Copper isotope ratios in magmatic

Geology,C –H –O –S –Pb isotope systematics and geochronology of the Yindongpo gold deposit,Tongbai Mountains,central China:Implication for ore genesisJing Zhang a ,Yan-Jing Chen b ,c ,⁎,Franco Pirajno d ,Jun Deng a ,Hua-Yong Chen c ,e ,Chang-Ming Wang aaState Key Laboratory of Geological Processes and Mineral Resources,China University of Geosciences,Beijing 100083,China bKey Laboratory of Orogen and Crust Evolution,Peking University,Beijing 100871,China cKey Laboratory for Mineralogy and Metallogeny,Guangzhou Institute of Geochemistry,Chinese Academy of Sciences,Guangzhou 510640,China dCentre for Exploration Targeting,School of Earth and Environment,University of Western Australia,35Stirling Highway,Crawley WA 6008,Australia eCODES ARC Center of Excellence in Ore Deposits,University of Tasmania,7001,Australiaa b s t r a c ta r t i c l e i n f o Article history:Received 19September 2012Received in revised form 10January 2013Accepted 13January 2013Available online 11February 2013Keywords:GeologyIsotope geochemistry Ore genesisYindongpo gold deposit Tongbai MountainsThe Yindongpo gold deposit is located in the Weishancheng Au –Ag-dominated polymetallic ore belt in Tongbai Mountains,central China.The ore bodies are stratabound within carbonaceous quartz –sericite schists of the Neoproterozoic Waitoushan Group.The ore-forming process can be divided into three stages,represented by early barren quartz veins,middle polymetallic sul fide veinlets and late quartz –carbonate stockworks,with most ore minerals,such as pyrite,galena,native gold and electrum being formed in the middle stage.The average δ18O water values changed from 9.7‰in the early stage,through 4.9‰in the middle stage,to −5.9‰in the late stage,with the δD values ranging between −65‰and −84‰.The δ13C CO 2values of ore fluids are between −3.7‰and +6.7‰,with an average of 1.1‰.The H –O –C isotope systematics indi-cate that the ore fluids forming the Yindongpo gold deposit were probably initially sourced from a process of metamorphic devolatilization,and with time gradually mixed with meteoric water.The δ34S values range from −0.3‰to +5.2‰,with peaks ranging from +1‰to +4‰.Fourteen sul fide samples yield 206Pb/204Pb values of 16.990–17.216,207Pb/204Pb of 15.419–15.612and 208Pb/204Pb of 38.251–38.861.Both S and Pb isotope ratios are similar to those of the main lithologies of the Waitoushan Group,but differ from other lithologic units and granitic batholiths in the Tongbai area,which suggest that the ore metals and fluids originated from the Waitoushan Group.The available K –Ar and 40Ar/39Ar ages indicate that the ore-forming process mainly took place in the period of 176–140Ma,during the transition from collisional compression to extension and after the closure of the oceanic seaway in the Qinling Orogen.The Yindongpo gold deposit is interpreted as a stratabound orogenic-style gold system formed during the transition phase from collisional compression to extension.The ore metals in the Waitoushan Group were extracted,transported and then accumulated in the carbona-ceous sericite schist layer.The carbonaceous sericite schist layer,especially at the junction of collapsed anti-cline axis and fault structures,became the most favorable locus for the ore bodies.©2013Elsevier B.V.All rights reserved.1.IntroductionThe concept of orogenic-type gold deposit was first introduced by Bohlke (1982)and then thoroughly addressed by Groves et al.(1998),Kerrich et al.(2000)and Goldfarb et al.(2001)to de fine a class of structurally controlled gold deposits formed by fluids,assumed to have originated mainly from syn-to post-orogenic metamorphic devolatilization.Several structurally-controlled lode gold deposits in China and elsewhere have been assigned to the class of orogenic gold de-posits (Chen et al.,2000a,2000b,2001,2012a,2012b;Chen et al.,2005a,2008;Crispini et al.,2011;Fan et al.,2003;Hart et al.,2002;Jiang et al.,2009a,2009b;Kerrich et al.,2000;Mao et al.,2002;Rui et al.,2002;Zhao et al.,2011;Zhou et al.,2002)and interpreted to have mainly formed during continental collision tectonics.Consequently,a tectonic model for collisional orogeny,metallogeny and fluid flow (CMF model)was established to interpret the metallogenic mechanism and space –time patterns of various genetic types including orogenic gold lodes (Chen and Fu,1992;Chen et al.,2004;Pirajno,2009,2012).Many structurally-controlled Ag±Pb –Zn,Pb –Zn±Ag,Cu and Mo lodes have also been interpreted as orogenic type (Chen,2006),including the Tieluping and Yindonggou Ag deposits in Henan province (Chen et al.,2004,2005b;Sui et al.,2000;Zhang et al.,2009);the Gaojiabaozi Ag de-posit in Liaoning province (Wang et al.,2008;Yu et al.,2009);the Tiemurt Pb –Zn –Cu (Zhang et al.,2012),the Wulasigou Cu (Zheng et al.,2012)and Mengku Fe (Wan et al.,2012)deposits in Xinjiang;the Lengshuibeigou,Xigou and Wangpingxigou Pb –Zn±Ag deposits inOre Geology Reviews 53(2013)343–356⁎Corresponding author at:Key Laboratory of Orogen and Crust Evolution,Peking University,Beijing 100871,China.E-mail address:yjchen@ (Y.-J.Chen).0169-1368/$–see front matter ©2013Elsevier B.V.All rights reserved./10.1016/j.oregeorev.2013.01.017Contents lists available at SciVerse ScienceDirectOre Geology Reviewsj ou r n a l h o m e p a g e :w w w.e l s e v i e r.c o m /l o c a t e /o r e g e or e vHenan province(Qi et al.,2007,2009;Yao et al.,2008);the Bainaimiao Cu±Au deposit in Inner Mongolia(Li et al.,2008);and the Zhifang Mo (Deng et al.,2008),the Dahu Mo–Au(Li et al.,2011a;Ni et al.,2008, 2012)and the Longmendian Mo(Li et al.,2011b)deposits in Henan province.Recent advances have not only improved the understanding of ore genesis and exploration targeting in orogenic belts,but also intro-duced several new uncertainties.One of them is whether the orogenic type deposit can occur as stratabound style;if not,how to clarify the ge-netic type of deposits formed by metamorphic ore-formingfluids that focused in specific lithologies(e.g.,carbonaceous beds,stratigraphic un-conformities);and if so,what are the geochemical signatures and metal sources of these stratabound orogenic-type deposits.Several gold de-posits,such as Muruntau in Uzbekistan,Kumtor in Kyrgyzstan,Sukhoi Log in Russia,Homestake in USA(Bierlein and Maher,2001;Goldfarb et al.,2001)and Sawayardun in Xinjiang(Chen et al.,2012a,b;Liu et al.,2007),Yangshan in Gansu(Yang et al.,2006,2009)and Yindongpo in Henan(Chen,1995;Zhou et al.,2002),show stratabound characteris-tics but alsofit an orogenic-style of mineral system.In this contribution we report the results of studies on the Yindongpo gold deposit,which occurs in the Weishancheng ore belt in Tongbai Mountains,Henan province,central China(Zhang et al., 2011).The Yindongpo deposit contains32,337kg Au at an average grade of7.61g/t,130.5t Ag at an average grade of38.41g/t, and26,792t Pb at an average grade of0.95%(Zhang Guan,pers. comm.).The deposit is characterized by a stratabound to stratiform ge-ometry,and has attracted the interest of geologists for its metallogenic style,ore genesis,spatial distribution and economic potential(Chen and Fu,1992;HBGMR,1985;Hu et al.,1988;Luo,1992;Xu et al.,1995; Zhang et al.,2009).However,an integrated study on the deposit has not been reported as yet.This paper summarizes the geology and H–O–C–S stable and radiogenic isotopic systematics of the Yindongpo gold deposit,and discusses the sources of ore metals andfluids,as well as the ore-forming mechanism(s).2.Geological setting2.1.Regional geologyThe Tongbai Mountains are part of the Central China Orogen (Fig.1A)that was formed during the Mesozoic collision between the Yangtze and North China continents(Wu and Zheng,2012),with the Shang-Dan fault zone being interpreted as main suture(Fig.1B).The Shang-Dan suture zone comprises ophiolite slices and Paleozoic–Triassic sediments,the latter containing radiolarian fossils(Du et al., 1997;Feng et al.,1994).North of the Shang-Dan suture is the northern Qinling accretionary belt(Chen et al.,2009)that includes the Qinling Metamorphic Complex,the Erlangping and Kuanping terranes.These terranes are south of the Luanchuan fault,which is accepted as the boundary between the Qinling Orogen and the reactivated southern margin of the North China Craton(Fig.1B).The Qinling Metamorphic Complex comprises the Qinling Group(pre-Rodinian metamorphic basement)and Neoproterozoic to Paleozoic granitoids which were mostly formed in magmatic-arc settings.The Erlangping terrane, which hosts the Weishancheng ore belt,is bound by the Zhu-Xia fault to south and the Waxuezi fault to north(Fig.1B,C),and mainly com-prises Neoproterozoic–Early Paleozoic volcano-sedimentary succes-sions and associated intrusions that formed in a back-arc basin(Chen et al.,2004;Hu et al.,1988;Sun et al.,2002).In the Kuanping terrane, the Kuanping Group mainly consists of Mesoproterozoic muscovite–biotite(quartz)schists,metagabbros,basaltic rocks and ophiolite slices, and is interpreted as a Mesoproterozoic ophiolite complex accreted to the southern margin of North China Craton(Gao et al.,1991;He etal.,Fig.1.Schematic map showing the geology of the Tongbai Mountains(Zhang et al.,2011).A)Location of the Qinling–Tongbai–Dabie Mountains.B)Tectonic framework of the Qinling–Tongbai–Dabie Mountains.C)Geology of the Tongbai Mountains and the location of the Yindongpo gold deposit.SDF,Shang-Dan suture zone;MLF,Mian-Lue suture zone.SBF,San-Bao fault;F1,Machaoying fault;F2,Luanchuan fault;F3,Waxuezi fault;F4,Zhu-Xia fault;F5,Tong-Shang fault;F6,Tan-Lu fault;F7,Duanzhuang(Duanzhuang–Duimenchong)fault.344J.Zhang et al./Ore Geology Reviews53(2013)343–3562009;Hu et al.,1988;Luo,1992;Zhao et al.,2004,2009).The Kuanping Group is locally covered by or interleaved with Neoproterozoic to Early Paleozoic metamorphic sediments,and thereby is interpreted to have developed in Neoproterozoic or Early Paleozoic(Chen et al.,2009;and reference therein).The Weishancheng Au–Ag-dominated polymetallic ore belt in the northern Tongbai Mountains,strikes WNW for about20km with a width of ca.1km,and is located in the Erlangping terrane,north of the Zhu-Xia fault(F4in Fig.1C).Its eastern and western extensions are covered by Wucheng and Nanyang Cenozoic basins,respectively. The ore belt contains the Yindongpo Au deposit,the Poshan Ag deposit and the Yindongling Ag-dominated polymetallic deposit,as well as nu-merous small ore deposits or occurrences(Figs.1and2).2.2.Local geologyAll the deposits and occurrences in the Weishancheng ore belt are hosted in low-grade metamorphic carbonaceous rocks of the Waitoushan Group(Figs.1and2),which has a total thickness of about2500m and consists of mica schist,quartz–mica schist,plagioclase–amphibole schist, marble and minor quartzite.The Waitoushan Group is divided into the Upper Waitoushan,Mid-dle Waitoushan and Lower Waitoushan Formations(abbreviated as UWF,MWF and LWF respectively in the following text andfigures), each containing several members(Fig.3).The UWF is mainly composed of quartz–mica schist.The MWF comprises plagioclase–amphibole schist and carbonaceous quartz–sericite schist.The LWF contains more plagioclase–amphibole schist and marble.In the Tongbai Mountains,the Waitoushan Group is unique for its high abundance of organic carbon,Au,Ag and other metallic elements(Chen and Fu, 1992;HBGMR,1994).The Yindongpo gold deposit is hosted in the sec-ond member of MWF(Fig.3).The axis of the Heqianzhuang anticline strikes90°–120°,and is subparallel with the regional faults(Fig.2).This anticline comprises the Waitoushan Group and Dalishu Formation of the Erlangping Group.The anticlinal axis dies to the east and the hinge plunges towards the west.The Waitoushan Group occurs along the axis of the anticline,whereas the Dalishu Formation forms its southern limb.The orebodies are mainly sited in the hinge and/or along the two limbs of the anticline(Figs.2B,4,5A,C).The NW-trending faults are the dominant regional structures,and are crosscut by the ENE-trending,post-ore faults(Fig.2A).The largest fault is labeled F1and controls the Yindongpo deposit(Fig.2B).The anticline was intruded by granitic plutons,such as the Taoyuan Paleozoic granodiorite pluton and Liangwan monzogranite pluton.The Taoyuan granodiorite yields biotite K–Ar ages of390–357Ma,with the magma being sourced from the basement of northern Qinling accre-tionary belt(Zhang et al.,1999,2000).It intruded the Erlangping Group and Early Paleozoic quartz diorite then was intruded by granites,such as the Liangwan pluton,of Mesozoic age(Yanshanian;see below) (Figs.1and2).The Liangwan monzogranite pluton intruded the Dalishu Formation of the Erlangping Group(Figs.1and2)at128–111Ma(bio-tite K–Ar,whole rock Rb–Sr isochrones)and originated from partial melting of the Tongbai complex in southern Qinling terrane,implying that the lower crust of northern Tongbai Mountains(corresponding to northern Qinling accretionary belt)contains the components fromtheFig.2.Schematic map showing regional and ore geology of the Yindongpo Au deposit.A)Geology of the Weishancheng ore belt after Zhang et al.(2011).B)Geology and distribution of the Yindongpo orebodies,modified after HBGMR(1994).Abbreviations:XLZ,Xialaozhuang;GLZ,Guolaozhuang;ZZ,Zhangzhuang;LJC,Luanjiachong;JZ,Jiangzhuang;WG,Weigou;NXG, Nanxiaogou;ZhZ,Zhuzhuang.345J.Zhang et al./Ore Geology Reviews53(2013)343–356southern Qinling terrane,via a northward-directed continental subducting slab (Zhang et al.,1999,2000,2011).3.Deposit geology3.1.Characteristics of the orebodiesThe Yindongpo gold deposit covers an area 2km long and 0.6–0.9km wide (Fig.2B).The distribution of the orebodies is strictly con-trolled by carbonaceous beds (graphite-rich quartz –sericite schists)and the Heqianzhuang anticline and fault systems (Figs.2and 4A).The orebodies are typically stratabound and lenticular in shape,or occur as saddles and veins,and generally dip with the hosting strata (Fig.2B).The orebodies in the northern limb of the anticline are steeper than those in the southern limb (Fig.2B).The contacts between orebodies and wallrocks are gradational and are determined by a cut-off grade.The depth of orebodies increases from southeast to northwest.Most of orebodies are hosted in the second member of MWF (Figs.2B,3and 4),especially in the silici fied quartz –sericite schist and/or carbonaceous quartz –sericite schist.The No.0exploration line divides the Yingdongpo deposit into east-ern and western sectors.The eastern sector contains 19ore bodies,with Nos.1,2,3and 3–1being thick,long and continuously mineralized (Figs.2B and 4).In the western ore sector,Nos.51,52,54and 55are the most important orebodies,but are thinner,smaller and less contin-uously mineralized than those in the eastern sector (Figs.2B and 4).The No.1orebody is the largest,with Au reserves accounting for 78%of the ore in eastern sector (HBGMR,1994).It is 1600m long,600m deep and 8m wide,with average grades of 6.23g/t Au and 50g/t Ag,respectively.The ores were mined by open pitting and underground operation.3.2.Ore types and ore mineral assemblagesAltered tectonite breccia,fine vein-disseminated silici fied schist,and silici fied (carbonaceous)quartz –sericite schist (Fig.5),are all Au,Ag,Fe,Cu,Sb,As,Bi,Pb,Zn,Co and Sn enriched,but only Au attained suf ficient ore grades to be economically extracted.Ore minerals include sul fides,native elements,sulfates and oxides (Fig.5),such as pyrite,chalcopy-rite,sphalerite,galena,native gold,electrum and argentite,and ac-counting for up to 10%of the ore by volume.Gangue minerals are mainly quartz,sericite and carbonate.Fine-grained graphite is com-monly present in the ores (Fig.5D).Cataclastic textures and fissure-fillings are commonly observed.Stockworks,veinlets,disseminations,and banded ores are the main ore styles (Fig.5).3.3.Mineralization stages and wallrock alterationOn the basis of the paragenetic sequences of minerals (Fig.6),ore petrography and crosscutting relationships,the ore-forming process can be divided into three stages,namely,an early-stage barren quartz veins or replacement with or without pyrite (Fig.5F),a middlestageFig.3.Lithostratigraphy and ore metal concentrations of the Waitoushan Group.From HBGMR (1994).346J.Zhang et al./Ore Geology Reviews 53(2013)343–356with polymetallic sul fides (Fig.5G,H),and a late stage of quartz –carbonate veinlets (Fig.5I).Abundant pyrite,galena,native gold,electrum and other ore minerals formed in the middle stage.Three stage fluid –rock interactions resulted in wallrock alteration,mainly including silici fication,sericitization,carbonation and chloritization.Silici fication is the most prominent and in the early stage it was pervasive.Locally,the wallrocks were completely re-placed by fine-grained quartz with minor sericite,forming sericite-bearing siliceous replacement and/or quartz veins.In this case,the primary fabrics of wallrocks,such as schistosity and cleavage,cannot be observed because they were obliterated by pervasive silici fication.In general,ore grades increase with increasing intensity of hydrother-mal alteration.4.Samples and analytical methodsMost samples in this study were collected from No.1orebody at Levels of 155,145,115and 75(the digits represent the meters above the sea level).Sampling was carried out taking into account the field recognition of lateral zonation and the three-stage evolution of the mineralization.Rock samples collected from different strata were pulverized in an agate mill under 200meshes.Mineral aggregates were taken from the specimens using tweezers and then were crushed into grains with sizes of 0.1–0.5mm.After panning and filtration,clean mineral grains (quartz,calcite,and sul-fides)were handpicked under the binocular microscope.In order to eliminate other interlocking minerals (e.g.sul fides),quartz separates were soaked in HNO 3-solution at a temperature between 60and 80°C for 12h and rinsed with deionized water.Then the separates were treated 6times using supersonic centrifugal clari fier and rinsed with deionized water for a week.The last rinsed water was monitored by an atomic absorption spectrophotometer to con firm that no ions were left.The samples were dried in an oven before analysis.For sul fides,approximately 10to 50mg were first leached in acetone to remove surface contamination and then washed by distilled water and dried at 60°C in the oven.The carbonate separates were only washed by distilled water and dried at 60°C in the oven.The analytical methods were explained in detail by Ding (1988).The carbon isotopic composition of fluid inclusion was measured on CO 2.Separated from fluid inclusions in quartz and calcite during thermal decrepitation,the CO 2gas was collected and condensed using a liquid nitrogen-alcohol cooling trap (−70°C)for analysis on a MAT-252mass spectrometry.Hydrogen isotope analysis of water contained in fluid in-clusions was collected in a similar manner.After collection the water was puri fied and then reduced using zinc to produce hydrogen which was analyzed on a MAT-253mass spectrograph.To measure oxygen iso-tope ratios,quartz separates were reacted with BrF 5at 500–550°C for at least 5h to generate O 2which was condensed using liquid nitrogen.The collected O 2was converted to CO 2at about 700°C with platinum as cat-alyzer,and then the CO 2was analyzed on MAT-252mass spectrometry.Sulfur isotope ratios in sul fides were analyzed on SO 2using Delta-S mass spectrometer.For lead isotope ratios,approximately 10to 50mg of sul fide samples was first leached in acetone to remove surface contamination and then washed by distilled water and dried at 60°C in the oven.Washed sul fides were dissolved in dilute mix solution of nitric acid and hydro fluoric acid.Following ion exchange chemistry,the lead in the solution was loaded onto rhenium filaments using a phosphoric acid –silica gel emitter.The lead isotopic compositions were measured on MAT-261thermal ioniza-tion mass spectrometer with the standard sample NBS 981.The H –O –C isotopes were measured in the State Key Laboratory of Lithosphere Evolution,Institute of Geology and Geophysics,Chinese Academy of Science.Isotopic data were reported in per mil relative to the Vienna SMOW standard for oxygen and hydrogen,and the Peedee Belemnite limestone (PDB)standard for carbon.Both sulfur and lead isotope analyses were finished at the Open Laboratory of Iso-topic Geochemistry,Chinese Academy of Geological Sciences.The Sul-fur isotopic compositions were reported relative to the Canyon Diablo Triolite (CDT)standard.Total uncertainties were estimated to be bet-ter than ±0.2‰for δ18O,±2.0‰for δD,±0.2‰for δ13C,and ±0.2‰for δ34S at the σlevel respectively.Estimated precision for the 206Pb/204Pb,207Pb/204Pb and 208Pb/204Pb ratios is about 0.1%,0.09%and 0.30%at the 2σlevel respectively.The K –Ar isochron age was analyzed by RGA-10dating system in Key Laboratory of Orogen and Crust Evolution,PekingUniversityFig.4.Simpli fied exploration sections showing orebodies of the Yindongpo Au deposit.Modi fied after HBGMR (1994).347J.Zhang et al./Ore Geology Reviews 53(2013)343–356and the systematic error of K –Ar dating is estimated to be b 4%.The 40Ar/39Ar plateau age was analyzed at the Geochronology Research Laboratory of Queen's University,Ontario,Canada.40Ar/39Ar analyses were performed by standard laser step-heating techniques described in detail by Clark et al.(1998).All data have been corrected for blanks,mass discrimination,and neutron-induced interferences.A plateau age is obtained when the apparent ages of at least three consecutive steps,comprising a minimum of 55%of the 39Ar k released,agreeFig.5.Geology,ore type and mineral assemblages of the Yindongpo gold deposit.A)Heqianzhuang anticline axis shown at an open pit;B)ore-hosting fault developed along the boundary between carbonaceous schist and two-mica schist;C)north limb of the No.55orebody (30°∠60°)and its foot-and hanging-walls;D)a small-size anticline in altered carbonaceous quartz schist;E)pyrite-bearing quartz veinlets in carbonaceous quartz schist;F)early-stage barren,milky quartz vein;G)pyrite-rich,high-grade ore;H)middle-stage ore rich in pyrite and galena;I)late-stage quartz-carbonate vein;J)chalcopyrite armored with covellite;K)euhedral pyrite in quartz;L.pyrite with cataclastic texture;M)sphalerite with thin film of tiny galena;N)sphalerite containing chalcopyrite droplets,forming exsolution texture;O)early-stage pyrite replaced by galena.348J.Zhang et al./Ore Geology Reviews 53(2013)343–356within 2σerror with the integrated age of the plateau segment.Errors and isotope-correlation diagrams represent the analytical precision at ±2σ.5.Isotope systematics 5.1.Hydrogen –oxygen isotopesThe δD and δ18O values for the Yindongpo ore deposit are listed in Table 1.The δ18O water was calculated according to the δ18O mineral and trapping temperature of fluid inclusion which was estimated according to homogenization temperature and its pressure correlation.The fluids of early-stage quartz (sample 99H09)have an δ18O water value of about +10.6‰,higher than the maximum for magmatic water,suggesting that the fluids were sourced from metamor-phic devolatilization rather than magmatism (Chen et al.,2005b,2008).It is common knowledge that magmatic fluids are generated from the magma above the temperature of 573°C (lowest eutectic point).The δ18O water ratio of the initial magmatic fluids is not higher than the δ18O quartz of the equilibrated magmatic rocks,due to 1000ln αquartz –water >0when T b 724°C.Hence the maximum δ18O water value of magmatic water was estimated to be 9‰(Fig.7).During continuous cooling and water –rock reaction processes,the δ18O water of magmatic water was reduced again along with the formation of hy-drothermal minerals such as quartz.If the fluids forming the Yindongpo deposit were initially magmatic and still kept δ18O water =+10.6‰when the temperature decreased to 414°C,their initial δ18O water must be far higher than 10.6‰.Such δ18O water value is obviously higher than the estimated maximum for magmatic water,also higher than the δ18O values of granitoids in Qinling –Tongbai Mountains,which range 6.1‰–10.4‰(Chen et al.,2000b ).Thus,the early stage fluid must be metamorphic in origin,instead of magmatic or meteoric,which is further supported by sulfur and lead isotope signatures,discussed ahead.The δ18O values of the middle-stage fluids range from +3.1‰to +5.5‰,averaging +4.9‰;whereas the δD values range from −68‰to −84‰,and average −75‰.Compared to the early-stage fluids,sam-ples of the middle-stage fluids clearly shift towards the meteoric water line (Fig.7),suggesting a signi ficant input of meteoric water into the fluid system.The δ18O water values of late-stage quartz and calcite are between −8.1‰and −3.7‰,averaging −5.9‰.Such low δ18O water values strong-ly indicate that the fluids were mainly sourced from meteoric water.Con-sidering the δD ratios in fluids vary in a narrow range (−65to −85‰)in early and middle stages,we estimate that the late stage δD water values are similar to the middle stage.These measured and estimated δD water values are close to that of Mesozoic meteoric water in Qinling Moun-tains (Fig.7).Assuming that the average δD water value of the late stage is same to that of the middle stage,the late stage samples are close to or shift towards the meteoric water line,especially to the domain of Mesozoic meteoric water in Qinling mountain range (Fig.7),which was drawn by Zhang (1989)from a H –O isotope geochemical study of numerous meteoric hydrothermal deposits formed in Mesozoic.This suggests that the late stage fluids are of meteoric origin.In conclusion,the average δ18O Water values changed from 9.7‰in the early stage,through 4.9‰in the middle stage and −5.9‰in the late stage,with the δD values ranging between −60‰and −90‰,strongly support that the ore fluids of the Yindongpo gold deposit were initially sourced from metamorphic devolatilization,and later changed to mainly meteoric water,from the early to the late stages of the mineralization process.5.2.Carbon isotopesThe δ13C CO 2values of the early-and middle-stage fluids forming the Yindongpo Au deposit widely vary between −3.7‰and +6.7‰,with an average of 1.1‰(Table 1).These values are higher than those of organic matter (ca.−27‰),atmospheric CO 2(−7to −11‰;Hoefs,2004),freshwater carbonate (−9to −20‰:Hoefs,2004),igneous rocks (−3to −30‰:Hoefs,2004;Zheng,1999),continental crust (−7‰:Faure,1986)and the mantle (−5to −7‰:Hoefs,2004);and therefore,the CO 2in the fluids forming the Yindongpo mineral system cannot independently have been supplied by any one or a mixture of the above-mentioned reservoirs.The marine carbonate,which is the carbon reservoir with highest δ13C value (ca.0.5‰;Schidlowski,1998),must be considered as the source of CO 2in the ore fluids,at least as a necessary end-member,considering that released CO 2via decarbonation could have higher δ13C than the residue carbonates (Jiang et al.,2004;Tang et al.,2011,in press ).The δ13C values of the carbonates in Waitoushan Group range from +1.9‰to +2.9‰(Table 1),suggesting that they most likely provided CO 2(with the highest δ13C value of 6.7‰)for the Yindongpo ore fluid-system via metamorphic de-carbonation.The δ13C values of calcite in late-stage veins at Yindongpo deposit range from −2.4‰to −0.6‰(Table 1),and correspond to the δ13C CO 2values of −2.8‰to −1.0‰calculated using the carbon isotope fractionation equation of for calcite –CO 2system (Chacko et al.,1991).The calculated δ13C CO 2values are lower than the δ13C CO 2values of ore-forming fluids in early and middle stages,suggesting that the fluid system was mixed with or replaced by meteoric water,which ef ficiently reduced the δ13Cvalue.Fig.6.Paragenetic sequence for major minerals of the Yindongpo Au deposit.349J.Zhang et al./Ore Geology Reviews 53(2013)343–356。

矿床地质MINERAL DEPOSITS2024年2月February ，2024第43卷第1期43（1）：177~194*本文得到国家重点研发计划课题（编号：2022YFC2905101）、科技基础资源调查专项课题（编号：2022FY101701）、中国地质调查局项目（编号：DD2023350、DD20221692）联合资助第一作者简介孙海瑞，男，1987年生，正高级工程师，长期从事岩石及矿床地球化学研究。

Email:*******************通讯作者吕志成，男，1966年生，研究员，长期从事成矿规律与找矿预测研究。

Email:******************收稿日期2023-08-16；改回日期2024-02-02。

孟秋熠编辑。

文章编号：0258-7106（2024）01-0177-18Doi:10.16111/j.0258-7106.2024.01.011粤东金坑锡铜多金属矿燕山期岩浆热液叠加成矿*孙海瑞1,2，吕志成1,2**，李永胜1,2，韩志锐3，于晓飞1,2，杜轶伦1,2（1中国地质调查局发展研究中心，北京100037；2自然资源部矿产勘查技术指导中心，北京100037；3中国工程科学杂志社，北京100029）摘要金坑锡铜多金属矿位于广东莲花山断裂带北东段，是近些年来在粤东地区新发现的典型锡铜多金属矿，关于该矿床的成因类型和成矿机制一直存在较大争议。

矿区勘查工作在马山矿段首次发现伴有明显铜矿化的热液隐爆角砾岩，对于揭示矿床成因具有重要意义。

LA-ICP-MS 锆石U-Pb 年代分析结果显示，花岗质角砾成岩年龄约为150Ma ，εHf (t )值为-8.20~-4.55，二阶段Hf 模式年龄值为1.73~1.49Ga ，指示岩浆主要来自于中元古代地壳物质，并有地幔物质加入。

硫化物原位硫同位素分析结果显示，不同阶段硫化物硫同位素组成具有明显差别。

第一阶段（Py-Ⅰ）和第二阶段(Py-Ⅱ)黄铁矿存在显著的硫同位素变化，前者为-0.65‰~1.11‰（n =5），后者为1.30‰~1.93‰（n =5），与Py-Ⅱ共生黄铜矿同位素值为1.42‰~1.87‰（n =16）。

矿业英语(蒋林筛选)abnormality 反常一般说anormaly的人更多吧adit 平硐adit collar 平硐口adit cut mining 平硐开采adit entrance 平硐口adit mine 平硐开采矿山adit mouth 平硐口adjoining rock 围岩正常人说country rock吧advance bore 超前钻孔也有说pilot hole的agglomeration 聚集air adit 通风平硐就是air wayair drill 风钻air pick 风镐air pipe 风管air shaft 风井airleg 气腿风钻听起来更像汉语alluvial gold 砂金更常见的说法是placer alluvium 冲积层ammon dynamite 硝安炸药ammon explosive 硝铵炸药amphibole 角闪石analyst 化验员assayer更准确点anchor bolt 锚杆angle of bedding 层理面倾斜角anticline 背斜anticlinorium 复背斜antimony 锑assay 试金正常人都叫化验automatic feed 自动给料automatic feeder 自动给矿机automatic installation 自动设备auxiliary adit 辅助平峒auxiliary equipment 辅助设备auxiliary fan 辅助扇风机auxiliary level 辅助平巷auxiliary shaft 辅助竖井azimuth angle 方位角back bolting 顶板锚杆支护back filling 充填back stoping 上向梯段回采ball mill 球磨机band ore 带状矿石bank height 台阶高度barrier pillar 安全煤柱这个就叫safety pillar也行basalt 玄武岩base charge 基本装药量;炮眼底部装约bearing 煤层走向;轴承bed 地层belt feeder 带式给矿机beneficiating method 选矿法bin 矿仓biotite 黑云母bit 钎头就叫钻头也行blast hole 炮眼blasting charge 装炸药blind shaft 暗井正常人都说盲井block 采区;块;滑车组block caving method 分段崩落采矿法正确说法是sublevel caving board and pillar 房柱式开法跟room and pillar是一样的bolting 锚杆支护borehole 钻孔borehole survey 钻孔测量boring bar 钻杆drillrodbornite 斑铜矿bottom dump skip 底卸式箕斗bottom wall 下盘正确说法是heading wall 或footwallbucket excavator 多斗挖掘机bulldozer 推土机cage 罐笼calcite 方解石calculation of reserves 储量计算capstan winch 绞盘carbonaceous 炭质的casing pipe 套管caved area 崩落区cement 水泥charge 装药chloride 氯化物chute 溜道circuit 回路classification screen 分级筛classifier overflow 分级机溢流clay 粘土clay band 粘土夹层clay bed 粘土层cleaning 精浮选就是精选没有浮cleavage 劈理closed circuit crushing 闭路破碎collar cave 井颈塌落combustion 燃烧common drift 共用平巷compressed air 压缩空气compressor 压缩机concentrate 精矿contaminated air 污浊空气contour map 等高线图control 第;操纵;治理conveyor 运输机copper 铜core 岩心core sample 岩心试样coring 岩心钻进crack 裂缝crane 起重机cross adit 石门cross cutting 石门掘进cross level 横巷crush 破碎crusher 破碎机crusher jaw 破碎机颚crushing rolls 辊碎机crystal 晶体curvature 曲率cushioning 缓冲cuthole 掏槽炮眼cyanide 氰化物dacite 英安岩daily advance 日掘进进度day drift 平硐day output 日产量degree of extraction 回采率正确说法是recovery dehydration 脱水dehydrator 脱水器deister table 垂特摇床delamination 剥离delay 迟滞delay action blasting 迟发爆破densification 浓缩deposition 沉淀depot 仓库desulphurization 脱硫detonate 起爆detonating charge 起爆装药detonating cord 导爆线detonator 雷管developement drift 开拓平巷diagram 曲线图diameter 直径diamond 金刚石diesel electric locomotive 柴油电机车dike 岩脉dilution 稀释注意这个大部分时间翻译为贫化diorite 闪长岩dioxide 二氧化物dip angle 倾角directional drilling 定向钻进discontinuity 不连续性dissolubility 溶解性dissolvent 溶剂ditch 沟道dolomite 白云石drain 排水管drill bar 钻杆drill bit 钎头drill rig 钻车drill rod 钻杆drilling jumbo 钻车dry assay 干法试金dump car 翻斗车elastic 弹性的elastic strain 弹性应变electrum 银金矿engineering 工程entry 水平巷道entry advance 平巷推进entry bottom 平巷底entry brushing 巷道挑顶entry driving 平巷掘进entry pillar 平巷煤柱environment 环境environment pollution 环境污染environment protection 环境保扩evaporation 蒸发exploration 探矿explosion 爆炸explosive 炸药extraction 采掘extraction drift 回采平巷eye survey 目测face 叫工作面！！！facilities 设备fan 扇风机fault 断层fault basin 断层盆地fault coal 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right 采矿权moisture 湿气mud fluid 钻探用泥桨narrow vein 薄矿脉nickel 镍nitrate 硝酸盐non electric initiation system 非电起爆装置non metal 非金属open circuit 开路open pit bench 露天矿阶段opencast mining 露天开采opencast mining machinery 露天采矿机械opencast mining method 露天开采法opening 开拓巷道opening driving 开拓掘进opening for drainage 排水巷道ore 矿石ore bearing vein 含矿脉ore benefication 选矿ore bin 矿石仓ore block 矿块ore concentration 选矿ore concentration plant 选矿厂ore crusher 矿石破碎机ore deposit 矿床ore dilution 矿石贪化ore drawing 放矿ore dressing 选矿ore dressing plant 选矿厂ore extraction 矿石开采ore pass 放矿溜道orebody 矿体orefield 矿区outlet 出口outlet shaft 上风竖井output 产量;输出功率overhead 架空的oxidation 氧化oxide 氧化物packing 充填panel 采区paraffin 石蜡pass 溜道pillar 矿柱placer 砂矿placer gold 砂金pneumatic pick 风镐portal 入口powder 炸药powder drift 爆破平巷precipitate 沉淀物prop 支柱prospecting 勘探prospecting adit 勘探平硐prospecting bore 勘探钻孔prospecting drift 勘探巷道prospecting drill 勘探钻机prospecting guide 勘探标志prospecting schaft 探竖井prospecting tool 勘工具prospecting trench 勘探沟prospecting work 勘探工作prospective value 预期值prospector 勘探者pulp 矿浆pulverization 粉碎pump 泵pump capacity 泵能力pump chamber 泵房pump dredge 泵式挖掘船pump head 泵唧扬程pump man 司泵工pumping compartment 泵隔间pumping equipment 排水设备pumping head 水头pumping out 扬水pumping plant 泵唧装置pumping shaft 排水井pumping station 水泵站pumproom 泵房pumpset 泵唧装置pumpway 泵隔间purity 纯度pyrite 黄铁矿quarry 采石场quarry bank 露天矿的梯段quartz 石英radioactive 放射性的radius 半径raise 天井reagent 试剂reclamation operation 复田工作reflotation 再浮选regional 区域的regional metamorphism 区域变质regional prospecting 区域勘探register 记录器;计量表retreating mining 后退式开采return air 回风rigidity 刚度rock dump 废石堆roller 辊rolling shaft 溜道roof 顶板room 室;矿房rope 绳索rubble 砾石rupture 破裂safety berm 保安平台safety pillar 保安矿柱sample 试样sampler 采样器sampling 取样sampling device 采样器sampling method 取样法sampling mill 试样磨机sand 砂scraper 扒矿机scraper apron 耙斗后壁scraper box 扒斗scraper bucket 耙斗screen 筛screening 筛分seam 地层sedimentary rock 沉积岩service cage 辅助罐笼service drift 辅助平巷service entry 辅助平巷service raise 人行天井service roadway 辅助巷道service shaft 辅助竖井service track 辅助线set 组shaft 上风竖井就是竖井shale 页岩shallow mine 浅矿shank 钎尾short wall mining 短壁采煤法shot boring 钻粒钻进shot drill 钻粒钻机shrinkage 留矿sieve 筛silicate 硅酸盐silicatization 硅化酌siliceous rock 硅质岩石sill 底梁sink 开凿;下沉slurry 矿泥;洗涤用水stage 阶段stope 回采工祖叫做采场！！！stoping 回采stoping and filling 充填回采stoping drift 回采平巷stoping face 回采工祖stoping hole 回采炮眼stoping layout 采矿设计stoping limit 临界品位stoping machine 采矿机stoping method 回采方法storage 仓库sublevel 分段sublevel caving method 分段崩落开采法sublevel caving system 分段崩落开采法sublevel crosscut 中间水平石门sublevel drift 分阶段平巷sublevel interval 分阶段间距sublevel long hole benching 分层台阶深孔开采sublevel method 分段开采法sublevel mining 分段回采sublevel open stope method 分段无充填工祖采矿法sublevel roadway 分阶段平巷sublevel stoping 分段回采采掘subsurface flow 地下水流subterraneous quarry 地下采石场subvertical 立井subvertical shaft 暗竖井sulphate 硫酸盐sulphide 硫化物sulphide concentrate 硫化矿精矿sulphide dust explosion 硫化物尘末爆炸surface mine 露天矿山surface miner 露天矿工surface mining 露天开采surface mining method 露天采矿法surface plan 地面平面图surface plant 地面设备surface stripping 地表剥离surface subsidence 地表塌陷surface tension 表面张力surface transport 地面运输survey 测量survey mark 测量标记surveying 测量surveying compass 测量罗盘surveying equipment 测量仪器surveying instrument 测量仪器surveying marker 测量标surveying rod 测量标尺surveyor 测量员surveyor's rod 测量标尺susceptibility 磁化率;感受性syncline 向斜tailing 尾矿tailing elevator 尾矿提升机tailings 尾矿tailings disposal plant 尾矿处理装置tailings pond 尾煤沉淀池tails 尾矿take off the gangue 清理矸石tectonic 构造的telescopic conveyor 伸缩输传送带telescopic drilling post 伸缩式钻机柱telescopic prop 伸缩支柱tensile strain 拉伸变形tension 张力test pit 探井thickener 浓缩机thril 联络小巷thriling 联络小巷throat 巷道口topographic map 地形图track 轨道trailer 拖车train 系列trainroad 临时铁路tram 矿车trolley 矿车undercut level 底切水平underlayer 下伏层upper level 上水平upper limit 上限ventilate 通风ventilation raise 通风天井ventilation reversal 反向通风ventilation scheme 通风系统图vibrate 振动vibrated concrete 振实的混凝土vibrating ball mill 振动球磨机vibrating chute 振动式滑槽vibrating conveyor 振动输送机vibrating dryer 振动干燥机vibrating feeder 振动给矿机vibrating mill 振动磨碎机vibrating screen 振动筛vibrating sieve 振动筛vibrating system 振动系统vibrating table 振动台vibrodrill 振动钻机vibrodrilling 振动打钻vibrofeeder 振动给矿机viscidity 粘度volcanic rock 火山岩wall rock 围岩waste fill 废石充填waste heap 废石堆waste ore 废矿water drainage 排水water drainage roadway 排水平巷water drip 水滴water entry 排水平巷water filled charge 充水装药water flooding 注水法water proof 防水的water pump 水泵well 井winch 绞车working area 采区working bed height 采煤层厚度working bench 开采台阶working coditions 开采条件zinc 锌zircon 锆石zone 带zone of compression 压缩带zone of contact 接触带zone of fracture 破裂带zone of oxidation 氧化带。

锂辉石密度1. 简介锂辉石是一种重要的矿物，其化学式为LiAl(Si2O6)，属于正长石类。

它是一种含锂的硅酸盐矿物，常见于火山岩和高温、高压结晶岩中。

锂辉石具有多种用途，包括作为锂资源的来源、电池材料以及陶瓷和玻璃工业的原料等。

本文将介绍锂辉石的密度及其相关知识。

2. 密度定义密度是物质单位体积内所含质量的量度。

在国际单位制中，密度的单位为千克每立方米（kg/m³）或克每立方厘米（g/cm³）。

密度可以通过测量物体质量和体积来计算。

3. 锂辉石的密度锂辉石是一种具有相对较高密度的矿物。

根据实验数据和文献资料，锂辉石的密度约为2.6-3.1 g/cm³。

具体数值可能会因样品来源、纯度和结晶状态等因素而有所差异。

4. 影响锂辉石密度的因素锂辉石的密度受多种因素的影响，以下是一些主要因素：4.1 化学成分锂辉石的化学成分对其密度有一定影响。

化学成分中的主要元素包括锂、铝和硅。

一般来说，元素的原子质量越大，物质的密度也越大。

因此，在化学成分相同的情况下，含有较高原子质量元素的锂辉石样品可能具有更高的密度。

4.2 结晶状态锂辉石在不同温度和压力条件下结晶形成不同结构状态。

这些结构状态可能会影响其密度。

例如，在高温高压条件下形成的β-锂辉石相比室温条件下形成的α-锂辉石具有更高的密度。

4.3 杂质含量杂质是指在晶体中存在但并非其基本组分的物质。

杂质含量对晶体物性有重要影响，包括密度。

在锂辉石中，常见的杂质元素包括钠、钾、钙等。

这些杂质可以改变晶体结构和原子间距，从而影响其密度。

4.4 结晶质量结晶质量是指晶体的纯度和完整度。

纯度较高、结晶较完整的锂辉石样品通常具有更高的密度。

不同产地和加工方法可能会导致锂辉石样品的结晶质量不同，进而影响其密度。

5. 锂辉石的应用锂辉石作为一种重要的矿物资源，具有广泛的应用前景。

以下是一些主要应用领域：5.1 锂资源锂是一种重要的工业金属，广泛应用于电池、冶金、化工等领域。

２０２３／０３９（１１）：３４７９ ３４９０ＡｃｔａＰｅｔｒｏｌｏｇｉｃａＳｉｎｉｃａ　岩石学报ｄｏｉ：１０．１８６５４／１０００ ０５６９／２０２３．１１．１６索青宇，李昌昊，申萍等．２０２３．黑龙江多宝山铜（钼）矿床叠加成矿：辉钼矿Ｒｅ Ｏｓ年龄和硫化物原位硫同位素证据．岩石学报，３９（１１）：３４７９－３４９０，ｄｏｉ：１０．１８６５４／１０００－０５６９／２０２３．１１．１６黑龙江多宝山铜（钼）矿床叠加成矿：辉钼矿Ｒｅ Ｏｓ年龄和硫化物原位硫同位素证据索青宇１，２，３　李昌昊１，２，３　申萍１，２，３ 赵俊康４　楚翔凯１，２，３ＳＵＯＱｉｎｇＹｕ１，２，３，ＬＩＣｈａｎｇＨａｏ１，２，３，ＳＨＥＮＰｉｎｇ１，２，３ ，ＺＨＡＯＪｕｎＫａｎｇ４ａｎｄＣＨＵＸｉａｎｇＫａｉ１，２，３１ 中国科学院地质与地球物理研究所，中国科学院矿产资源研究重点实验室，北京　１０００２９２ 中国科学院大学地球与行星科学学院，北京　１０００４９３ 中国科学院地球科学研究院，北京　１０００２９４ 紫金矿业集团股份有限公司矿产地质勘查院，厦门　３６１０００１ ＫｅｙＬａｂｏｒａｔｏｒｙｏｆＭｉｎｅｒａｌＲｅｓｏｕｒｃｅｓ，ＩｎｓｔｉｔｕｔｅｏｆＧｅｏｌｏｇｙａｎｄＧｅｏｐｈｙｓｉｃｓ，ＣｈｉｎｅｓｅＡｃａｄｅｍｙｏｆＳｃｉｅｎｃｅｓ，Ｂｅｉｊｉｎｇ１０００２９，Ｃｈｉｎａ２ ＣｏｌｌｅｇｅｏｆＥａｒｔｈａｎｄＰｌａｎｅｔａｒｙＳｃｉｅｎｃｅｓ，ＵｎｉｖｅｒｓｉｔｙｏｆＣｈｉｎｅｓｅＡｃａｄｅｍｙｏｆＳｃｉｅｎｃｅｓ，Ｂｅｉｊｉｎｇ１０００４９，Ｃｈｉｎａ３ ＩｎｎｏｖａｔｉｏｎＡｃａｄｅｍｙｏｆＥａｒｔｈＳｃｉｅｎｃｅ，ＣｈｉｎｅｓｅＡｃａｄｅｍｙｏｆＳｃｉｅｎｃｅｓ，Ｂｅｉｊｉｎｇ１０００２９，Ｃｈｉｎａ４ ＧｅｏｌｏｇｉｃａｌＰｒｏｓｐｅｃｔｉｎｇＩｎｓｔｉｔｕｔｅ，ＺｉｊｉｎＭｉｎｉｎｇＧｒｏｕｐＣｏ ，Ｌｔｄ ，Ｘｉａｍｅｎ３６１０００，Ｃｈｉｎａ２０２３ ０６ ２９收稿，２０２３ ０９ ２０改回ＳｕｏＱＹ，ＬｉＣＨ，ＳｈｅｎＰ，ＺｈａｏＪＫａｎｄＣｈｕＸＫ ２０２３ ＳｕｐｅｒｉｍｐｏｓｅｄｍｉｎｅｒａｌｉｚａｔｉｏｎｏｆｔｈｅＤｕｏｂａｏｓｈａｎＣｕ（Ｍｏ）ｄｅｐｏｓｉｔｉｎＨｅｉｌｏｎｇｊｉａｎｇＰｒｏｖｉｎｃｅ：ＩｎｄｉｃａｔｅｄｂｙｔｈｅｍｏｌｙｂｄｅｎｉｔｅＲｅ Ｏｓｉｓｏｔｏｐｉｃｄａｔｉｎｇａｎｄｓｕｌｆｕｒｉｓｏｔｏｐｅｃｏｍｐｏｓｉｔｉｏｎ．ＡｃｔａＰｅｔｒｏｌｏｇｉｃａＳｉｎｉｃａ，３９（１１）：３４７９－３４９０，ｄｏｉ：１０．１８６５４／１０００ ０５６９／２０２３．１１．１６Ａｂｓｔｒａｃｔ Ｐｏｒｐｈｙｒｙｃｏｐｐｅｒｄｅｐｏｓｉｔｓｃａｎｂｅｄｅｆｏｒｍｅｄｂｙｓｕｂｓｅｑｕｅｎｔｍａｇｍａｔｉｃ ｔｅｃｔｏｎｉｃ ｍｅｔａｍｏｒｐｈｉｃｅｖｏｌｕｔｉｏｎ，ｒｅｓｕｌｔｉｎｇｉｎｔｈｅｃｏｎｓｅｑｕｅｎｔｓｕｐｅｒｉｍｐｏｓｅｄｍｉｎｅｒａｌｉｚａｔｉｏｎａｎｄｔｈｅｒｅｍｏｂｉｌｉｚａｔｉｏｎｏｆｐｒｅ ｅｘｉｓｔｉｎｇｏｒｅｓ Ｔｈｉｓｐｒｏｃｅｓｓｍｉｇｈｔｐｏｔｅｎｔｉａｌｌｙｉｎｃｒｅａｓｅｔｈｅｏｒｅｇｒａｄｅａｎｄ／ｏｒｒｅｓｏｕｒｃｅ ＷｅｆｏｃｕｓｏｎｔｈｅＤｕｏｂａｏｓｈａｎＣｕ（Ｍｏ）ｄｅｐｏｓｉｔ，ｔｗｏｍｉｎｅｒａｌｉｚａｔｉｏｎｐｅｒｉｏｄｓｗｅｒｅｉｄｅｎｔｉｆｉｅｄｗｉｔｈｉｎｔｈｅＤｕｏｂａｏｓｈａｎｄｅｐｏｓｉｔｉｎｔｈｉｓｓｔｕｄｙ，ｉ ｅ ，ｔｈｅｐｏｒｐｈｙｒｙｐｅｒｉｏｄａｎｄｔｈｅｓｕｐｅｒｉｍｐｏｓｅｄｐｅｒｉｏｄ ＴｅｎｍｏｌｙｂｄｅｎｉｔｅｓａｍｐｌｅｓｆｒｏｍｔｈｅｓｕｐｅｒｉｍｐｏｓｅｄｐｅｒｉｏｄｙｉｅｌｄＲｅ Ｏｓｉｓｏｔｏｐｉｃｍｏｄｅｌａｇｅｓｏｆ４３５ ６±１０ ５Ｍａｔｏ４４６ １±７ １Ｍａ，ａｎｄａｎｉｓｏｃｈｒｏｎａｇｅｏｆ４４０ １±４ ５Ｍａ（ＭＳＷＤ＝０ ５６） Ｃｏｍｂｉｎｅｄｗｉｔｈｔｈｅａｇｅｏｆｍａｇｍａｔｉｃａｃｔｉｖｉｔｙｄｅｖｅｌｏｐｅｄｉｎｔｈｅｒｅｇｉｏｎ，ｉｔｉｓｓｕｇｇｅｓｔｅｄｔｈａｔｔｈｅｓｕｐｅｒｉｍｐｏｓｅｄｍｉｎｅｒａｌｉｚａｔｉｏｎａｎｄｔｈｅＬａｔｅＯｒｄｏｖｉｃｉａｎｂａｓａｌｔｉｃａｎｄｅｓｉｔｅｓｈｏｕｌｄｂｅｆｏｒｍｅｄｉｎａｕｎｉｆｉｅｄｇｅｏｌｏｇｉｃａｌｅｖｅｎｔｉｎｔｈｅＤｕｏｂａｏｓｈａｎｄｅｐｏｓｉｔ Ｔｈｅｉｎ ｓｉｔｕｓｕｌｆｕｒｉｓｏｔｏｐｅｒｅｓｕｌｔｓｏｆｃｈａｌｃｏｐｙｒｉｔｅａｎｄｐｙｒｉｔｅｆｒｏｍｄｉｆｆｅｒｅｎｔｍｉｎｅｒａｌｉｚａｔｉｏｎｐｅｒｉｏｄｓｓｈｏｗｔｈａｔｔｈｅａｖｅｒａｇｅδ３４Ｓｖａｌｕｅｏｆｃｈａｌｃｏｐｙｒｉｔｅｉｎｔｙｐｉｃａｌｐｏｒｐｈｙｒｙｖｅｉｎｓｉｓ－２ １２‰，ｗｈｉｌｅｔｈｏｓｅｏｆｃｈａｌｃｏｐｙｒｉｔｅａｎｄｐｙｒｉｔｅｉｎｔｈｅｓｕｐｅｒｉｍｐｏｓｅｄｍｉｎｅｒａｌｉｚａｔｉｏｎａｒｅ－１ ７８‰ａｎｄ－１ ０３‰，ｒｅｓｐｅｃｔｉｖｅｌｙ，ｗｈｉｃｈｆａｌｌｉｎｔｏｔｈｅｒａｎｇｅｏｆａｍａｎｔｌｅｓｏｕｒｃｅ，ｉｎｄｉｃａｔｉｎｇｔｈａｔｔｈｅｓｕｌｆｕｒｏｆｔｈｅｄｅｐｏｓｉｔｍａｉｎｌｙｃｏｍｅｓｆｒｏｍｔｈｅｍａｇｍａ Ｈｏｗｅｖｅｒ，ｐｒｅｖｉｏｕｓｓｔｕｄｉｅｓｈａｖｅｆｏｕｎｄｔｈａｔｃｈａｌｃｏｐｙｒｉｔｅｆｏｒｍｅｄｄｕｒｉｎｇｔｈｅｓｕｐｅｒｉｍｐｏｓｅｄｍｉｎｅｒａｌｉｚａｔｉｏｎｈａｓｌｏｗδ３４Ｓｖａｌｕｅｓ（－１２ ９‰～－５ ６‰）ａｓａｒｅｓｕｌｔｏｆｔｈｅｍｉｇｒａｔｉｏｎｏｆｌｉｇｈｔｓｕｌｆｕｒ３２Ｓｗｈｉｃｈｉｓｅａｓｉｌｙｃａｒｒｉｅｄｂｙｌａｔｅ ｓｔａｇｅｆｌｕｉｄｓａｎｄｄｅｐｏｓｉｔｅｄｉｎａｒｅａｓｏｆａｌｏｗｅｒｓｔｒｅｓｓ Ｔｈｅｉｓｏｔｏｐｉｃｃｏｍｐｏｓｉｔｉｏｎｓｉｎｄｉｃａｔｅｔｈａｔｔｈｅｍｉｎｅｒａｌｉｚｅｄｅｌｅｍｅｎｔｓｉｎｔｈｅｓｕｐｅｒｉｍｐｏｓｅｄｐｅｒｉｏｄｅｉｔｈｅｒｏｒｉｇｉｎａｔｅｄｆｒｏｍｎｅｗｍａｇｍａｔｉｓｍｏｒｉｎｈｅｒｉｔｅｄｆｒｏｍｐｒｅ ｅｘｉｓｔｉｎｇｒｏｃｋ（ｏｒｅ）ｂｏｄｉｅｓＫｅｙｗｏｒｄｓ ＤｕｏｂａｏｓｈａｎｐｏｒｐｈｙｒｙＣｕ（Ｍｏ）ｄｅｐｏｓｉｔ；Ｓｕｐｅｒｉｍｐｏｓｅｄｍｉｎｅｒａｌｉｚａｔｉｏｎ；Ｒｅ Ｏｓｉｓｏｔｏｐｅａｇｅ；Ｓｕｌｆｕｒｉｓｏｔｏｐｅ摘　要 斑岩型矿床易受后期岩浆、构造、变质等地质作用影响，使得矿床自身发生改造变形。

锆石成因矿物学与锆石微区定年的综述发布时间：2021-05-31T13:49:05.760Z 来源：《基层建设》2021年第3期作者：李璇[导读] 摘要：锆石是一种硅酸盐矿物，在中酸性火成岩中很常见，也存在于变质岩和其他沉积物中。

河北地质大学河北石家庄 050031摘要：锆石是一种硅酸盐矿物，在中酸性火成岩中很常见，也存在于变质岩和其他沉积物中。

锆石是地球上形成最古老的矿物之一，因其稳定性好而成为同位素地质年代学最重要的定年矿物。

通过微区原位定年技术，能够给出有关寄主岩石的地质演化历史等重要信息，这可以为地质过程的精细年代学格架的建立提供有效的证据。

文章主要对锆石的微区原位测试技术、锆石的成因类型进行综述，并阐述其存在问题和发展方向。

关键词：锆石成因；微区原位测试；锆石U-Pb法引言传统意义上，锆石一直被视为具有高度稳定性的矿物，能持久保持矿物形成时的物理和化学特征，特别是元素和同位素特征。

普通铅含量低，富含U,Th等放射性元素，离子扩散速率低，封闭温度高等特点，因此被广泛应用于岩石学、矿物学和地球化学研究中。

以精细的锆石矿物学研究为基础，开展同位素定年工作，锆石已成为U-Pb法定年的理想对象。

1.研究现状对锆石的研究现状从以下几个方面进行讨论：锆石按照成因分类分为岩浆锆石、变质锆石和热液锆石。

第一类为岩浆岩中的锆石，岩浆锆石是指在岩浆中结晶形成的锆石，一般锆石自形程度较高，在双目镜下呈现无色透明。

锆石在硅中等饱和-饱和的岩浆岩中较多，在硅不饱和的岩浆岩中则较少，变质岩、沉积岩中可以保留部分原岩岩浆锆石残留核。

岩浆锆石一般具有岩浆振荡环带，通过观察发现一般中基性的岩浆锆石具有较宽的振荡环带，这是因为高温条件下微量元素扩散快；而酸性的岩浆锆石形成的振荡环带较窄，是因为低温条件下微量元素的扩散速度慢。

第二类为变质岩中的锆石，在变质作用过程中形成的锆石。

具有变质成因的锆石可以分为以下三类，包括变质结晶锆石，变质增生锆石和变质重结晶锆石。

专利名称：QUANTITATIVE ANALYSIS OF COPPER IN MATERIAL MAINLY COMPOSED OF ZINCOXIDE发明人：SATOU MASUMI申请号：JP6084984申请日：19840330公开号：JPS60205238A公开日：19851016专利内容由知识产权出版社提供摘要：PURPOSE:To elevate the accuracy of quantitative analysis by coinciding acid concentrations of a sample solution which is prepared by adding boronic acid to material dissolved in hydrochloric acid and hydrofluoric acid with a solution for calibration curve to measure the absorbance thereof at the wavelength of 324.8nm with an atomic absorptiometer separately, which are compared to the calibration curve. CONSTITUTION:Acid concentrations are coincided of a sample solution which is prepared by adding boric acid to material dissolved in hydrochloric acid and hydrofluoric acid with a solution for calibration curve to remove the effect thereof while both the solutions are put on an atomic absorptiometer separately to measure the absorbance thereof at the wavelength of 324.8nm. Then, the integrated values of the absorbances are used as measured value and compared to the calibration curve prepared by measuring the solution for calibration curve to determine the concentration of copper. Thus, the quantitative analysis of trace of copper can be done at a high accuracy employing the atomic absorptiometer.申请人：MEIDENSHA KK更多信息请下载全文后查看。

锆石结构特征及其研究内容与意义锆石作为一种副矿物广泛存在于各类岩石中，具有耐熔、耐腐蚀的特性，化学性质极其稳定，当原岩经历后期地质作用发生改变时，锆石可以被很好地保存下来。

此外，锆石是U、Th、Hf、REE等微量元素的主要富集矿物，这些元素可以作为测定岩石形成年龄的母同位素或探讨原岩形成过程的重要指示物(Hoskin and Schaltegger, 2003)。

人们对于锆石的研究和利用由来已久且应用广泛，主要包括利用其U-Th-Pb同位素进行年龄计算，Lu-Hf同位素体系和O同位素结合示踪原岩源区，近几年来还增加了对其Zr同位素的研究，这些在地壳和岩石圈地幔的时间演化过程中具有重要意义(Dhuime et al., 2012; Harrison et al., 2005; Valley et al., 2005; Wilde et al., 2001）。

1. 锆石化学成分和内部结构锆石是一种硅酸盐矿物，化学式为Zr[SiO4]，除了主要含Zr外，还包括Hf、Nb、Ta、Th和REE等元素。

化学成分是ZrO2一般为67.2wt%，SiO2约32.8wt%。

主要存在于酸性岩和变质岩中，沉积岩中的锆石也是来自风化的火成岩和变质岩，多为碎屑锆石。

根据成因，锆石可以被分为岩浆锆石和变质锆石，观察其内部结构的常用方法有HF酸蚀刻图像、背散射电子（BSE）图像和阴极发光电子（CL）图像。

在CL图像中，部分锆石可见清晰的核边结构。

岩浆锆石通常具有震荡环带结构（图1（a）），少部分有扇形分带的结构。

振荡环带的宽度与锆石寄主岩石的成分和锆石结晶时岩浆温度有关，微量元素在岩浆温度锆石扩散速度较快快，因而锆石结晶时形成的环带较宽（如辉长岩中的锆石）；低温时微量元素扩散慢，形成的环带较窄（如I型和S型花岗岩中的锆石）(Rubatto and Gebauer, 2000)。

扇形分带的结构是由于锆石结晶时外部环境变化导致各晶面的生长速率不一致(Vavra et al., 1996)。