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Remnants of the Proto-Tethys are mainly preserved in the region between south of the North China-Tarim Block and north of Qiangtang-Sibumasu/Baoshan Blocks. Magmatic-metallogenic events related to the Proto-Tethyan subductions were rarely reported, and the subduction history and polarity of the Proto-Tethyan are still under debate. Here, we presented new data of zircon U Pb ages, whole-rock Sr–Nd–Pb isotopes, major and trace elements and zircon Hf isotopes for the volcanic rocks in the northeastern Altyn Mountains. Information of over 14 volcanic-hosted deposits/prospects in the region has been compiled. These volcanic ore hosts consist mainly of basaltic andesite, andesite, dacite and rhyolite rocks. The andesite and rhyolite rocks are newly zircon U Pb dated to be Late Cambrian-Early Ordovician (andesite: 490.5 ± 5.2 Ma; rhyolite: 492.6 ± 2.9 Ma and 491.6 ± 5.6 Ma), representing the timing of volcanism and VMS (Volcanogenic Massive Sulfide) mineralization. All the volcanic rocks belong to the high-K calc-alkaline and shoshonite series: the andesite rocks from the Kaladawan area in north of the region display arc geochemical affinities and contain (87Sr/86Sr) i (0.7082–0.7083) and ε Nd (t) (−9.7 to −7.6), indicating that they were likely formed by partial melting of the mantle wedge with subducted sediment inputs. The rhyolite rocks from the Kaladaban area in south of the region are characterized by high SiO 2 (64.46–78.55 wt%), low alkali (Na 2 O + K 2 O, 3.46–7.17 wt%), and contain (87Sr/86Sr) i (0.7063–0.7095), ε Nd (t) (−6.6 to −1.5), and zircon ε Hf (t) (−5.5 to 5.4), indicating that they were likely derived from partial melting of the lower crust with depleted mantle inputs. Rock assemblage and geochemistry suggest that volcanic rocks in the northeastern Altyn Mountains may have formed in a continental arc setting. Their spatial distributions with respect to the ophiolites in the region suggest that the subduction was likely south-dipping. This subduction-related arc magmatism may have formed the many important VMS and porphyry–skarn deposits in the region. Unlabelled Image • The Kaladawan ore-hosting volcanic rocks yielded zircon U Pb age of 492.6–490.5 Ma. • The volcanics have geochemical characters similar to typical arc igneous rocks. • The south-dipping subduction of Proto-Tethys Ocean formed a continental island arc. [ABSTRACT FROM AUTHOR]

The Kaladawan Fe–Mo ore field in Altyn (Xinjiang Province, NW China) contains six Fe (–Mo) deposits, with total proven reserves of 60 Mt Fe and 10,000 t Mo. Tabular, lensoidal and stratiform orebodies occur in the Cambrian foliated marble, phyllite, carbonaceous slate, chlorite–sericite schist and quartz–sericite schist along the exocontact zone of the Kaladawan granite. Skarns are extensively developed and dominated by garnet, pyroxene, epidote, tremolite and actinolite, with minor chlorite, zoisite, quartz and calcite. Ore minerals are mainly magnetite and molybdenite. Five alteration and mineralization stages (I–V) were identified: the prograde (I) and retrograde (II) skarns are characterized by assemblages of garnet–pyroxene and epidote–tremolite–actinolite, respectively, intruded and replaced by mineral assemblages of magnetite–epidote–zoisite (III), quartz–sulfides (IV) and calcite–chlorite (V) in younging order. The Kaladawan garnet contains more andradite (61.2–94.4 mol%) than grossularite (37.5–5.0 mol%). Pyroxene is Mg-rich and Fe-poor, with an endmember range of 55.4–94.7 mol% diopside and 42.5–4.7 mol% hedenbergite. Amphibole comprises mainly tremolite and actinolite. The Kaladawan skarn mineral contents resemble typical skarn Fe and Mo deposits. In-situ LA-ICP-MS magnetite trace element analysis had identified unusually high Mg, Mo and Cr concentrations. The high Mo and the absence of molybdenite inclusions in magnetite suggest that the hydrothermal fluids may have been Mo-rich. The magnetite also contains similar (Ti + V) and (Al + Mn) values with typical skarn Fe deposits. Therefore, the Kaladawan Fe–Mo mineralization is best attributed to be skarn-type, and related to the Kaladawan granite intrusion. [ABSTRACT FROM AUTHOR]

[Display omitted] • • Mn(II) complex 1 with 8-hydroxyquinoline-N-oxide was firstly synthesized. • • Mn(II) complex 1 showed high in vitro antitumor activity toward A549/DDP cells. • • Mn(II) complex 1 can cause mitochondrial dysfunction. A new manganese(II) complex bearing an 8-hydroxyquinoline- N -oxide (HNQ) ligand, i.e., [Mn(HNQ) 2 (CH 3 OH) 2 Cl 2 ] (1), was synthetized and fully characterized by single-crystal X-ray diffraction, infrared spectroscopy, electrospray ionization mass spectrometry, and elemental analysis, which revealed that Mn(II) complex 1 is a six-coordinated mononuclear compound. The anticancer activity of Mn(II) complex 1 against A549/DDP and A549 cancer cells and HL-7702 normal cells was tested and compared with that of MnCl 2 ⋅4H 2 O, cisplatin, and HNQ. Mn(II) complex 1 displayed potent cytotoxic activity, especially against A549/DDP tumor cells, with IC 50 values of 0.02 ± 0.01 μM, whereas it was practically inactive against HL-7702 normal cells. Mechanistic studies indicated that the cytotoxic activity of Mn(II) complex 1 proceeds via induction of mitochondria-mediated intrinsic apoptosis in A549/DDP cells. [ABSTRACT FROM AUTHOR]

Abstract: Principal component analysis (PCA) is employed to investigate the relationship between CO2 emissions (COEs) stemming from fossil fuel burning and cement manufacturing and their affecting factors. Eight affecting factors, namely, Population (P), Urban Population (UP); the Output Values of Primary Industry (PIOV), Secondary Industry (SIOV), and Tertiary Industry (TIOV); and the Proportions of Primary Industry's Output Value (PPIOV), Secondary Industry's Output Value (PSIOV), and Tertiary Industry's Output Value (PTIOV), are chosen. PCA is employed to eliminate the multicollinearity of the affecting factors. Two principal components, which can explain 92.86% of the variance of the eight affecting factors, are chosen as variables in the regression analysis. Ordinary least square regression is used to estimate multiple linear regression models, in which COEs and the principal components serve as dependent and independent variables, respectively. The results are given in the following. (1) Theoretically, the carbon intensities of PIOV, SIOV, and TIOV are 2573.4693, 552.7036, and 606.0791kt per one billion $, respectively. The incomplete statistical data, the different statistical standards, and the ideology of self sufficiency and peasantry appear to show that the carbon intensity of PIOV is higher than those of SIOV and TIOV in China. (2) PPIOV, PSIOV, and PTIOV influence the fluctuations of COE. The parameters of PPIOV, PSIOV, and PTIOV are ?2706946.7564, 2557300.5450, and 3924767.9807kt, respectively. As the economic structure of China is strongly tied to technology level, the period when PIOV plays the leading position is characterized by lagging technology and economic developing. Thus, the influence of PPIOV has a negative value. As the increase of PSIOV and PTIOV is always followed by technological innovation and economic development, PSIOV and PTIOV have the opposite influence. (3) The carbon intensities of P and UP are 1.1029 and 1.7862kt per thousand people, respectively. The carbon intensity of the rural population can be inferred to be lower than 1.1029kt per thousand people. The characteristics of poverty and the use of bio-energy in rural areas result in a carbon intensity of the rural population that is lower than that of P. [Copyright &y& Elsevier]

The Great Hingan Range is located in the eastern sector of the Central Asia Orogenic Belt, and is the second important Mo province in China, next to the Qinling–Dabie orogenic belt. Previous studies concluded that all the Mo deposits (Mo-only or Mo-dominated polymetallic) in the area were formed in the Mesozoic, and related either to the syn- to post-collisional setting following the closure of the Paleo-Asia Ocean, or to the westward subduction of the Pacific plate. However, the fluids forming the giant Diyanqin'amu porphyry Mo deposit in the area disagree with the features of collision-type Mo deposits, but accord with those of the subduction- or continental arc-type. The Mo mineralization is hosted in the Late Jurassic volcanic rocks and genetically related to the buried porphyritic granite and aplitic granite. Two porphyritic granite samples yield LA-ICP-MS zircon weighted mean 206 Pb/ 238 U ages of 158.7 ± 0.8 Ma (MSWD = 0.64, 2σ) and 158.0 ± 0.9 Ma (MSWD = 0.38, 2σ), respectively. The aplitic granite yields a zircon U–Pb weighted mean 206 Pb/ 238 U age of 156.9 ± 1.1 Ma (MSWD = 0.48, 2σ), slightly younger than the porphyritic granite. Seven molybdenite samples from the ores yield Re–Os isotope ages of 156.1 ± 2.2 to 158.1 ± 4.3 Ma. These ages constrain that the Diyanqin'amu Mo system was formed in the period of 159–156 Ma. The granites at the deposit 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 affinity. These granites and the host volcanic rocks are characterized by enrichment of K, Rb, U, Pb, Th and LREE, and depletion of Nb, Ta, Ti and HREE, with negative Eu anomaly, which are similar to magmatic rocks in the Andean arc. Zircon grains from the granites show positive ε Hf ( t ) values of 4.2–9.0, with T DM2 (Hf) ages of 0.63–0.94 Ga. These geochemical data imply that the granites at Diyanqin'amu are highly fractionated I-type, formed in a continental arc generated by the southeastward subduction of the Mongol–Okhotsk oceanic plate. [ABSTRACT FROM AUTHOR]

This paper proposes a simple and feasible surface modification method to suppress the moisture-induced degradation of the green-emitting phosphor Ba 2 SiO 4 :Eu 2+ (BSO:Eu 2+ ), which hits its reliability very hard and restricts its wide commercialization in WLEDs. A hydrophobic surface layer was formed on the surface of this phosphor via hydrolysis and polymerization of tetraethylorthosilicate (TEOS) and polydimethylsiloxane (PDMS). The produced surface layer consisted of an amorphous silicon dioxide with a thickness of ∼2 nm along with the presence of −CH 3 groups on the surface. The modified phosphor featured superior stability in high-pressure water steam conditions at 150 °C. [ABSTRACT FROM AUTHOR]

Six new Pd(II), Pt(II) and Ag(I) complexes, (1);{Pd (L 1)]2C 6 H 4 } 2 Cl 4 } (2); Pt(L 2)(DMSO)Cl; 3; {PtL 5 ] 2 C 6 H 4 } 2 ·PhCOO-⋅11NO 3 -; 4; {[Pt(L 4)] 2 C 6 H 4 }; the binuclear cyclometalated complex the polymer chain (5); {[PtL 5 ]C 6 H 4 }·NO 3 -}; and the polymeric silver species (6); Zn(L 6) 2 ·AgNO 3 ·CHCl 3 were synthesized and thoroughly characterized using X-ray diffraction and spectroscopic techniques (L 1 =(S,S)-1,4-i-PrOx] 2 C 6 H 4 } 2 Cl 4 , L 2 =Di(2,2-bis(4R-isopropyl-4,5-dihydro-oxazol-2-yl)acetonitrile) zinc (II) (B R1);L 3 = 1,4-bis(4R-benzyl-4,5-dihydro-oxazol-2-yl)benzene (A R2); L 4 = 1,4-bis(4R-benzyl-4,5-dihydro-oxazol-2-yl)benzene，L 5 =1,4-bis(4R-benzyl-4,5-dihydro-oxazol-2-yl)-benzene，L 6 =Di(2,2-bis(4S-isopropyl-4,5-dihydrooxazol-2-yl)acetonitrile) zinc (II). Complexes 1-6 showed cytotoxic effects against human tumour cell lines, including a multidrug-resistant subline. Oxazoline and Pd complex 1 induced apoptosis in A549 cells. DFT calculations were also performed to exhibit the excellent bioactivity of complex 1 against A549, MDA-MB-231, and KB cells. Complex 1, with the best docking score and a stable interaction network within the binding site of the G-quadruplex, could stably interact with the G-quadruplex. Additionally, complex 1 was further used in the animal experiment of human lung adenocarcinoma cells in nude mice. By comparing with the model control group, the tumour volume, relative tumour volume and relative tumour proliferation rate T/C decreased significantly in the cisplatin group and compound 1 (complex 1) group. [Display omitted] • Six novel mononuclear, dinuclear and one-dimensional Pd(II), Pt(II) and Ag(I) complexes related with oxazoline ligands have been easily prepared in good yields from 68% to 92%. • Pd(II), Pt(II) and Ag(I) complexes showed different cytotoxic effects against human tumour cell lines, especially complex 1 could induce an apoptosis in cell A549. • DFT calculations and molecular docking simulations were performed to explore the possible interaction mechanism between these complexes and the binding pocket of G-quadruplex. • Comparing with the control group, the tumour volume, relative tumour volume and relative tumour proliferation rate T/C decreased significantly in the animal experiment by using complex 1. [ABSTRACT FROM AUTHOR]

The Caixiashan giant carbonate-hosted Zn–Pb deposit (~ 131 Mt@ 3.95% Zn + Pb) formed by replacement of dolomitized marble, with stratiform massive and breccia bodies is located near the base of the Proterozoic Kawabulake Group limestone and marble. It is one of the largest carbonated-hosted massive sulfides Zn–Pb ore deposits in Northwest China to have been discovered in recent years. Abundant pyrite occurs in dolomitized marble, along fractures in dolomitized clasts in the host rocks and filling cracks in the host rock. Locally, colloform or framboidal pyrites are observed in the early period and sometimes replaced by the later sphalerite. The sulfide assemblage of the main ore stage is characterized by massive or disseminated sphalerite and galena, with less pyrite than the earlier stage, and minor pyrrhotite. Galena occurs as small veins cutting the early-formed sphalerite. Dolomite and calcite are the main gangue minerals that co-precipitated with these sulfides. Tremolite and quartz alteration commonly overprints the orebodies. According to the crosscutting relationships and the different mineral associations within the host rocks and ore bodies, three stages are recognized at Caixiashan, i.e., syn-sedimentary pyrite (stage I), pyrite alteration, sphalerite–carbonate and galena–pyrite–carbonate (stage II-1, stage II-2 and stage II-3, respectively) and magmatic/metamorphic reworking (stage III). Calcite and quartz crystals are important host minerals among the three hypogene stages (stages I–III, although quartz mainly occurred in stage III). Stage I contains only aqueous inclusions (W-type), which were homogenized from 110 to 236 °C (main range of 138–198 °C and average at 168 °C; main range = average ± σ) and the salinities are from 0.5 to 16.5 (main range of 5.1–15.1 with average of 10.1) wt.% NaCl eqv. In the pyrite alteration of stage II-1 the W-type fluid inclusions homogenized from 175 to 260 °C (main range of 210–260 with average of 235) and the salinities range from 8.5 to 22.4 (main range of 16.7–20.1 with average of 18.4) wt.% NaCl eqv. In the main Zn–Pb mineralization stage (stage II-2–3), four types of fluid inclusions were identified an aqueous phase (W-type), a pure carbon phase (PC-type), a carbon phase containing (C-type) and mineral bearing inclusions (S-type). The W-type fluid inclusions of stage II-2–3 homogenized at 210 to 370 °C (main range of 253–323 and average at 270) and the salinities range from 5.9 to 23.1 (main range of 13.3–20.3 with average at 16.8) wt.% NaCl eqv.; C-type homogenized at 237 °C to 371 °C and the salinities range from 6.4–19.7 wt.% NaCl eqv.; S-type fluid inclusions homogenized at 211 to 350 °C and daughter minerals melted between 340 and 374 °C during heating, indicating a salinity range of 42 to 44 wt.% NaCl eqv. PC-type fluid inclusions with homogenization temperatures of CO 2 phase show large variation from 7.4 °C to 21.2 °C. Laser Raman analyses show that CH 4 , CO 2 and SO 4 2 − coexist in the main mineralization stage fluids. The magmatic/metamorphic reworking stage only contains W-type fluid inclusions which yield homogenized between 220 and 360 °C (main range of 251–325 and average at 288), with salinities ranging from 1.7 to 23.0 (main range of 14.3–20.0 and average at 18.8) wt.% NaCl eqv. The textural features, mineral assemblages and fluid geochemistry suggest that the Zn–Pb ores were formed through hydrothermal convection of hot marine waters along the faults and fractures resulting in metal (Zn, Pb and Fe) enriched stratiform orebodies. Subsequent rapid precipitation of sulfides was triggered by sulfate (SO 4 2 − ) thermal reduction with the CH 4 preserved in sedimentary rocks and early stage I pyrite bodies. This process occurred at moderate temperatures ( ca . 270 °C). Higher-temperature magmatic hydrothermal alteration overprinted the orebodies, but only provided a minor contribution to the mineralization. [ABSTRACT FROM AUTHOR]

Zircon U–Pb ages of high Mg dioritic dikes in the Mesoproterozoic Kawabulake Group in the Eastern Tianshan area, NW China indicate that they were emplaced in the Early Carboniferous at 353–348 Ma. The dikes consist of medium-grained plagioclase and hornblende with minor clinopyroxene and trace quartz. They are characterized by intermediate SiO 2 (60–62 wt.%), low TiO 2 (0.63–0.71 wt.%), relatively high Al 2 O 3 (15.1–15.8 wt.%) and MgO contents (3.45–4.15 wt.%) with Mg# generally higher than 56 (56–59). The geochemistry of the high Mg diorites suggest they were formed by similar magmatic processes to sanukitoid high Mg Andesites such as those of the Setouchi volcanic belt, Japan. Zircons from the high Mg dioritic dikes have ε Hf( t ) values of −6.8 to +14.5. The dominantly positive values suggest a juvenile source, whereas the small number of negative values suggests mature components were also incorporated into the source. Similarly, the positive ε Nd( t ) values (0 to +2.2) are interpreted to reflect a juvenile source whereas the negative values of (−5.2 to 0) suggest participation of old crustal rocks in the petrogenesis of the diorites. The variable ε Hf( t ) and ε Nd( t ) values suggest that the mature material was assimilated during magma ascent rather than in the mantle wedge which would result in more uniform values. Mass balance calculations suggest that the dioritic dikes were derived from sources composed of approximately 97% juvenile mantle-derived material and 3% sediment. Petrographic, elemental, and isotopic evidence suggest that the dioritic dikes were generated by partial melting of depleted mantle that migrated into the shallow crust where it assimilated older sedimentary rocks of the Mesoproterozoic Kawabulake Group. [ABSTRACT FROM AUTHOR]

The easy-to-use method for detecting uric acid in human serum is of great importance because of its crucial role in physiological and pathological processes. Herein, a simple and effective strategy was designed for colorimetric sensing of uric acid using the morphological transition of Ag nanoprisms. In the presence of uricase, uric acid was oxidized to produce H 2 O 2 . Subsequently, the morphology of Ag nanoprisms changed from triangle to round by etching of H 2 O 2 , leading to a more than 120 nm blue shift of surface plasmon resonance spectral band. The color change from pale blue to purple related to concentration change of uric acid can be judged by naked eyes. A linear relationship between the blue shift of peak of Ag nanoprisms and uric acid concentration ranged from 1.0 to 40 μM. The detection limit of uric acid was 0.7 μM. Some potential interferents (e.g., ascorbic acid, glucose, dopamine, hypoxanthine and various amino acids) in human serum showed no interference. Serum samples could be directly added into Ag nanoprism–uricase sensing system, and the assay can be completed within one hour. The proposed sensor was successfully applied for detecting uric acid in human serum with the recoveries over 95%. The obtained results are in agreement with those measured by biochemistry analyzer with the average relative error of 5.1%. The Ag nanoprism–uricase sensor offers advantages of high selectivity and sensitivity, low-cost instruments, and rapid assay without sample pretreatment. Thus, the present uric acid sensor has great potential in applications for biochemical analysis and clinical diagnosis. [ABSTRACT FROM AUTHOR]