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For reservoirs with complex non-Gaussian geological characteristics, such as carbonate reservoirs or reservoirs with sedimentary facies distribution, it is difficult to implement history matching directly, especially for the ensemble-based data assimilation methods. In this paper, we propose a multi-source information fused generative adversarial network (MSIGAN) model, which is used for parameterization of the complex geologies. In MSIGAN, various information such as facies distribution, microseismic, and inter-well connectivity, can be integrated to learn the geological features. And two major generative models in deep learning, variational autoencoder (VAE) and generative adversarial network (GAN) are combined in our model. Then the proposed MSIGAN model is integrated into the ensemble smoother with multiple data assimilation (ESMDA) method to conduct history matching. We tested the proposed method on two reservoir models with fluvial facies. The experimental results show that the proposed MSIGAN model can effectively learn the complex geological features, which can promote the accuracy of history matching.

DEAD-box RNA helicases regulate growth, development, and stress response of plants. In this study, a gene encoding a DEAD-box RNA helicase, GhRH32, was identified in upland cotton (Gossypium hirsutum L.). Gene silencing experiments demonstrated that GhRH32 functions as a negative regulator in cold tolerance. ATPase activity and ATP content analysis revealed that GhRH32 regulates ATP supply. Subcellular localization analysis showed that GhRH32 is targeted to the nucleus. Furthermore, we found that GhRH32 interacts with GhCBF, and the expression of CBF pathway genes increased in plants that were subjected to virus induced gene silencing (VIGS). Taken together, our results indicate that GhRH32 could be a potential molecular target to improve cold tolerance in plants.

The Tangjiaping Mo deposit is located in the Dabie Shan in eastern China. Molybdenum (Mo) mineralization mainly occurs as veinlets in the Tangjiaping granite porphyry, which is featured by the development of potassic-silicic-, phyllic- and propylitic alterations. The Mo-mineralized granite porphyry yields a zircon U Pb age of 118.1 ± 0.8 Ma (MSWD = 1.6, 2σ, n = 24), and may have formed under post-collision extensional tectonics after the Yangtze–North China collision. The Tangjiaping granite porphyry is characterized by the enrichments of LILEs and LREEs, depletions of Ba, Nb, Ta, Sr, P, Ti and HREEs, and negative Eu anomaly. Zircons from the granite porphyry yield negative eHf(t) of − 15.3 to − 9.9, with TDM2(Hf) ages of 1.80 to 2.14 Ga. The 206Pb/204Pb, 207Pb/204Pb and 208Pb/204Pb of the granite porphyry and its K-feldspar are 16.842–17.342, 15.388–15.439 and 37.706–38.260, respectively, while those of the sulfides are 17.090–17.832, 15.420–15.510, and 37.550–38.026, respectively. The δ34S of these sulfides exhibit a relatively narrow range of 3.2–4.9‰, with an average of 4.0‰. The Hf Pb S isotopic signatures indicate that the granite porphyry and the ore-forming materials at Tangjiaping were mainly derived from the partial melting of both the Southern Dabie Complex and the Precambrian basement of the North China Craton.

The Dabie Shan in central East China is a collisional orogenic belt suturing the North China and Yangtze blocks. It was formed by Jurassic-Early Cretaceous continental collision , following the Triassic closure of the northernmost paleo-Tethyan Ocean. In the area, at least ten porphyry Mo systems have been discovered, including two giant ones, with a total reserve of > 3 Mt Mo metal. The porphyry-type Mo mineralization mainly occurred during 156–110 Ma, in the post-collisional extension setting. The location of Mo deposit is controlled by NW- and NNE-trending faults, mostly in the south of the Gui-Mei Fault suturing the North China and Yangtze blocks. Mo mineralization is generally associated with the Yanshanian high-K calc-alkaline metaluminous-peraluminous granitic intrusions, with orebodies being located in the intrusions and/or host-rocks. The hydrothermal ore-forming process generally includes four stages, with the initial ore-forming fluids being featured by high temperature, high salinity and CO 2 -rich. Geochemical signatures indicate that the ore-causative magmatism in the Dabie Shan mainly originated from either the northern or southern Dabie complex, but mixed with the Precambrian rocks of the North China block, except for the Tianmugou porphyry system which shares more similar geological and geochemical characteristics with the porphyry Mo deposits in eastern Qinling Orogen. We also develop a scissor-style intracontinental subduction model to interpret the differences in spatial distribution, geneses, and geochemical and geological characteristics between the Mo deposits in Dabie Shan and Qinling Orogen. In our model, the basement of the North China Block southwardly underthrusted beneath the Dabie Shan, possibly along the Gui-Mei Fault; whilst the basement of the Yangtze Block northwardly underthrusted beneath the Qinling Orogen; and the inferred Minggang-Xinyang fault zone served as a dextral strike-slip fault zone in the North China Block, but acted as a sinistral transpressional fault zone within the orogenic area. Compared to the subduction- or Endako- and rift- or Climax-types of porphyry Mo deposits, the porphyry Mo deposits in the Dabie Shan are unique because of their crustal source for the magma and ore-forming materials, and as such are assigned to the Dabie- or collision-type. Hence we develop a new global tectonic model for porphyry Mo deposits of three types, showing their genetic tectonic settings .

Southwest (SW) China hosts more than 26 Mo (Mo-only, Mo-dominated and Mo-bearing) deposits with a total reserve of > 2.5 Mt Mo metal. The region has become one of the most important Mo mineral provinces in China. These Mo deposits are usually fault-controlled, and are located mainly in: (1) Lhasa Terrane, characterized by widely distributed Yanshanian–Himalayan igneous rocks; (2) Qiangtang Terrane, composed by Proterozoic and Early-Paleozoic crystalline basement and Devonian to Jurassic cover rocks; (3) East Kunlun Terrane, comprising Precambrian metamorphic rocks intruded by Paleozoic and Mesozoic granitoid plutons; (4) West Kunlun Terrane, characterized by Precambrian metamorphic basement, Paleozoic metasedimentary rocks, and Early-Paleozoic and Carboniferous–Triassic arc-type plutons; and (5) Yidun arc, composed by Middle and Upper Triassic volcanic–sedimentary successions. The Mo mineralization styles are dominated by porphyry-type, but also contain porphyry-skarn, skarn and porphyry-quartz vein types. Orebodies are vein-type or lensoidal, and are hosted by a variety of metamorphic, volcanic, granitic and sedimentary rocks of different ages. Fluid-rock interactions are exemplified by alteration zonation, which usually grades from an innermost potassic alteration zone, via a silicic/sericite alteration zone, to an outermost propylitic alteration zone. The initial high-temperature ore-forming fluids are magmatic in origin, and contain CO 2 -bearing fluid inclusions. The initial ore-forming fluids would have then evolved to low-temperature, low-pressure, low-salinity and CO 2 -poor (with meteoric water input) at the late alteration/mineralization stage. Causative granitoids for these Mo deposits have relatively high SiO 2 , K 2 O and Al 2 O 3 , and low TiO 2 and MgO, showing a metaluminous to peraluminous high-K calc-alkaline to shoshonitic affinity. These granitoids exhibit significant depletions in Ba, Nb, Ta, P and Ti, and enrichments in Rb, Th, U and K. It is suggested that they were originated from partial melting of a lower rejuvenated crust, as evidenced by their Sr-Nd-Pb isotopic signatures. The Mo deposits in East and West Kunlun were formed in the Triassic (ca. 258–214 Ma), related to the Paleo-Tethys Ocean subduction and the subsequent continental collision. Major Mo mineralization in the Qiangtang and Lhasa terranes mainly occurred during the syn-collisional compression to post-collisional extension transition of the Qiangtang–Lhasa (ca. 43–35 Ma) and India–Asia (ca. 30–14 Ma) collisions, respectively. The Late-Cretaceous Mo mineralization (ca. 88–73 Ma) in the Yidun arc was formed during the late- or post- Lhasa–Qiangtang collision setting, or the intraplate extension led by the post-Himalayan escape tectonics. The wide range of molybdenite Re contents in these major SW Chinese Mo deposits indicates remarkable differences in metal, fluid sources and ages.

The Qian'echong Mo deposit is a giant porphyry deposit in the Dabie Shan of eastern China. Molybdenum (Mo) mineralization mainly occurs as numerous veinlets in altered schists, with the development of potassic, phyllic, argillic, and propylitic alteration assemblages. A buried granite porphyry stock and locally exposed dikes are spatially and genetically related to the Mo mineralization. Zircon crystals from exposed quartz porphyry, rhyolitic porphyry, and granite porphyry dikes, as well as a buried granite porphyry dike yield weighted average 206 Pb/ 238 U ages of 128.9 ± 1.1 Ma (MSWD = 0.30, 2σ, n = 13), 127.42 ± 0.94 Ma (MSWD = 0.58, 2σ, n = 17), 127.44 ± 0.98 Ma (MSWD = 1.6, 2σ, n = 16), and 126.6 ± 1.4 Ma (MSWD = 0.67, 2σ, n = 15), respectively. The buried granite porphyry stock yields a zircon U–Pb weighted average age of 124.7 ± 1.6 Ma (MSWD = 1.5, 2σ, n = 16), which is slightly younger than the exposed dikes, but within error of the age of the buried granite porphyry dike. Five molybdenite samples from the ores yield Re–Os isotope ages of 123.31 ± 1.02 to 128.49 ± 1.40 Ma, which are consistent with the U–Pb ages for the igneous rocks These age data constrain magmatic–hydrothermal activity at the Qian'echong Mo deposit to a period of about six million years from 129 to 123 Ma. This period overlaps the recognized regional Mo mineralization event in the Dabie Shan of 142–111 Ma, which took place during the post-collisional tectonism subsequent to amalgamation of the Yangtze and North China blocks. The Qian'echong granite porphyry stock and dikes have high contents of SiO 2 , K 2 O and Al 2 O 3 , and low contents of TiO 2 , MgO and CaO, showing a peraluminous high-K calc-alkaline to shoshonite affinity, with obvious LREE enrichment and a negative Eu anomaly. The rocks have a high initial 87 Sr/ 86 Sr of 0.70729 to 0.71788 and highly negative e Nd( t ) values of − 16.2 to − 26.1, with T DM2 (Nd) ages of 2.24 to 3.03 Ga. Their ( 206 Pb/ 204 Pb)t, ( 207 Pb/ 204 Pb)t, and ( 208 Pb/ 204 Pb)t values range from 16.017 to 16.701, 15.252 to 15.368, and 37.095 to 37.578, respectively. This Sr–Nd–Pb isotopic signature indicates that the causative granitic intrusions for the Qian'echong deposit were mainly melts with components of both the northern Dabie complex and the Taihua and Xiong'er Groups that are part of the Precambrian basement of the North China block. The melts were generated during the tectonic extrusion of the Dabie Shan and their emplacement onto the basement of the North China block. The Qian'echong Mo deposit is unique based upon the crustal source for the causative porphyry, localization of most mineralization in the surrounding schist country rocks, and the CO 2 -rich ore-forming fluid. Thus we propose the Qian'echong deposit to represent a new sub-type of porphyry Mo deposit, herein termed collisional- or Dabie-type porphyry deposit.

The Donggou Mo deposit in the eastern Qinling area, China, is a giant porphyry system discovered based on a targeting concept by using the tectonic model for collisional orogeny, metallogeny and fluid flow (CMF model). Mo mineralization is associated with the Donggou aluminous A-type granite porphyry and was formed during the Early Cretaceous in a tectonic regime of continental extension. The orebodies mainly occur as numerous veinlets in the host-rocks. Hydrothermal ore-forming processes include at least three stages, characterized by veinlets of (1) quartz + K-feldspar + minor molybdenite, (2) quartz + molybdenite ± beryl and (3) quartz + carbonate + fluorite. Three types of fluid inclusions (FIs) are distinguished in quartz and beryl in stages 1 and 2, i.e., aqueous (W-type), carbonic–aqueous (C-type) and solid-bearing (S-type), with only aqueous FIs observed in stage 3 minerals. S-type FIs contain variable daughter minerals including halite, chalcopyrite, calcite and an unidentified transparent crystal, but only halite can dissolve during heating. Halite-bearing S-type FIs are mainly homogenized by halite dissolution at 182–416 °C, corresponding to salinities of 30.9–49.2 wt.% NaCl equiv.; minor halite-bearing S-type FIs are homogenized to liquid at 190–360 °C via vapor disappearance, with salinities of 29.1–36.2 wt.% NaCl equiv. Other FIs in minerals of stages 1, 2 and 3 are homogenized at temperatures of 341–550 °C, 220–440 °C and 125–225 °C, with salinities of 8.0–18.3, 5.3–16.8 and 0.5–7.3 wt.% NaCl equiv., respectively. The estimated minimum trapping pressures are up to 141 MPa in stage 1 and up to 81 MPa in stage 2, respectively, corresponding to an initial mineralization depth of no less than 5 km. The quartz in veinlets yields δ 18 O values of 8.5–10.0‰, corresponding to δ 18 O H 2 O values of − 2.9 to 5.9‰, while the δD H 2 O values of fluid inclusions range from − 59 to − 82‰. These data suggest that the ore fluids forming the Donggou deposit changed from high-temperature, high-salinity, CO 2 -rich magmatic to low-temperature, low-salinity and CO 2 -poor meteoritic fluids via boiling and mixing, resembling those of other magmatic–hydrothermal systems in Qinling Orogen and Dabie Shan. This supports the notion that the porphyry systems generated in a post-collisional tectonic setting were initially CO 2 -rich, as indicated by abundant C-type and CO 2 -bearing S-type fluid inclusions.

The giant Dongshengmiao Zn–Pb–Cu deposit is located in the Langshan district, northern China. The ores are hosted within a Proterozoic rift sequence, which underwent lower greenschist facies metamorphism and shear deformation during development of Early Cretaceous intraplate orogenic belt. Northwest-dipping thrust faults, which share similar orientations and dip angles with the orebodies, are well developed in the mining area. Syngenetic stratabound sulfides were formed during the Proterozoic rifting event, but syngenetic ore textures have seldom been preserved except for some pretectonic fine-grained pyrite. Petrological observation, 39 Ar/ 40 Ar geochronology, combined with previous isotopic and fluid inclusion studies indicates that significant Zn–Pb–Cu remobilization took place as a result of thrust faulting associated with metamorphic devolatilization of ore-hosting rocks at ca. 136 Ma, coeval with the intraplate orogeny and regional crustal shortening. Sulfides were redistributed in shear structures or along grain boundaries of ore-hosting carbonates, and Fe-rich carbonates were ideal sites for Zn–Pb–Cu precipitation.

Regional intra-arterial chemotherapy (RIAC) is a potential alternative treatment for advanced pancreatic cancer (APC) with fewer adverse effects than other treatment options. However, specific biomarkers to determine the prognosis of patients with APC have thus far, been unsatisfactory. Glypican-1 (GPC1) in exosomes has been identified as an early diagnostic biomarker for pancreatic adenocarcinoma. The aim of the present study was to investigate whether the presence of GPC1 in extracellular vesicles (EVs) could serve as a predictor of RIAC outcome for patients with APC. EVs in circulation were isolated and the percentage of GPC1+ EVs was measured using flow cytometry. Compared with healthy individuals, the levels of GPC1+ EVs were significantly increased in patients with APC (P

The Donggebi giant porphyry Mo deposit in Hami city, Xinjiang Province, NW China, was formed in the Triassic in the Jueluotage metallogenic belt of Eastern Tianshan. Mo mineralization is associated with the Donggebi porphyritic granite, occurring as numerous stockworks in the altered wall rocks. The hydrothermal ore-forming process can be divided into four stages, from early to late, characterized by veinlets composed of (1) quartz + K-feldspar ± beryl ± pyrite ± tourmaline; (2) quartz + molybdenite ± K-feldspar ± tourmaline ± fluorite ± beryl; (3) quartz + polymetallic sulphides ± fluorite; and (4) quartz + calcite ± fluorite. Three types of fluid inclusions (FIs) are distinguished in this study based on petrographic and microthermometric criteria, i.e. carbonic (C-type), aqueous (W-type) and solid-bearing fluid inclusions (S-type). All three types of FIs can be observed in the quartz, beryl and fluorite formed in stages 1, 2 and 3, while the stage 4 minerals only contain aqueous inclusions. The FIs in minerals of stages 1, 2, 3 and 4 yield homogenization temperatures of 261–443, 210–385, 152–304 and 159–263 °C, respectively, and salinities of ≤9.3 wt.% NaCl equiv., without consideration of the contribution from daughter minerals. The maximum estimated pressure decrease from 193 MPa in stage 1, through 182 MPa in stage 2, to 129 MPa in stage 3, suggesting the maximum mineralizing depths decreased from 8.4, through 7.9, to 5.6 km, and possibly occurred at 5.6–7.9 km. Therefore, the ore-forming fluids at Donggebi are characterized by high-temperature, CO2-bearing and NaCl-poor and then progressively evolved to CO2-poor and lower-temperature. Copyright © 2014 John Wiley & Sons, Ltd.

(1) Background: Upland cotton (Gossypium hirsutum L.) is the most important natural fiber worldwide, and it is extensively planted and plentifully used in the textile industry. Major cotton planting regions are frequently affected by abiotic stress, especially drought stress. Drought resistance is a complex, quantitative trait. A genome-wide association study (GWAS) constitutes an efficient method for dissecting the genetic architecture of complex traits. In this study, the drought resistance of a population of 316 upland cotton accessions was studied via GWAS. (2) Methods: GWAS methodology was employed to identify relationships between molecular markers or candidate genes and phenotypes of interest. (3) Results: A total of 8, 3, and 6 SNPs were associated with the euphylla wilting score (EWS), cotyledon wilting score (CWS), and leaf temperature (LT), respectively, based on a general linear model and a factored spectrally transformed linear mixed model. For these traits, 7 QTLs were found, of which 2 each were located on chromosomes A05, A11, and D03, and of which 1 was located on chromosome A01. Importantly, in the candidate regions WRKY70, GhCIPK6, SnRK2.6, and NET1A, which are involved in the response to abscisic acid (ABA), the mitogen-activated protein kinase (MAPK) signaling pathway and the calcium transduction pathway were identified in upland cotton at the seedling stage under drought stress according to annotation information and linkage disequilibrium (LD) block analysis. Moreover, RNA sequencing analysis showed that WRKY70, GhCIPK6, SnRK2.6, and NET1A were induced by drought stress, and the expression of these genes was significantly different between normal and drought stress conditions. (4) Conclusions: The present study should provide some genomic resources for drought resistance in upland cotton. Moreover, the germplasm of the different phenotypes, the detected SNPs and, the potential candidate genes will be helpful for molecular marker-assisted breeding studies about increased drought resistance in upland cotton.

The Yaochong porphyry Mo deposit in Xinxian County, Henan Province, China, is located in the Hong’an terrane, that is, the western part of the Dabie orogen. The Dabie orogen is part of a >1,500 km long, Triassic continental collision belt between the North China Block and the South China Block. Four types of vein are present. Paragenetically, from early to late, they are as follows: stage 1 quartz + K-feldspar ± pyrite ± magnetite vein; stage 2 quartz + K-feldspar + molybdenite ± pyrite vein; stage 3 quartz + polymetallic sulfides ± K-feldspar vein; and stage 4 quartz ± carbonate ± fluorite vein. Four compositional types of fluid inclusion, pure CO2, CO2 bearing, aqueous, and solid bearing, are present in quartz from the first three stages; only low-salinity aqueous fluid inclusions occur in quartz from the last stage. All the estimated salinities are ≤13.1 wt% NaCl eq., and no halite crystals were identified. Homogenization temperatures for the fluid inclusions from stages 1 to 4 are in the ranges of 262–501, 202–380, 168–345, and 128–286 °C, respectively, and estimated depths decrease from 6.9 to 8.9 km, through 6.2–7.2, to ~4.7 km. Quartz separates from the veins yielded a δ18O value of 7.7–11.2 ‰, corresponding to δ18OH2O values of −1.3 to 6.9 ‰ using temperature estimates from fluid inclusion data; δDH2O values of fluid inclusion vary from −80 to −55 ‰, and δ13CCO2 from −2.3 to 2.7 ‰, suggesting that the ore-fluids evolved from magmatic to meteoric sources. We conclude that the ore-forming fluid system at Yaochong was initially high temperature, high salinity, and CO2-rich and then progressively evolved to CO2-poor, lower salinity, and lower temperature, by mixing with meteoric water, which results in ore precipitation.

Huogeqi is a shear zone-hosted epigenetic deposit within the greenschist-amphibolite facies of the Mesoproterozoic Langshan Group in the Langshan district on the northern margin of the North China Craton (NCC). Copper mineralization in the Huogeqi deposit was formed in two stages: a main-stage controlled by the shear zone and characterized by brittle-ductile ore-forming structures and a lower greenschist facies mineral assemblage, and a late stage characterized by open space-filling textures and low-temperature minerals. Based on microthermometric and Raman microprobe analysis, the main-stage Cu-bearing fluid was mesothermal, low-salinity and H2O–CH4-dominant, and was generated by an interaction between a deep-crustal metamorphic fluid and graphite-bearing host rocks. This interaction resulted in a more CH4-rich fluid, which was more amenable to be immiscible. We showed that immiscibility of the H2O–CH4 fluid occurred due to temperature decrease, prior to the main-stage Cu mineralization; Cu was finally precipitated from the resultant H2O-rich aqueous fluid. Main-stage Cu mineralization temperature was obtained using various methods: 310–370 °C by intersection of isochors of coexistent CH4 and aqueous inclusions; 364 ± 41 °C on average by pressure correction of the homogenization temperatures of aqueous inclusions; and 362 ± 26 °C using the chlorite geothermometer. Pressure during Cu-deposition fluctuated between lithostatic and hydrostatic at depths of ca. 10–12 km, but it seemingly had no effect on the mineralization process. The late-stage Cu-bearing fluid was a low temperature, low salinity, H2O of meteoric origin.

The Qian'echong Mo deposit in Guangshan county, Henan Province, China, is a giant porphyry Mo deposit formed in Early Cretaceous in the Dabie Shan. Mo mineralization is associated with the Qian'echong granite porphyry, mainly presenting as numerous veinlets in the altered wallrocks, with potassic, phyllic, argillic and propylitic alteration developed. The hydrothermal ore-forming process can be divided into four stages: quartz + potassic feldspar + magnetite stage 1, quartz + molybdenite stage 2, quartz + carbonate + polymetal sulfide stage 3 and quartz + carbonate + fluorite stage 4. Fluid inclusions (FIs) can be distinguished between pure carbonic, carbonic, aqueous and solid-bearing types, but only the stage 1 quartz contains all the four types of FIs. The stage 2 quartz has three of the four types of FIs, with exception of PC-type. The stage 3 minerals are developed with the aqueous FIs with or without daughter minerals, but short of any kinds of CO 2 -bearing FIs. In stage 4 minerals, only the W-type FIs can be observed. The FIs in minerals of stages 1, 2 and 3 are mainly homogenized at temperatures of 260 − 400 °C, 200 − 340 °C and 160 − 300 °C, with salinities of 2.00 − 11.58 wt.% NaCl.eqv, 1.06 − 10.98 wt.% NaCl.eqv and 0.53 − 9.47 wt.% NaCl.eqv, respectively. The estimated minimum trapping pressures are up to 100 MPa in stage 1 and to 62 MPa in stage 2, respectively, corresponding to an initial mineralization depth of no less than 4 km. The quartz separates from veinlets yield δ 18 O values of 7.1 − 10.2‰, corresponding to δ 18 O H 2 O values of − 1.4 − 5.7‰, and the δD H2O values of fluid inclusions of − 55 −− 72‰, suggesting that the ore-fluids evolved from magmatic to meteoric in sources. Therefore, the initial fluids forming the Qian'echong deposit, compared to those forming the porphyry systems in volcanic arcs, are characterized by relatively high temperature, high salinity, high f O 2 , CO 2 -rich, and NaCl-poor, considering that no halite has been observed in S-type FIs. We suggest that the “CO 2 -rich fluid” is a distinctive feature of porphyry systems developed in continental collision regime.

The Nannihu Mo–W deposit, located in the Henan Province of China, is a giant porphyry deposit formed in the Qinling Orogen during the Jurassic continental collision between the North China and Yangtze Cratons. Mo–W mineralization is associated with the Nannihu porphyritic monzogranite, occurring as numerous stockwork veinlets in the altered wallrocks and the causative porphyry. Both the porphyry stock and wallrocks underwent intense hydrothermal alteration, ranging outwardly from potassic to phyllic alteration, and to carbonation zones with increasing distance from the intrusion. The hydrothermal ore-forming process can be divided into four stages characterized by veinlets, from early to late: (1) quartz + potassic feldspar ± molybdenite ± pyrite; (2) quartz + molybdenite veins containing minor pyrite and chalcopyrite; (3) quartz + polymetal sulfide; and (4) quartz + carbonate + fluorite. Most of the ores are formed during stages 2 and 3. Four types of fluid inclusions (FIs) are distinguished in this study based on petrographic and microthermometric criteria, i.e. pure CO 2 , NaCl–H 2 O, CO 2 –H 2 O and daughter mineral-bearing fluid inclusions. All of the four types of FIs can be observed in the hydrothermal quartz formed in stages 1, 2 and 3; while the stage 4 minerals contain only NaCl–H 2 O fluid inclusions. Fluid inclusions of stage 1 are mainly homogenized between 350 and 460 °C, with salinities ranging from 5.7 to 17.9 wt.% NaCl equiv. The stage 2 FIs yield homogeneous temperatures of 300–380 °C and salinities of 3.5–16.9 wt.% NaCl equiv. FIs of stage 3 are homogenized between 250 and 370 °C, with salinities of 1.8–14.3 and 28.6–39.1 wt.% NaCl equiv. FIs of stage 4 are homogenized at temperatures of 115 to 265 °C, yielding salinities of 0.5 to 1.2 wt.% NaCl equiv. Daughter minerals, such as halite, chalcopyrite and some unknown minerals, are frequently present in stage 3 FIs, which probably represent a reducing and oversaturated fluid-system resulting from fluid-boiling. The daughter mineral-bearing FIs coexist with vapor- and liquid-rich NaCl–H 2 O FIs that have contrasting salinities. These FIs are homogenized in divergent ways at similar temperatures, suggesting that fluid boiling took place in stages 2 and 3. The estimated pressures range from 70 to 270 MPa in stage 1, through 30–150 MPa in stage 2, to 30–85 MPa in stage 3, corresponding to a depth of no less than 3 km. In other words, the ore-forming fluids are characterized by high temperature, high salinity, high f O 2 and high CO 2 content; and fluid-boiling resulted in CO 2 release, f O 2 decrease and ore mineral precipitation. We suggest that the CO 2 -rich fluid is a distinctive feature of porphyry systems developed in continental collision setting, in transitional compressional to extensional regime, contrasting to the CO 2 -poor NaCl–H 2 O fluids observed in volcanic arcs.

In this paper, TZS88 aluminum alloy mechanical properties of three months of natural aging is tested, the microstructure and the strengthening mechanism is studied by the application of optical metallographic microscope and scanning electron microscopy. The results show that TZS88 aluminum reinforced mainly caused by solid solution strengthening, aging strengthening and dispersion strengthening, and as such its tensile strength, hardness and elongation in the natural aging have reached ZQSn6-6-3 bronze level, the microstructure are compounds which included α(Al) solid solution matrix + Sn + s, θ, T, ε etc.

In this paper, the WC-5TiC-10 Co mixture mixed by WC2.96μm, (Ti, W)C 2.52μm and Co2.38μm and prepared by high-energy ball milling. The result shows: After 60h’s ball milling the powder began to reunite more and more as the time extended . The average grain size of powder is 50 nm after144h. After 1300°C~1400°C vacuum-sintering the hardness of the sample is 94.8 ~ 95.4HRA. 4.2 ~ 5.2 HRA higher than the traditional cemented carbides with the same composition. After 1400°C vacuum-sintering the compressive strength and flexural strength of cemented carbides is 2060 MPa and 1200 MPa. Slightly less than the traditional cemented carbides with the same composition.