelling.

The Taihua Complex is an important metamorphic rock suite at the southern margin of the Trans-North China Orogen and hosts important mineral deposits. Its protolith and metamorphic ages are still controversial. The 1.85-Ga Longmendian Mo deposit in the Xiong’ershan is hosted by the khondalite series of the Duangou Formation, Taihua Complex. Three kinds of rocks are collected for SHRIMP/CAMECA U–Pb dating, including the meta-sedimentary rock that occurred as wallrock, the Mo-mineralized meta-gabbro that intruded the meta-sedimentary rock, and the leucosome that cut both the meta-sedimentary rock and the meta-gabbro. Zircon U–Pb analyses reveal that the precursor of the meta-sedimentary rock was crystallized between 2200 ± 4 and 2742 ± 18 Ma (with most before 2500 Ma), whereas the protolith of the meta-gabbro was formed at 2178 ± 6 Ma. Anatexis zircons in the leucosome yield a weighted mean age of 1943 ± 8 Ma that is indistinguishable with the metamorphic age of the meta-gabbro (1952 ± 4 Ma). In the intensively altered meta-gabbro, hydrothermal titanites were formed by at least two pulses of crystallization at 1940 ± 7 Ma and 1916 ± 9 Ma, respectively. The new data reveal that the khondalite series of the Duangou Formation were formed between 2200 Ma and 2178 Ma. The results are inconsistent with previous subdivision of the Taihua Complex into the Upper Taihua and Lower Taihua Subgroup. Instead, they fit well with the tripartitite divison into the Beizi Group (3.0–2.55 Ga), the Dangzehe Group (2.55–2.3 Ga) and the Shuidigou Group (2.3–2.1 Ga). Compiling zircon U–Pb ages indicate that in the Trans-North China Orogen, the 1.95 Ga and 1.85 Ga metamorphic events are widespread and prominent.

The Tumen Mo–F deposit is located on the southern margin of the North China Craton in central China. The deposit represents a fluorite-vein system hosted by carbonate rocks in the Neoproterozoic Luanchuan Group. Previous studies identify four hydrothermal stages at the deposit characterized by: Stage 1 veins of white fluorite, Stage 2 purple fluorite–molybdenite–pyrite (–galena), Stage 3 calcite–galena–pyrite–sphalerite (–chalcopyrite), and Stage 4 carbonate assemblages. The δ 34 S values for sulfides from the Tumen deposit range between −7.1 and 5.0‰, with a bimodal distribution. The Stage 2 sulfides have δ 34 S values of −2.7 to 5.0‰ that are similar to that of granitic rocks, but different from andesite in the Xiong’er Group, amphibolitic gneiss in the Taihua Supergroup and the carbonaceous shale and chert in the Luanchuan Group. The near-zero δ 34 S values indicate a possible magmatic source for the Stage 2 fluids. However, the δ 34 S values for the Stage 3 sulfides have negative mean and a restricted range from −7.1 to −4.6‰, which is different from that of the Xiong’er Group and Taihua Supergroup. The 34 S-depleted fluid for the Stage 3 sulfides was inherited from the host rocks in the Luanchuan Group with low δ 34 S values of −12.4 to 7.2‰. New Sr–Nd–Pb isotope data obtained from fluorite at Tumen indicate that the fluorite has higher Pb-isotope ratios, higher ɛ Nd(t) and lower I Sr (t) values than the host rocks. The results suggests that the ore-forming fluids had ɛ Nd(t) > −4.8, I Sr (t) 206 Pb/ 204 Pb) i > 17.998, ( 207 Pb/ 204 Pb) i 208 Pb/ 204 Pb) i ɛ Nd(t) = −3.8 to −1.3, I Sr (t) = 0.7006–0.7061 for Neoproterozoic syenite in Qinling Orogen. This suggests that the deposit is related to a magmatic hydrothermal vein system associated with Neoproterozoic syenitic magmatism.

The 1.85 Ga Longmendian Mo deposit in East Qinling is the oldest Mo system recognized in China. It is unique for three reasons: (1) quartzofeldspathic orebodies are away from any intrusion or fault, (2) it is closely associated with migmatitic rocks, and (3) it has remarkably high Re content in molybdenite (504 to 1660 ppm). The origin of the deposit is poorly constrained. In the Longmendian deposit, strong Mo mineralization is always associated with hydrothermally altered migmatitic amphibolites. To probe into ore genesis, detailed fluid inclusion studies are carried out on both mineralized migmatitic amphibolites and ore-barren rocks. Four compositional types of fluid inclusions are observed, including CO 2 ± CH 4 (PC-type), CO 2 –H 2 O (C-type), daughter mineral-bearing (S-type) and H 2 O–NaCl (W-type). Quartz in mesosome and melanosome of mineralized migmatitic amphibolites contains all of the four types of inclusions. Measurements of immiscible inclusion assemblages in the ores constrain the Mo-mineralization temperatures and pressures to be 225–390 °C and 114–265 MPa, respectively. Primary fluid inclusions in barren migmatitic gneisses are dominated by S-type, and minor of C- and PC-types which are identical to those in the leucosome of migmatitic amphibolites. These inclusions yield lower homogenization temperatures than those in the mineralized mesosome and melanosome of migmatitic amphibolites, suggesting that the ore-causative, injected melts should have higher temperatures and originated from depths. Such features of the ore-forming fluids indicate that the Longmendian deposit was a migmatitic-hydrothermal system caused by high-temperature melt injection. This interpretation can also be supported by the observations below: (1) tourmaline is abundant in melanosome, but absent in mesosome; (2) the consistent quartzofeldspathic composition of leucosome is independent of mesosome; (3) leucosome in migmatitic amphibolite crosscuts each other; (4) halite-bearing fluid inclusions are prevalent in studied samples, which is the feature of granitic rocks, instead of the scenarios of in situ migmatites; and (5) the trapping temperatures of fluid inclusions in mineralized migmatitic amphibolite are much lower than those required for partial melting, but higher than those obtained from barren migmatitic rocks.

The Tumen molybdenite–fluorite vein system is hosted by carbonate rocks of the Neoproterozoic Luanchuan Group, located on the southern margin of the North China Craton (NCC) in central China. Previous studies divided the mineralization into four stages according to the crosscutting relationships between veinlets and their mineral assemblages. In this contribution, two distinctive types of fluorite mineralization are recognized: 1) the first type (Type 1) includes colourless, white or green fluorite grains present in Stage 1 veins; and 2) the second type includes Type 2a purple fluorite present in Stage 2 veins and does not coexist with sulfides, and Type 2b purple fluorite crystals associated with sulfides in Stage 2 veins. The rare earth element (REE) content in the fluorite ranges between 13.8 and 27.9 ppm in Type 1, 16.9 and 27.2 ppm in Type 2a, and 42.5 and 75.1 ppm in Type 2b, which suggests that the fluorite was precipitated from acidic fluids (given that REEs are mobile in saline HCl-bearing fluids at high temperature (~ 400 °C)). Comparing the REE chemistry of the Stage 1 against Stage 2 fluorite, the LREE/HREE ratios decrease from 9.8 to 4.0, La/Yb ratios decrease from 16.0 to 6.9 and La/Ho ratios decrease from 10.2 to 3.0, indicating that the hydrothermal process was at high-T and low-pH conditions. The Eu/Eu* ratios in the fluorite decrease from 1.11 ± 0.35 for Type 1 through 0.89 ± 0.19 for Type 2a to 0.75 ± 0.17 for Type 2b, suggesting a gradual increase in oxygen fugacity ( f O 2 ) and pH of the mineralising fluid. The Tb/Ca, Tb/La and Y/Ho ratios of the fluorite types indicate that they were formed from the interaction between magmatic fluids and carbonate wallrocks. The fluorite samples show similar REE + Y (REY) patterns to those of dolostone units in the Luanchuan Group and the nearby Neoproterozoic syenite, suggesting that the REY in the fluorite was mainly sourced from the host-rocks, although the syenite could be an additional minor source.

The Yindonggou Ag–Au(–Pb–Zn) deposit is hosted by metamorphosed volcanic rocks of the ca. 740–760 Ma Wudangshan Group in the Proterozoic Wudang Block of the southern part of the Qinling Orogen, central China. The deposit consists of a series of mineralized quartz veins located in the Yindongyan Anticline. Based on the mineral assemblages and cross-cutting relationships of quartz veins, the deposit can be divided into: (1) early fine-grained quartz–sphalerite–galena veins; (2) fine-grained quartz–silver–gold veins containing minor amounts of pyrite; (3) coarse-grained quartz veins with minor amounts of galena, sphalerite, and chalcopyrite; and (4) late ankerite–quartz veins. Most of the Pb–Zn mineralization formed during the early (Stage 1) veins followed by the deposition of Ag–Au mineralization in the Stage 2 veins. The δ18O value for the ore-forming fluids decreases from 6.6–9.4‰ in the Stage 1 veins through 3.6–4.9‰ in the Stage 2 veins to −1.2‰ to 0.4‰ in the Stage 3 veins (the δ18O values could not be determined for the Stage 4 veins). Furthermore, the δD values are −74‰ for the Stage 1 veins, −95‰ to −56 ‰ for the Stage 2 veins, and −48‰ to −73‰ for the Stage 3 veins. The δ13C values for ankerite in the Stage 4 veins are between −2.9‰ and −1.1‰. The δD vs. δ18OH2O plot for these values indicates that there was a shift from metamorphic fluids during the formation of the early veins to meteoric fluids during the formation of the later veins at the deposit. The H–O–C isotope systematics also indicate that the ore fluids forming the deposit were probably initially sourced from metamorphic dehydration of volcanic-carbonate rocks in the ca. 740–760 Ma Wudangshan Group and with time gradually mixed with meteoric water by Stage 4. The δ34S values for sulphides from the deposit range from −0.9‰ to 7.1‰ in the Stage 1 veins, 3.8‰ to 5.0‰ in the Stage 2 veins, and 2.4‰ to 11.3‰ in the wallrocks. Sulphides from the mineralized Stage 1 veins yield 206Pb/204Pb ratios of 16.44–16.6, 207Pb/204Pb ratios of 15.25–15.5, and 208Pb/204Pb ratios of 36.4–36.98. Five pyrite samples from the Stage 2 veins yield 206Pb/204Pb ratios of 16.475–16.529, 207Pb/204Pb ratios of 15.346–15.395, and 208Pb/204Pb ratios of 36.49–36.616. Both the S and Pb isotope ratios are between the ratios for units in the Wudangshan Group and mantle but differ from other lithological units in the Wudang Block, which suggest that the mineralized fluids interacted with both the Wudangshan Group and deep-seated sources. Thus, we suggest that the original ore-forming fluids are metamorphic in origin, and the metal deposition resulted from fluid mixing. From the characteristics observed, the Yindonggou Ag–Au(–Pb–Zn) deposit can be classified as an orogenic-type deposit generated during the Triassic Qinling Orogeny resulting from northward oceanic plate subduction along the Mian-Lue Suture. Copyright © 2014 John Wiley & Sons, Ltd.

The East Qinling region in central China, hosting several tens of Mesozoic magmatic-hydrothermal Mo deposits, is one of the largest molybdenum belts in the world. The Zhifang Mo deposit is hosted in volcanic rocks of the Xiong'er Group in the Waifangshan area, Qinling Orogen. Previous studies variously correlated the mineralization in this deposit with Yanshanian magmatism or Palaeo-Mesoproterozoic volcanic-hydrothermal events. The orebodies are associated with quartz veins and controlled by subsidiary faults of the Machaoying Fault. The ore-forming process can be divided into the early, middle and late stages and is characterized by quartz-pyrite, quartz-polymetallic sulphide and quartz-carbonate veins, respectively. The early-stage quartz is structurally deformed, suggesting a compressional tectonic regime; the middle-stage sulphides fill the fractures of the early-stage assemblages and show no deformation, suggesting a tensional setting; the late-stage veins mostly infill the open-space fissures. Three types of fluid inclusions (FIs) are identified at the Zhifang deposit: H2O-NaCl (W-type), CO2-rich (C-type) and daughter mineral-bearing inclusions (S-type). Fluid inclusions of early-stage quartz homogenize between 380 and 470 °C, with salinities ranging from 0.4 to 9.6 wt.% NaCl equiv., whereas the late-stage calcite contains only the W-type FIs with homogenization temperatures of lower than 240 °C, and salinities of 0.4–8.7 wt.% NaCl equiv. This indicates that the ore fluid system evolved from CO2-rich, probably metamorphic hydrothermal to CO2-poor, meteoric fluid. All three types of FIs can be observed in the middle-stage quartz, and even in the microscopic domain of a crystal, suggesting that this heterogeneous association was trapped from a boiling fluid system. These FIs homogenized at temperatures ranging from 250 to 360 °C and display two salinity clusters of