218 resultados para CA2 STORES
Resumo:
Duobuza copper deposit, newly discovered typical gold-rich porphyry copper deposit with superlarge potential, is located in the Tiegelong Mesozoic tectonic -magmatic arc of the southern edge of Qiangtang block and the northern margin of Bangonghu-Nujiang suture. Quartz diorite porphyrite and grandiorite porphyry, occurred in stock, are the main ore-bearing porphyries. As the emplacement of porphyry stock, a wide range of hydrothermal alteration has developed. Within the framework of the ore district, abundant hydrothermal magnetite developed, and the relationship between precipitation of copper and gold and hydrothermal magnetite seems much close. Correspondingly, a series of veinlets and network veinlets occurred in all alteration zones. Therefore, systematic research on such a superlarge high-grade Duobuza gold-rich porphyry copper deposit can fully revealed the metallogenic characteristics of gold-rich porphyry copper deposits in this region, establish metallogenetic model and prospecting criteria, and has important practical significance on the promotion of regional exploration. In addition, this research on it can enrich metallogenic theory of strong oxidation magma-fluid to gold-rich porphyry copper deposit, and will be helpful to understand the metallogenic characteristics in early of subduction of Gangdese arc stages and its entire evolution history of the Qinghai-Tibet Plateau, the temporal and spatial distribution of ore deposits and their geodynamics settings. Northern ore body of Duobuza copper deposit have been controlled with width (north-south) about 100 ~ 400 m, length (east-west) about 1400 m, dip of 200 , angle of dip 65 ~ 80 . And controlled resource amount is of 2.7 million tons Cu with grade 0.94% and 13 tons Au with 0.21g/tAu. Overall features of ore body are large scale, higher grade copper, gold-rich. Ore occurred in the body of granodiotite porphyry and quartz diorite porphyrite and its contact zone with wall rock. Through the detailed mapping and field work studies, some typies of alteration are identificated as follows: albitization, biotititation, sericitization, silication, epidotization, chloritization, carbonatization, illitization, kaolinization and so on. The range of alteration is more than 10km2. Wall alteration zone can be divided into potassic alteration, moderate argillization alteration, argillization, illite-hydromuscovite or propylitization from ore-bearing porphyry center outwards, but phyllic alteration has not well developed and only sericite-quartz veins occurred in local area. Moreover, micro-fracture is development in ore district , and correspondingly a series of veinlets are development as follows: biotite vein (EB type), K-feldspar-biotite-chalcopyrite-quartz vein, magnetite-antinolite-K-feldspar vein, quartz-chalcopyrite-magnetite veins (A-type), quartz-magnetite-biotite-K-feldspar vein, chalcopyrite veinlets in potassic alteration zone; (2) chalcopyrite occurring in the center veinquartz vein (B type), chalcopyrite veinlets, chalcopyrite-gypsum vein in intermediate argillization alteration; (3) chalcopyrite- pyrite-quartz vein, pyrite-quartz vein, chalcopyrite-gypsum veins, quartz-gypsum- molybdenite-chalcopyrite vein in argillization alteration; (4) gypsum veins, quartz-(molybdenite)-chalcopyrite vein, quartz-pyrite vein, gypsum- chalcopyrite vein, potassium feldspar veinlets, Carbonate veins, quartz-magnetite veins in the wall rock. In short, various veins are very abundant within the framework of the ore district. The results of electronic probe microscopy analysis (EMPA) indicate that Albite (Ab 91.5~99.7%) occurred along the rim of plagioclase phenocryst and fracture, and respresents the earliest stages of alteration. K-feldspar (Or 75.1~96.9%) altered plagioclase phenocryst and matrix or formed secondary potassium feldspar veinlets. Secondary biotite occurred mainly in phenocryst, matrix and veinlets, belong to magnesium-rich biotite formed under the conditions of high-oxidation magma- hydrothermal. Chloritization developed in all alteration zones and alterd iron- magnesium minerals such as biotite and hornblende and then formed chlorite veinlets. As the temperature rises, Si in the tetrahedral site of chlorite decreased, and chlorite component evolved from diabantite to ripiolite. The consistent 280~360 of formation temperature hinted that chlorite formed on the same temperature range in all alteration zones. However, formation temperature range of chlorite from the gypsum-carbonate-chlorite vein was 190~220, and it may be the product of the latest stage of hydrothermal activity. The closely relationship between biotite and rutile indicate that most of rutiles are precipitated in the process of biotite alteration and recrystallization. In addition, the V2O3 concentration of rutile from ore body in Duobuza gold-rich porphyry copper deposit is >0.4, indicate that V concentration in rutile has important significance on marking main ore body of porphyry copper deposit. Apatites from Duobuza deposit all are F-rich. And apatite in the wall rock contained low MnO content and relatively high FeO content, which may due to the basaltic composition of the wall rocks. The MnO in apatite from altered porphyry show a strong positive correlation with FeO. In addition, Cl/F ratio of apatite from wall rock was highest, followed by the potassic alteration zone and potassic alteration zone overprinted by moderate argillization alteration was the lowest. SO2 in Apatite are in the scope of 0 to 0.66%, biotite in the apatite has the highest SO2, followed by the potassic alteration zone, potassic alteration zone overprinted by moderate argillization alteration, and the lowest in the surrounding rocks, which may be caused by the decrease of oxygen fugacity of hydrothermal fluid and S exhaust by sulfide precipitation in potassic alteration. Magnetite in the wall rock have higher Cr2O3 and lower Al2O3 features compared with altered porphyry, this may be due to basalt wall rock generally has high Cr content. And magnetites have higher TiO2 content in potassic alteration than moderate argillization alteration overprinted by potassic alteration, argillization and wall rock, suggested that its formation temperature in potassic alteration was the highest among them. The ore minerals mainly are chalcopyrite and bornite, and Au contents of chalcopyrite, bornite, and pyrite are similar with chalcopyrite slightly higher. The Eu* negative anomaly of disseminated chalcopyrite was relatively lower than chalcopyrite in veinlets. Within a drill hole, the Eu* negative anomaly of disseminated chalcopyrite was gradually larger from bottom to top. Magnetite has the same distribution model, with obvious negative Eu* abnormal, and REE in great changes. The gypsum has the highest REE content and the obvious negative anomaly, and biotite obviously has the Eu* abnormal. Based on the petrographic and geochemical characteristics, five series of magmatic rocks can be broadly classified; they are volcanic rocks of the normal island arc, high-Nb basaltic rocks, adakites, altered porphyry and diorite. The Sr, Nd, Hf isotopes and geochemistry of various series of magmatic rock show that they may be the result of mixing between basic magma and various degrees of acid magma coming from lower crust melted by high temperature basic underplating from partial melting of the subduction sediment melt metasomatic mantle wedge. Furthermore S isotope and Pb isotope of the sulfide, ore-bearing porphyries and volcanic rocks indicated ore-forming source is the mantle wedge metasomatied by subduction sediment melt. Oxygen fugacity of magma estimated by Fe2O3/FeO of whole rock and zircon Ce4+/Ce3+ indicated that the oxidation of basalt-andesitic rocks is higher than ore-forming porphyry, and might imply high-oxidation characteristics of underplated basic magma. Its high oxidative mechanism is likely mantle sources metasomatied by subduction sediment magma, including water and Fe3+. And such high oxidation of basaltic magma is conducive to the mantle of sulfides in the effective access to melt. And the An component of dark part within plagioclase phenocryst zoning belong to bytownite (An 74%), and its may be a result of magma composition changes refreshment by basaltic magma injection. SHRIMP zircon U-Pb and LA-ICP-MS zircon U-Pb geochronology study showed that the intrusions and volcanic rocks from Duobuza porphyry copper deposit belong to early Cretaceous magma series (126~105Ma). The magma evolution series are as follows: the earliest diorite and diorite porphyrite ore-bearing porphyry and barren grandiorite porphyry basaltic andesite diorite porphyrite andesite basaltic andesite, and magma component shows a evolution trend from intermediate to intermediate-acid to basic. Based on the field evidences, the formation age of high-Nb basalt may be the latest. The Ar-Ar geochronology of altered secondary biotite, K-feldspar and sericite shows that the main mineralization lasting a interval of about 4 Ma, the duration limit of whole magma-hydrothermal evolution of about 6 Ma, and possibly such a long duration limit may result in the formation of Duobuza super-large copper deposit. Moreover, tectonic diagram and trace element geochemistry of volcanic rocks and diorite from Duobuza porphyry copper deposit confirm that it formed in a continental margin arc environment. Zircon U-Pb age of volcanic rocks and porphyry fall in the range of 105~121Ma, and Duobuza porphyry copper deposit locating in the north of the Bangonghu- Nujiang suture zone, suggested that Neo-Tethys ocean still subducted northward at least early Cretaceous, and its closure time should be later than 105 Ma. Three major inclusion types and ten subtypes are distinguished from quartz phenocrysts and various quartz veins. Vapor generally coexisting with brine inclusions, suggest that fluid boiling may be the main ore-forming mechanism. Raman spectrums of fluid inclusions display that the content of vapor and liquid inclusion mainly contain water, and vapor occasionally contain a little CO2. In addition, the component of liquid inclusions mainly include Cl-, SO42-, Na+, K+, a small amount of Ca2+, F-; and Cl- and Na+ show good correlation. Vapor mainly contains water, a small amount of CO2, CH4 and C2H6 and so on. The daughter minerals identified by Laman spectroscopy and SEM include gypsum, chalcopyrite, halite, sylvite, rutile, potassium feldspar, Fe-Mn-chloride and other minerals, and ore-forming fluid belong to a complex hydrothermal system containing H2O-NaCl-KClFeCl2CaCl2. H and O isotopic analysis of quartz phenocryst, vein quartz, magnetite, chlorite and gypsum from all alteration zones show that the ore-forming fluid of Duobuza gold-rich porphyry copper deposit consisted mainly of magmatic water, without addition of meteric water. Duobuza gold-rich porphyry copper deposit formed by the primary magmatic fluid (600-950C), which has high oxidation, ultra-high salinity and metallogenic element-rich, exsolution direct from the magma, and it is representative of the typical orthomagmatic end member of the porphyry continuum. Moreover, the fluid evolution model of Duobuza gold-rich porphyry copper deposit has been established. Furthermore, two key factors for formation of large Au-rich porphyry copper deposit have been summed up, which are ore-forming fluids earlier separated from magma and high oxidation magma-mineralization fluid system.
Resumo:
The Grove Mountains, including 64 nunataks, is situated on an area about 3200km2 in the inland ice cap of east Antarctica in Princess Elizabeth land (72o20'-73101S, 7350'-75o40'E), between Zhongshan station and Dome A, about 450km away from Zhongshan station (6922'S, 7622'E). Many workers thought there was no pedogenesis in the areas because of the less precipitation and extreme lower temperature. However, during the austral summer in 1999-2000, the Chinaer 16 Antarctic expedition teams entered the inland East Antarctica and found three soil spots in the Southern Mount Harding, Grove Mountains, East Antarctica. It is the first case that soils are discovered in the inland in East Antarctica. Interestingly, the soils in this area show clay fraction migration, which is different from other cold desert soils. In addition, several moraine banks are discovered around the Mount Harding. The soil properties are discussed as below. Desert pavement commonly occurs on the three soil site surfaces, which is composed of pebbles and fragments formed slowly in typical desert zone. Many pebbles are subround and variegated. These pebbles are formed by abrasion caused by not only wind and wind selective transportation, but also salt weathering and thaw-freezing action on rocks. The wind blows the boulders and bedrocks with snow grains and small sands. This results in rock disintegration, paved on the soil surface, forming desert pavement, which protects the underground soil from wind-blow. The desert pavement is the typical feature in ice free zone in Antarctica. There developed desert varnish and ventifacts in this area. Rubification is a dominant process in cold desert Antarctic soils. In cold desert soils, rubification results in relatively high concentrations of Fed in soil profile. Stained depth increases progressively with time. The content of Fed is increasing up to surface in each profile. The reddish thin film is observed around the margin of mafic minerals such as biotite, hornblende, and magnetite in parent materials with the microscope analyzing on some soil profiles. So the Fed originates from the weathering of mafic minerals in soils. Accumulations of water-soluble salts, either as discrete horizons or dispersed within the soil, occur in the soil profiles, and the salt encrustations accumulate just beneath surface stones in this area. The results of X-ray diffraction analyses show that the crystalline salts consist of pentahydrite (MgSO4-5H2O), hexahydrite (MgSO4-6H2O), hurlbutite (CaBe2(PO4)2), bloedite (Na2Mg(S04)2-4H2O), et al., being mainly sulfate. The dominant cations in 1:5 soil-water extracts are Mg2+ and Na+, as well as Ca2+ and K+, while the dominant anion is SO42-, then NO3-, Cl- and HCO3-. There are white and yellowish sponge materials covered the stone underside surface, of which the main compounds are quartz (SiO2, 40.75%), rozenite (FeSOKkO, 37.39%), guyanaite (Cr2O3-1.5H2O, 9.30%), and starkeyite (MgSO4-4H2O, 12.56%). 4) The distribution of the clay fraction is related to the maximum content of moisture and salts. Clay fraction migration occurs in the soils, which is different from that of other cold desert soils. X-ray diffraction analyses show that the main clay minerals are illite, smectite, then illite-smectite, little kaolinite and veirniculite. Mica was changed to illite, even to vermiculite by hydration. Illite formed in the initial stage of weathering. The appearance of smectite suggests that it enriched in magnesium, but no strong eluviation, which belongs to cold and arid acid environment. 5) Three soil sites have different moisture. The effect moisture is in the form of little ice in site 1. There is no ice in site 2, and ice-cement horizon is 12 cm below the soil surface in site 3. Salt horizon is 5-10 cm up to the surface in Site 1 and Site 2, while about 26cm in site 3. The differentiation of the active layer and the permafrost are not distinct because of arid climate. The depth of active layer is about 10 cm in this area. Soils and Environment: On the basis of the characteristics of surface rocks, soil colors, horizon differentiation, salt in soils and soil depth, the soils age of the Grove Mountains is 0.5-3.5Ma. No remnants of glaciations are found on the soil sites of Mount Harding, which suggests that the Antarctic glaciations have not reached the soil sites since at least 0.5Ma, and the ice cap was not much higher than present, even during the Last Glacial Maximum. The average altitude of the contact line of level of blue ice and outcrop is 2050m, and the altitude of soil area is 2160m. The relative height deviation is about 110m, so the soils have developed and preserved until today. The parental material of the soils originated from alluvial sedimentary of baserocks nearby. Sporepollen were extracted from the soils, arbor pollen grains are dominant by Pinus and Betula, as well as a small amount Quercus, Juglans, Tilia and Artemisia etc. Judging from the shape and colour, the sporepollen group is likely attributed to Neogene or Pliocene in age. This indicates that there had been a warm period during the Neogene in the Grove Mountains, East Antarctica.
Resumo:
Aspergillus niger100;100,-Ca2+Mg2+Al3+Fe3+K+Mn2+,H2PO4-SO42-Cl-,XRD:;
Resumo:
,:SO2 -4 > K+ Ca2 + HCO-3 >Na + Mg2 + Cl - > NO-3 NH+4 > PO3 -4 ,HCO-3 > SO2 -4 Ca2 + > Mg2 + Cl - > K+ Na + NO-3 > NH+4 > PO3 -4 ;,HCO-3 Ca2 + Mg2 + ,HCO-3 Ca2 + ,SO2 -4 HCO-3 Ca2 + ,K+ NH+4 HCO-3 ,Ca2 + ,K+ Mg2 + ;
Resumo:
,:,,,,,HCO -3 > SO2 -4 > Ca2 + >Mg2 + > K+ NO-3 Cl - > Na + > NH+4 > PO3 -4 ,HCO32Ca ;,PO3 -4 ,Ca2 + NO-3 ,,,HCO-3 Ca2 + Mg2 + ,K+ NH+4 ;,HCO-3 Mg2 + ,,NH+4 NO-3 ,
Resumo:
, 20042005. , SO2 -4 , NH +4 , Ca2 + , NO -3 H+, pH, . 4, SO2 -4 , NH+4 , NO -3 , Ca2 +F- , K+Mg2 +, Na+Cl- , H+.
Resumo:
X()(PAFC)()XCa4Fe9O17Ca3A12(OH)12CaAl2Fe4O10Ca2(A1Fe)2O5Fe()Fe()-FeOOHPAFC
Resumo:
()()()() 1 DOCDOCDOCDOCDOCDOCDOC 2 DOC50cm 3 DOC 4 DOCDOCDOC 5 DOC 6 DOCDOCDOCDOCDOC 7 DOC()DOCDOCDOC7DOC810DOCDOC 8 DOCpHHCO3-SICPPCO2Ca2+Mg2+pHDOCHCO3-SICPPCO2DOC(=90%)HCO3-SICPPCO2DOCDOCDOC
Resumo:
CaCaCaMgKKCaMg Sr 1pHNO3-87Sr/86Sr0.707160.71051 2130 cm 3Ca > K > MgCaKSr, CaSrBaMn 4 88.66%77.28%58.88%85.64%CaMg 587Sr/86Sr87Sr/86Sr87Sr/86Sr 6SrCa2+87Sr/86SrCa2+Ca2+Ca2+Ca2+
Resumo:
TSPSO220051120051231TSPF-Cl-SO42-NO3-NH4+K+Na+Ca2+Mg2+TSP 1. TSP36.91313.44µg/m3106.60µg/m3SO42-> NH4+> Ca2+ > NO3-> K+ > Na+ > Cl- > Mg2+ > F-SO42- (23.0412.16µg/m3)NH4+(3.052.23µg/m3)3730TSPTSPCl-SO42-NO3-NH4+K+Na+Ca2+Mg2+/:1.295.231.352.371.731.221.841.231.02 2. TSPTSPTSPTSPTSPTSPTSPTSPTSPTSPTSPTSPTSPTSPCa2+Mg2+F-(RH)SO42-NO3-NH4+Cl- 3. TSPTSPpH6.270.41Q0.82TSPSO42-TSP 4. NH4+SO42-NO3-R0.850.65NH4+SO42-0.8TSPNH4+(NH4)2SO4Ca2+Mg2+R=0.72 5. 2005TSPSO42-/ Ca2+13.64SO42-/ Ca2+20NO3-/SO42-0.15
Resumo:
NO3-SO42-AsCd 1. pH7.408.118.347.95DO7.51 mg/l8.27 mg/lDOTDSTDS152.78 mg/l 2. HCO3-HCO3- > SO42 -> Cl- > NO3-HCO3-SO42 -Cl-NO3-Ca2+Ca2+ > Mg2+ > Na+ > K+Ca2+ > Na+ > Mg2+ > K+ NO3- 3. Zn>Cr>Cu>As>Al>Pb>CdZn37.72g/lCd0.24g/lZn>Cr>Pb>As>Cu=Al>CdZn>Cr>As>Pb>Al>Cu>CdZn>Cr>Cu>As >Al>Pb>CdCuCr6.12g/l7.61g/lPbCdAl12.7 g/lZnAl AlAsPbZnCuCrAsAl 4. NO3-SO42-AsAl
Resumo:
65%()2006-42007-42217 1AS11-HCAG11-HCRFC-30KOH1mmol ( 06min) 1mmol30mmol (631min)1.5ml/min390.9992~0.9999RSD%5%RSD%5%(RSD%=13.8%)80~120% 2 pH2.496.923.2873.8%pH4.042%pH5.016.505.8318.4%(pH<4.0) 101028S/cm248S/cm2.252.8S/cm18.1S/cm 3SO42-NO3-H+Ca2+NH4+154.1mol/L33.9mol/L520.7mol/L226.4mol/L158.3mol/LH+496.9mmol/m2/yrH+78%SO42-151.5mmol/m2/yr195.3mmol/m2/yrCa2+NH4+Mg2+Na+K+NO3-Cl-138.7mmol/m2/yr50.9mmol/m2/yr26.8mmol/m2/yr11.4mmol/m2/yr32.3mmol/m2/yr12.6mmol/m2/yr SO42-NO3-Ca2+NH4+43.1mol/L19.3mol/L33.0mol/L49.5mol/L[H+]0.5mmol/m2/yrSO42-Ca2+NH4+13.9mmol/m2/yr10.6mmol/m2/yr15.9mmol/m2/yrMg2+Na+K+NO3-Cl-2.1mmol/m2/yr5.9mmol/m2/yr3.0mmol/m2/yr6.2mmol/m2/yr3.2mmol/m2/yr 4714.24mol/L9.35mol/L2.79mol/L4.95mol/L1.35mol/L2.31mol/L-7.9%-4.7%-6.1%18.7%-25.1%-7.5%-25.5%58.1%1.719.2%6.6%0.592.2%13.2% 13.5mmol/m2/year 8.9mmol/m2/year2.6mmol/m2/year26.7mmol/m2/year 14.5mmol/m2/year1.59mmol/m2/year 0.43mmol/m2/year0.04mmol/m2/year0.1mmol/m2/year 0.17mmol/m2/year 5pH(12h)5080% 6() 7pH250.1%19%1/2 8
Resumo:
CHO(20065~20074)(76)pH() (1) pH4.11(2.30~ 6.04)62.10 s•cm-1 (6.60 ~ 1630.00 s•cm-1)93.2%pHpH (2) SO42-> Ca2+> H+> NH4+> NO3-> Cl-> F->HCOO-> Mg2+> K+> CH3COO-> Na+> (COO)22-> PO43-> NO2-SO42-Ca2+H+NH4+NO3-148.15 mol•L-181.89 mol•L-177.74 mol•L-143.80 mol•L-131.50mol•L-131.97%17.67%16.78%9.45%6.54%SO42-NO3-Ca2+NH4+77%(Ca2+NH4+)H+NO3-nss-SO42-()NH4+SO42-NO3-SO42-NO3-SO42-SO2NO3-NOxCa2+Mg2+NH4+Cl-()HClCl2 (3) [HCOO-]T[CH3COO-]T[(COO)22-]T9.29 mol•L -16.47 mol•L-15.06 mol•L-122.28 mol•L-19.39 %>>> (4) (r= 0.86)NO3-nss-SO42-K+Na+Ca2+(F/A)aq(54%)(45%)(~) (5) pH514.79% (0.42~91.14%)3.66% (0.02~31.55%)pH31.95%26.16%8.02%11.17%pHpHpH (6) 94%SO42-Ca2+H+NH4+NO3-90.149.847.326.019.2 mmol•m-2•yr-1SO42-Ca2+H+NO3-NH4+TIN(TIN= NH4+ -N+ NO3- -N+ NO2- -N)45.7 mmol•m-2•yr-1NH4+NO3-TIN57.0%41.9%TINNOxP1.97 mmol•m-2•yr-1PP6%>>>(HCOO-CH3COO-CH3CH2COO-)47.2%
