Geological and isotopic evidence for magmatic-hydrothermal

ARTICLE

Geological and isotopic evidence for magmatic-hydrothermal origin of the Ag –Pb –Zn deposits in the Lengshuikeng District,east-central China

Changming Wang &Da Zhang &Ganguo Wu &

M.Santosh &Jing Zhang &Yigan Xu &Yaoyao Zhang

Received:7August 2012/Accepted:27March 2014/Published online:8April 2014#Springer-Verlag Berlin Heidelberg 2014

Abstract The Lengshuikeng ore district in east-central China has an ore reserve of ～43Mt with an average grade of 204.53g/t Ag and 4.63%Pb+Zn.Based on contrasting geological characteristics,the mineralization in the Lengshuikeng ore district can be divided into porphyry-hosted and stratabound types.The porphyry-hosted minerali-zation is distributed in and around the Lengshuikeng granite porphyry and shows a distinct alteration zoning including minor chloritization and sericitization in the proximal zone;sericitization,silicification,and carbonatization in the periph-eral zone;and sericitization and carbonatization in the distal zone.The stratabound mineralization occurs in volcano-sedimentary rocks at ～100–400m depth without obvious zoning of alterations and ore minerals.Porphyry-hosted and stratabound mineralization are both characterized by early-stage pyrite –chalcopyrite –sphalerite,middle-stage acanthite –native silver –galena –sphalerite,and late-stage pyrite –quartz –calcite.The δ34S values of pyrite,sphalerite,and galena in the ores range from ?3.8to +6.9‰with an average of +2.0‰.The C –O isotope values of siderite,calcite,and dolomite range from ?7.2to ?1.5‰with an average of ?4.4‰(V-PDB)and from +10.9to +19.5‰with an average of +14.8‰

(V-SMOW),respectively.Hydrogen,oxygen,and carbon iso-topes indicate that the hydrothermal fluids were derived main-ly from meteoric water,with addition of minor amounts of magmatic water.Geochronology employing LA –ICP –MS analyses of zircons from a quartz syenite porphyry yielded a weighted mean 206Pb/238U age of 136.3±0.8Ma considered as the emplacement age of the porphyry.Rb –Sr dating of sphalerite from the main ore stage yielded an age of 126.9±7.1Ma,marking the time of mineralization.The Lengshuikeng mineralization classifies as an epithermal Ag –Pb –Zn deposit.

Keywords Stable isotope .Geochemistry .Porphyry .Stratabound .Ag –Pb –Zn .Lengshuikeng

Introduction

The Lengshuikeng ore district,located in the Jiangxi Province of east-central China (Fig.1a ),contains more than 50ore bodies belonging to seven deposits hosted in granite porphyry,pyroclastic,and carbonate rocks.The ore reserves in Lengshuikeng have been estimated at ～43Mt with average grades of 2.11%Pb,2.61%Zn,204.53g/t Ag,0.08g/t Au,and 0.01%Cd.The ores can be grouped into two types:(1)porphyry-hosted (Yinluling,Baojia,and Yinzhushan)and (2)stratabound (Xiabao,Yinkeng,Yinglin,and Xiaoyuan).The porphyry-hosted mineralization is distributed within and around the Lengshuikeng granite porphyry,whereas the stratabound mineralization occurs in volcano-sedimentary rocks at ～100–400m depth.The spatial distribution of the porphyry-hosted and stratabound ore bodies,their mineral constituents,and the zoning of alteration assemblages are markedly different from those of typical porphyry deposits.

Editorial handling:T.Bissig and G.Beaudoin

C.Wang (*):

D.Zhang :G.Wu :M.Santosh :J.Zhang :Y .Xu :Y .Zhang

State Key Laboratory of Geological Processes and Mineral

Resources,China University of Geosciences,No.29,Xueyuan Road,Beijing 100083,People ’s Republic of China e-mail:wcm233@https://www.sodocs.net/doc/5111524502.html,

Y .Xu

No.912Geological Surveying Team,Bureau of Geology and Mineral Exploration and Development,Yingtan 334000,China

Miner Deposita (2014)49:733–749DOI 10.1007/s00126-014-0521-8

Over the past several decades,research in the Lengshuikeng ore district was focused on geological characteristics,mineral-ization,wall rock alteration,fluid inclusions,and geochemistry of the porphyry-hosted deposits (Deng 1991;Meng et al.2007;Wang et al.2010c ).Recently,stratabound Ag –Pb –Zn deposits have been found beneath the porphyry-hosted deposits,occur-ring in volcano-sedimentary rocks of the E ’huling Formation.This paper reports the geologic and isotopic characteristics of the porphyry-hosted and stratabound ores,in combination with those from Chinese literature.The regional and the

Lengshuikeng Ag –Pb –Zn ore district geologies,including the occurrence of ore bodies,and associated hydrothermal alter-ation are described,followed by a discussion of the origin of the Ag –Pb –Zn deposits.

Regional geological setting

The Lengshuikeng ore district is located in northeastern Jiangxi Province,east-central China,close to the Shaoxing

–

Fig.1a Location map for the Lengshuikeng District.b Sketch map showing the Late Mesozoic volcanic-intrusive complex belt in SE China.c Sketch map showing the regional geology of the Lengshuikeng ore district and Dexing ore field (modified after Jiang et al.2011).Major faults in the study area:Shi –Hang Shiwandashan –Hangzhou as collision-induced suture zone between the Cathaysia and Yangtze blocks,SJ Shaoxing –Jiangshan,ZD Zhenghe –Dapu

Jiangshan(SJ)fault between the Cathaysia and Yangtze blocks(Fig.1b).This fault represents the eastern part of the Shiwandashan–Hangzhou(Shi–Hang)fault zone and is con-sidered to mark the collisional suture zone in SE China(Yao et al.2011).Geophysical and remote sensing data suggest that the SJ fault extends deep into the lower crust and upper mantle (Fig.1c;Wang et al.2010c).The collisional amalgamation of the Cathaysia and Yangtze blocks into the proto“South China”Block(SCB)began in the early Qingbaikou period (～950±50Ma)and was completed by the end of the Jinning Orogeny at ca.850Ma(Shu and Charvet1996;Charvet et al. 1996;Li et al.2008,2010;Zhang and Zheng2013).During the Sinian(ca.850–600Ma),the Yangtze and Cathaysia blocks were rifted.In the Caledonian(600–405Ma),the Yangtze and Cathaysia blocks collided for a second time and reunited within the SCB(Zhou et al.2002;Wang et al.2010a, b).During the Variscan(405–270Ma),extension within the SCB resulted in Paleozoic intracontinental rifts.The Indosinian collision between the South China and North China blocks occurred from the Palaeozoic to Late Triassic(ca.270–208Ma;Wang et al.2013a,2014a). Magmatic activity during208to180Ma is documented by bimodal magmatism in southeastern Hunan Province and the A-type granitic magmatism in southern Jiangxi Province(Zhao et al.1998;Yu et al.2006,2010).From Triassic to Early Jurassic(180–145Ma),most areas of the Wuyi Mountains in the northeastern part of the Cathaysia Block(Fig.1b)were folded and uplifted before undergoing extensional collapse.The region ex-perienced Early Cretaceous granite magmatism(145–100Ma) and the formation of large-scale Late Cretaceous–Paleogene red bed sedimentary basins between100and70Ma(Jahn 1974;Jahn et al.1990;Zhou et al.2006;Shu et al.2009;Wang et al.2014b).

The Precambrian units include greenschist facies metamorphic rocks dated at1,000–800Ma(Fig.1c;Li et al.1996;Shu and Charvet1996;Zhou et al.2002; Shu et al.2009).The Cambrian and Ordovician rocks are mainly sandstone,mudstone,and carbonaceous mudstone. Silurian sedimentary rocks are absent.The Devonian, Carboniferous,and Permian strata comprise shallow marine to littoral facies clastic rocks,limestone,and dolomite.The Lower Triassic series consists of muddy limestone and shale. Middle Triassic strata are absent in most areas of the Wuyi Mountains.

The Wuyi Mountains are largely composed of Late Mesozoic volcanic rocks and associated clastic strata (Fig.1c).Lower Jurassic strata include conglomerate and coarse arkosic sandstone,quartz sandstone,and siltstone with carbonaceous mudstone and coal-bed intercalations.Middle Jurassic strata are composed of terrestrial clastic rocks and bimodal volcanic rocks.Upper Jurassic strata comprise andes-ite and rhyolitic tuffs and tuffaceous siltstone(Liu1985;Ye 1987).Lower Cretaceous strata include rhyolitic welded tuffs with basalt intercalations(Yu et al.2006).Upper Cretaceous siltstone and mudstone are intercalated with gypsum-bearing layers and basalt,the latter with an age of105–98Ma(Yu et al.2001).Paleogene strata include coarse clastic rocks,siltstone,and mudstone with inter-calated gypsum and oil-bearing shale.Neogene silt-stones locally overlie the Paleogene rocks.

Southeast China is characterized by extensive magmatism, which formed a belt of volcanic-intrusive complexes(Fig.1b). Two major tectono-magmatic periods have been recognized in the Wuyi Mountains:the Indosinian and the Yanshanian.The Indosinian magmatic period lasted from240to208Ma(Xie et al.2006).The Yanshanian igneous rocks formed during two main stages of Early Yanshanian(208–145Ma)and Late Yanshanian(145–90Ma)and are characterized by abundant rhyolitic volcanic rocks and highly aluminous granitoids(Jahn et al.1976;Chen1999;Li2000;Deng et al.2010,2011,2014; Zhou et al.2006;Zhao et al.2012).

Geology of the Lengshuikeng ore district

Deposit geology

The stratigraphic sequence in the Lengshuikeng District com-prises the Jurassic Daguding and E’huling Formations.The Daguding Formation is composed of andesite and rhyolitic tuffs and tuffaceous siltstone.The E’huling Formation is composed of tuffs,rhyolite,tuffaceous siltstone,sandstone, and manganese-and iron-rich carbonates,which are the main host of the stratabound ores.

The NE-striking F1fault dipping toward NW(Figs.2and 3a)comprises the northern segment of the Hushi fault.The most prominent structural feature in the Lengshuikeng District is F2reverse fault(Figs.2and3a).The stratabound fracture along the manganese-and iron-rich carbonate strata(Fig.3a) was cemented by later ore sulfide minerals and hydrothermal alteration minerals.

Middle Jurassic and Early Cretaceous magmatic rocks are exposed in the Lengshuikeng District(Fig.2).The Jurassic igneous rocks are mainly granitic including the Yinluling, Yinzhushan,Biaojia,and Yinglin porphyries.The Yinzhushan granite porphyry has been dated as162–159Ma (Meng et al.2007;Zuo et al.2010).The Early Cretaceous rocks include quartz syenite porphyry,rhyolite porphyry, alkali-feldspar granite porphyry,and mafic dykes(Fig.2). The quartz syenite porphyries crop out in the southeastern and northwestern parts of the Lengshikeng District(Fig.2),

with widely dispersed chloritization,sericitization,silicifica-tion,and carbonatization,with associated pyrite.Wang et al.(2010c )and Meng et al.(2007)reported that rhyolite porphyry and alkali-feldspar granite porphyry cut all the granite por-phyry and pyroclastic carbonate ore-hosted rocks (Fig.3)as well as the quartz syenite porphyry.

The least hydrothermally altered granite porphyries contain phenocrysts (15–35%)of quartz,plagioclase,K-feldspar,and biotite in a groundmass (65–85%)of subhedral K-feldspar,quartz,plagioclase,and minor biotite.Accessory minerals (～1%)are mainly magnetite,zircon,and apatite.Most quartz crystals are xenomorphic and exhibit undulose extinction.The quartz syenite porphyries contain phenocrysts (33–55%)of K-feldspar (～20%),biotite (～10%),and plagioclase (～8%)in a groundmass (45–67%)of subhedral K-feldspar,biotite,and quartz.K-feldspar phenocrysts are euhedral to subhedral,have a grain size of 2–5mm,and are locally replaced by sericite.Plagioclase phenocrysts are euhedral to subhedral,3–6mm in size,with evidence of weak silicification and sericitization.Biotite phenocrysts are 0.5–1.0mm in size and show alteration to chlorite and carbonate.

Ore bodies and wall rock alteration

Among the various ore deposits,the Baojia porphyry-hosted deposit is the most important,accounting for 52%of the total ore reserve in the Lengshuikeng District (Fig.2).

The porphyry-hosted ore bodies (Fig.3a )are associated with NNE-striking F 2reverse faults or comprise of fracture fillings in veins and breccias.Associated with the porphyry-hosted ore bodies is a distinct zoning of alteration and ore minerals,both vertically and laterally (Fig.3b,c ).An inner (or proximal)zone in the granite porphyry is characterized by enrichments in lead,zinc (with grade Pb+Zn >5%)with minor disseminated chalcopyrite and pyrite,and with minor chlorite and sericite alteration.The intermediate zone surrounds the inner zone near the contact between the granite porphyry and country rocks.This intermediate zone exhibits strong sericitization,carbonatization,and silicification,and in some cases,high-grade native silver mineralization (Ag >200g/t),with minor galena –sphalerite vein mineralization (Fig.4a ).The outer peripheral (or distal)zone is hosted by volcano-sedimentary country rocks to the granite porphyry and is de-fined by weakly developed silver,galena,sphalerite veins (Ag <100g/t;Pb+Zn <2%),and vein sericite and carbonate.Stratabound mineralization is hosted by manganese –iron carbonate layers of the E ’huling Formation (～5.0–33.1-m thickness)between tuffaceous sandstone and rhyolitic crystal tuff (Jiangxi Bureau of Geology and Mineral Exploration and Development (JBGMED)1982;Meng et al.2007).These rocks are characterized by high-grade native silver minerali-zation (Ag >200g/t),lead,zinc (with grade Pb+Zn >5%)as veins and breccias,with minor vein chlorite,sericite,and carbonate (Fig.4b,c ).Ore mineralogy and paragenesis

The mineralization in stratabound and porphyry-hosted ores can be divided into three stages (Fig.5):stage 1,pyrite –chalcopyrite –sphalerite;stage 2,silver minerals –galena –sphalerite;and stage 3,pyrite –quartz –calcite.The mineral assemblage of stage 1is dominantly pyrite and Fe-rich sphal-erite,with small amounts of chalcopyrite,cubanite,galena,arsenopyrite,pyrrhotite,and minor quartz (Fig.6a –c ).Stage 1mineralization was accompanied by chloritization and sericitization,replacing K-feldspar and plagioclase crystals in rhyolitic crystal tuff and granite porphyry.Siderite is intergrown with sphalerite but occurs mostly as overgrowths on sphalerite or as monomineralic cement in breccias and thin veinlets.Stage 2was the principal stage of silver –lead –zinc mineralization.This stage is characterized by sericitization and carbonatization,and minor chloritization.The silver –lead –zinc minerals of stage 2fill the manganese –

iron

Fig.2Geological map of the Lengshuikeng Ag –Pb –Zn ore district (after JBGMED 1982).Sections a and b are shown in Fig.3a –c

carbonate stratabound fractures.The dominant silver minerals are acanthite (Ag 2S)and native silver,which occur in fissures within manganese –iron carbonate or in the intergranular space between manganese –iron carbonate and early sulfides.In ad-dition,fine-grained canfieldite (Ag 8SnS 6),proustite (Ag 3AsS 3),aerosite (Ag 3SbS 3),Ag-bearing tetrahedrite (Cu 12Sb 4S 13),and kustelite (Ag,Au)occur in the intergranular pores of manganese –iron carbonate or as inclusions in galena,sphalerite,and other sulfides.The galena is euhedral and coarse-grained (Fig.6e ).V eins,veinlets,or disseminated silver minerals –gale-na –sphalerite are disseminated in the intergranular pores of manganese –iron carbonate (Fig.6f –h ).Stage 1pyrite is cut by galena and sphalerite vein (Fig.6b ),sphalerite surrounded by galena (Fig.4d ),and sphalerite cut by ankerite –galena vein.

In

Fig.3Geological features along sections a and b of the Baojiao deposit in the Lengshuikeng ore district (after JBGMED 1982):a relationship of ore bodies,b alteration zoning,and c mineralized zone

stage 3,ore minerals are dominated by pyrite,with lesser galena,pyrrhotite,and arsenopyrite.Calcite,quartz,and quartz –pyrite are characterized by open-space filling textures such as comb,veins,and veinlets and cut the stage 2galena or sphalerite veins (Figs.4e,f and 6d ).

Sampling and analytical procedure for stable and radiogenic isotopes

Samples were collected from ore materials at the ?80,?120,?152,and ?160m levels of underground workings,

outcrops

Fig.4Macroscopic features of samples selected for ore mineralogy and paragenesis studies.a Porphyry-hosted ore with vein galena and with chloritization and sericitization.b Brecciated stratabound-type ore.c Stratabound-type ore with vein sphalerite and galena and with chloritization,sericitization,and carbonation (Lu et al.2012).d Sphalerite phase (stage 1)surrounded by galena (stage 2)(Lu et al.2012).e Pyrite (stage 1)intersected by quartz vein (stage 3).g Disseminated ore intersected by pyrite vein (stage 3).Sp sphalerite,Gn galena,Py pyrite,Chl chloritization,Ser sericitization,Cbn carbonation,and Qz quartz

(Fig.2)at ～160m.s.l.elevations,and two drill holes in the Lengshuikeng ore district.Pure mineral concentrates from the porphyry-hosted and stratabound ores and wallrocks were prepared using a combination of heavy liquid and magnetic-and hand-picking techniques,and these were then checked by X-ray diffraction to ensure mineral purity.

Sulfur isotope analyses of sphalerite,galena,and pyrite were carried out at the Resource and Environment Analysis Centre of the Geochemistry Institute,Chinese Academy of Sciences.Pyrite,galena,and sphalerite were combusted with CuO at 1,000°C,and the sulfur isotopic compositions was determined on a MAT-253mass spectrometer.The sulfur isotopic compositions were reported relative to the Canyon Diablo Triolite (VCDT)standard.Routine analytical precision for standards material was ±0.2‰.

Rhodochrosite,siderite,calcite,and ankerite were handpicked under a stereomicroscope and washed with dis-tilled water.Carbon and oxygen isotopic measurements were made in the Environmental Isotope Geochemistry Laboratory of the Institute of Geology and Geophysics,Chinese Academy of Science.About 150μg was reacted with phosphoric acid at 72°C for 6h using a GasBench II (Thermo-Finnigan).The

CO 2produced was analyzed for carbon and oxygen isotope ratios using a MAT-253isotope ratio mass spectrometer.The carbon and oxygen isotope measurements have a precision better than 0.1‰.Accuracy and precision were routinely checked by running the carbonate standard NBS-19after every six measurements of the samples.Carbon isotope ratios are reported relative to Peedee belemnite (V-PDB),and oxy-gen isotope ratios are reported relative to standard mean ocean water (V-SMOW).

Rb –Sr analyses were performed at the Laboratory for Radiogenic Isotope Geochemistry (LRIG),Institute of Geology and Geophysics,Chinese Academy of Sciences (Li et al.2006).Sphalerite grains in Teflon?vessels,washed ultrasonically in analysis-grade alcohol and millipore water,were dissolved using 0.3ml 3N HNO 3and 0.1ml HF at 120°C.Rb and Sr were separated using ion exchange col-umns.Rb and Sr concentrations were measured by isotope dilution,and a mixed 87Rb/84Sr spike solution was used.Isotopic ratios of Rb and Sr were measured on an IsoProbe-T mass spectrometer at the LRIG.Correction of mass frac-tionation for Sr isotopic ratios was based on an 88Sr/86Sr value of 8.37521.Repeated measurements of NBS987Sr standard solution gave an average value of 87Sr/86Sr ratio of 0.710250±31(2σ).

One quartz syenite porphyry sample in the Lengshuikeng District (Fig.2)was selected for U –Pb zircon dating by laser ablation multi-collector inductively coupled plasma mass spectrometry (LA –(MC)–ICP –MS)at the Tianjin Institute of Geology and Mineral Resources,Tianjin,China (Li et al.2009).The zircon was ablated with a NUP193-FX ArF Excimer laser using a spot diameter of 35μm,with constant 13–14J/cm 2energy density and a frequency of 8–10Hz.The ablated material was carried in He into the plasma source of a GVI.All measurements were made in static mode,using Faraday cups for 238U,232Th,208Pb,206Pb,207Pb,and an ion-counting channel for 204Pb.A common Pb correction is achieved by using the measured 204Pb and assuming an initial Pb composition from Stacey and Kramers (1975).

Analytical results Sulfur isotope data

The δ34S values determined from 20sulfide samples collected in this study and δ34S data from previous works in the same area (Meng et al.2007;Xu et al.2001;No 912Geological Surveying Team (NGST)1997)are listed in Table 1and plotted in Fig.7.The δ34S values of sulfides in ores range from ?3.8to 6.9‰with an average of 2.0‰.However,the majority of sulfide minerals have δ34S values between ?1

and

Fig.5Mineral paragenesis of the porphyry-hosted and stratabound ores in the Lengshuikeng ore district showing mineral assemblages

4‰.The ranges of δ34S values of sulfides in the porphyry-hosted and stratabound ores from ?3.8to 6.9‰(average 2.3‰)and ?2.4to 4.9‰(average 1.7‰),respectively.The δ34S values of pyrite in the porphyry-hosted ores in pyrite –chalcopyrite –sphalerite (stage 1)range from 2.2to 4.9‰(average 3.9‰).However,the δ34S values of pyrite,sphaler-ite,and galena in the porphyry-hosted ores in silver minerals –

galena –sphalerite (stage 2)range from ?0.4to 3.1‰(average 2.0‰),0.9to 4.3‰(average 2.8‰),and ?2.4to 2.8‰(average ?0.4‰),respectively.The δ34S values of pyrite,sphalerite,and galena in the stratabound ores in pyrite –chal-copyrite –sphalerite (stage 1)range from 2.3to 4.0‰(average 3.3‰),3.5to 6.9‰(average 5.0‰),and 3.2‰,respectively.However,the δ34S values of pyrite,sphalerite,and galena

in

Fig.6Photomicrographs

showing the salient mineralogical and textural aspects.a Pyrite disseminated in porphyry-hosted ore and replacing K-feldspar crystals.b Granite porphyry fragments cemented by sulfide minerals with brecciated vein structure and pyrite breccias intersected by galena and sphalerite vein (Su 2013).c Chalcopyrite,galena,and

sphalerite in rhyolitic crystal tuff,with chloritization and

sericitization.d Galena with “crumpled ”texture and galena and sphalerite intersected by quartz vein.e Dolomite replaced by sphalerite and sphalerite surrounded by galena.f

Aggregate of acanthite in the intergranular pores of ferromanganese carbonate (Lu et al.2012).g Subhedral native silver occurring in the intergranular pores of ferromanganese carbonate

(Lu et al.2012).h Native silver vein in ferromanganese carbonate (Lu et al.2012).Aca acanthite,Cpy chalcopyrite,Dol dolomite,Fer ferromanganese carbonate,Gn galena,Ksp K-feldspar,Py pyrite,Qz quartz,Slv native silver,and Sp sphalerite

the stratabound ores in silver minerals–galena–sphalerite (stage2)range from2.3to2.8‰(average2.5‰),0.9to 3.8‰(average2.2‰),and?3.8to2.4‰(average0.1‰), respectively.

Carbon and oxygen isotope data

The carbon and oxygen isotope values of carbonate minerals were determined for nine hydrothermal siderite samples col-lected from the stratabound ores and crystal tuffs with weak alteration,two calcite vein samples,five ankerite vein sam-ples,and eight manganese–iron carbonate samples(rhodo-chrosite and siderite)from the volcano-sedimentary strata. Carbon and oxygen isotopic compositions are listed in Table2and plotted in Fig.8.

Theδ13C PDB values in rhodochrosite and siderite samples from the volcano-sedimentary strata vary from?7.0to?2.4‰(Table2).Theδ13C PDB values of hydrothermal carbonates in siderite,calcite,and ankerite samples vary from?7.2to ?2.2‰,from?3.3to?1.5‰,and from?3.9to?2.0‰,

Table1Sulfur isotopic compositions of sulfide minerals from the Lengshuikeng Ag–Pb–Zn ore district

Sample no.Mineral Stageδ34S(‰)Sample no.Mineral Stageδ34S(‰)Sample no.Mineral Stageδ34S(‰)

Stratabound ores Stratabound ores Porphyry-hosted ores

ZK504Py1 3.7PD152-4Gn2 1.1ZK10412-1b Py2 1.9

Zk13Py1 4.0ZK136-1Gn2?1.4L14c Py2 2.0

ZK410-2Py1 3.0LSK-74a Gn2 1.8L15c Py2 1.7

No12Py1 2.3N4-8-102b Gn20.1L16c Py2 2.4

ZK515Py1 3.2S4-0-28b Gn20.2L26c Py2 1.5 LSK-9a Py1 3.5LSK-101a Gn2 2.0126-2-1a Py2?0.4 LSK-9-1a Py1 3.6LSK-102a Gn2 2.4130N-4a Sp2 4.3 LSK-41a Py1 2.7So-8-11b Gn2?1.7130S-1a Sp2 2.9 LSK-42a Py1 3.6N4-8-77b Gn2?0.1L17c Sp2 3.2

ZK136-1Sp1 4.3N4-8-13b Gn2 1.1L18c Sp2 2.9

PD160-6Sp1 5.8N4-8-96b Gn2?0.9L19c Sp2 2.6

PD80-10Sp1 5.1N8-4-20b Gn20.2L20c Sp2 1.9

Zk197Sp1 3.5So-12-23b Gn2?3.8LSK-77a Sp2 4.6

No7Sp1 5.2N4-8-102b Py2 2.7LSK-78a Sp2 3.6

PD152-4Sp1 4.6N8-8-26b Py2 2.3L27c Sp2 1.5

ZK515Sp1 6.9So-8-11b Py2 2.3L28c Sp20.9 LSK-101a Sp1 4.6Porphyry-hosted ores130N-4a Gn2 1.2

PD80-13Sp1 5.0L1c Py1 4.9130S-1a Gn20.1 LSK-74a Sp1 4.8L2c Py1 4.9LSK-77a Gn2 1.6

ZK515Gn1 3.2L3c Py1 4.1L21c Gn2 2.8

N4-8-77b Py1 3.0L4c Py1 4.1L22c Gn2?0.3

N8-0-150b Py1 4.0L5c Py1 3.6L23c Gn2?0.9

ZK136-1Py2 2.8L6c Py1 3.6L24c Gn2?1.7

So-8-11b Sp2 2.3L7c Py1 2.2L25c Gn2?2.3

N4-8-77b Sp2 2.8L8c Py2 3.1L29c Gn2?0.1

N4-8-102b Sp2 1.0L9c Py2 3.0L30c Gn2?0.2 LSK-102a Sp2 3.8L10c Py2 2.6L31c Gn2?0.4

So-12-23b Sp20.9L11c Py2 2.5L32c Gn2?0.9

N4-8-77b Gn2?0.8L12c Py2 2.3L33c Gn2?1.1

Zk29Gn2 1.6L13c Py2 2.3L34c Gn2?1.2

Zk311Gn2?0.1ZK10010-718b Py2 2.3L35c Gn2?2.4

Zk198-1Gn20.2ZK10010-719b Py2 1.4

Sp sphalerite,Gn galena,Py pyrite

a Meng et al.(2007)

b Xu et al.(2001)

c NGST(1997)

isotopic composition of sulfide

minerals in the Lengshuikeng ore

district.a All sulfide minerals.b

Sulfide minerals in porphyry-

hosted ore.c Sulfide minerals in

stratabound ore

Table2Carbon and oxygen isotopic compositions of carbonate minerals from the Lengshuikeng Ag–Pb–Zn ore district.Theδ18O SMOW values were calculated fromδ18O PDB values using the formula:δ18O SMOW=1.03091×δ18O+30.91(González and Lohmann1985)

Sampling location Sample no.Lithology Mineralδ13C PDBδ18O SMOW ～152m elev.PD152-3Manganese–iron carbonate Rhodochrosite?3.311.6

～160m elev.160-4Manganese–iron carbonate Rhodochrosite?2.418.0

～120m elev.PD120-9Manganese–iron carbonate Siderite?3.914.6

～152m elev.PD152-11Manganese–iron carbonate Siderite?5.313.0 13703drill hole Zk315Manganese–iron carbonate Siderite?2.716.8 15150drill hole Zk18Manganese–iron carbonate Siderite?5.914.9

～152m elev.PD152-10Manganese–iron carbonate Siderite?5.513.4 13704drill hole Zk198-1Manganese–iron carbonate Siderite?7.019.5

～160m elev.160-3Crystal tuff Hydrothermal siderite?2.217.9 13213drill hole ZK513-1Crystal tuff Hydrothermal siderite?3.917.5 15150drill hole Zk32Crystal tuff Hydrothermal siderite?4.213.5

～120m elev.PD120-5Crystal tuff Hydrothermal siderite?5.917.5

～160m elev.160-6Stratabound ore Hydrothermal siderite?3.816.8

～120m elev.No5Stratabound ore Hydrothermal siderite?5.413.6

～120m elev.PD120-6Stratabound ore Hydrothermal siderite?5.913.5

～152m elev.PD152-4Stratabound ore Hydrothermal siderite?3.613.7 13213drill hole ZK509Stratabound ore Hydrothermal siderite?7.212.8 15150drill hole Zk33Ankerite vein Ankerite?3.313.1 15150drill hole Zk34Ankerite vein Ankerite?2.013.5 15151drill hole ZK136Ankerite vein Ankerite?3.313.9 15151drill hole Zk138-2Ankerite vein Ankerite?3.911.0 13703drill hole Zk309Ankerite vein Ankerite?3.012.4 15151drill hole ZK138-3Calcite vein Calcite?1.510.9 13703drill hole Zk313Calcite vein Calcite?3.311.9 Surface a83Carboniferous Limestone0.619.6

a NGST(1997)

respectively (Table 2).The δ18O SMOW values in rhodochrosite and siderite samples from the volcano-sedimentary strata vary from 11.6to 19.5‰and from 10.9to 11.9‰,respectively (Table 2).The δ18O SMOW values of hydrothermal carbonates in siderite,calcite,and ankerite samples vary from 12.9to 17.9‰,from 10.9to 11.9‰,and from 11.0to 13.9‰.One Carboniferous limestone sample is isotopically heavy (19.6‰;NGST 1997).

Rubidium and strontium isotope data

The Rb –Sr analytical data of sphalerite are given in Table 3.The sphalerite was separated from the manganese –iron car-bonate ores in the silver minerals –galena –sphalerite stage.Data regression for isochron ages and weighted mean values were performed using the ISOPLOT software (Ludwig 2001),with 2%error for 87Rb/86Sr ratios and 0.05%error for 87

Sr/86Sr at the 95%confidence level.The analytical data for sphalerite yielded an age of 126.9±7.1Ma (Fig.9)with an initial 87Rb/86Sr ratio of 0.71490(mean square weighted deviation (MSWD)=0.94).

Zircon U –Pb geochronology

Measured 206Pb/238U ages from individual zircons are shown in Fig.10,and the analytical results of LA –ICP –MS U –Pb dating are listed in Table 4.For the quartz syenite porphyry (sample T10),analyses from 20spots cluster close to the concordia,yielding a weighted mean 206Pb/238U age of 136.31±0.81Ma (2σ,MSWD=1.3;Fig.10).

Discussion

Ages of magmatism and mineralization

The results presented in this study together with those from previous investigations suggest multistage magmatism in the Lengshuikeng and adjacent regions.The magmatic activity took place principally during three periods,in the Jurassic,earlier Early Cretaceous,and later Early Cretaceous.

The Jurassic magmatism in the Lengshuikeng District is represented by the emplacement age of the granite

porphyry,

Fig.8Plots of calculated δ18O SMOW versus δ13C PDB from various samples in the Lengshuikeng ore district.Carbonate fields are from previous studies.The data are from four different materials including marine carbonate (Baker and Fallick 1989;Hoefs 1997),continental carbonate (Hoefs 1997),sedimentary organic matter carbon (Hodson 1977;Hoefs 1997),and magma-mantle carbonate (Taylor et al.1967;Valley 1986;Ray et al.1999).This plot offers information about various processes of CO 2and carbonate ions including meteoric water influence,

sea water penetration,sediment contamination,and high temperature influence,low temperature alteration (Deines 1989;Demrny and Harangi 1996;Demeny et al.1998;Hoernle et al.2002),decarboxylation and oxidation (Hofmann and Bernasconi 1998),decarbonate and carbon-ate dissolution (Lorrain et al.2003),crystallization differentiation with no significantly influence on the oxygen,and carbon isotopic composition (Santos and Clayton 1995;Bindeman 2008)

Table 3Rb –Sr isotopic

compositions of sphalerite in the Lengshuikeng Ag –Pb –Zn ore district

Sample no.Mineral Rb (μg/g)Sr (μg/g)87

Rb/86Sr

87

Sr/86Sr(±2σ)

I sr PD152-7Sphalerite 1.390 4.0800.98910.716557±340.71435ZK205Sphalerite 0.0960.9720.28660.715641±380.71500ZK513-1Sphalerite 2.060 1.820 3.27260.720846±220.71354No4

Sphalerite

0.960

3.960

0.70190.716056±18

0.71449

from the whole-rock Rb –Sr age of 159Ma (Meng et al.2007),LA –ICP –MS U –Pb zircon age of 154.3±3.0Ma to 163.6±2.1(Qiu et al.2013)and 155.1±0.97Ma (Wang et al.2013b ),and SHRIMP zircon U –Pb age of 162.0±2Ma (Zuo et al.2010).Previous studies reported the ages of the Daguding Formation volcanic rocks in the Lengshuikeng District,such as LA –ICP –MS zircon U –Pb ages of 161.0±1.0Ma for the rhyolite tuff (Wang et al.2013b )and 160.8±1.9Ma for the ignimbrite (Qiu et al.2013),and a SHRIMP zircon U –Pb age of 157.6±3.2Ma for the tuff (Di et al.2013).These age data coincide with the major magmatic event that took place during ca.164–154Ma in SE China as documented in other studies (Peng et al.2006;Yuan et al.2008;Li et al.2008).

The Early Cretaceous zircon U –Pb age of 136.3±0.8Ma obtained for the quartz syenite porphyry likely represents the crystallization age of the magma.Ages for the E ’huling Formation volcanic rocks in the Lengshuikeng District in previous studies include the LA –ICP –MS zircon U –Pb ages of 144±1Ma for the tuff,140±1for the rhyolite,137±1Ma for the rhyolite tuff,and 129±1Ma for the tuffite (Su 2013).

The second phase of Early Cretaceous magmatism in the Lengshuikeng District is represented by rhyolite porphyry,alkali-feldspar granite porphyry,and mafic dykes.The rhyo-lite porphyry and alkali-feldspar granite porphyry yielded ages of 110and 109.6Ma,respectively,based on whole rock K –Ar dating (JBGMED 1982;NGST 2003).

Dating of hydrothermal mineral deposits is often difficult to achieve,although the ages are critical for understanding the relationship between the timing of mineralization and other geological events.Rb –Sr dating of sphalerite has been suc-cessfully used to directly determine the age of sulfide miner-alization and to constrain models of large-scale migration of mineralizing fluids (e.g.,Brannon et al.1992;Nakai et al.1990,1993;Christensen and Halliday 1995;Christensen et al.1995;Walshaw and Menuge 1998;Yin et al.2009).Although sphalerite appears to yield meaningful Rb –Sr ages,the site of Rb and Sr and the factors controlling Rb/Sr fractionation in sphalerite remain uncertain (Nakai et al.1990;Schneider et al.2008).A Rb –Sr age of 126.9±7.1Ma was obtained from stage 2sphalerite in the stratabound ore,which is similar to the age of the volcano-sedimentary rocks of the E ’huling Formation (129±1Ma;Su 2013).The sphalerite residues display no correlation between 1/Sr and 87Sr /86Sr (Table 3),suggesting that the sphalerite Rb –Sr isochron age is not a pseudoisochron and has actual geological significance (e.g.,Nakai et al.1993).Chen (2011)has reported the mineralogical characteristics of sphalerite of the stratabound ore in the Lengshuikeng District,indicating no clay minerals in sphal-erite.Therefore,this age is interpreted to reflect the timing of the Pb –Zn mineralization.Available geochronological data for the Lengshuikeng District are summarized in Fig.11.The K –Ar ages of 138Ma for sericite in porphyry-hosted ore (JBGMED 1982;NGST 2003)and sphalerite Rb –Sr age of 127Ma in stratabound ore suggest that the hydrothermal alteration and mineralization do not overlap with any of the Jurassic magmatic ages.The ages for mineralization do,how-ever,overlap with the ages for the first phase of Early Cretaceous magmatism (ca.144to 129Ma;Su 2013).These relationships suggest that stage 2is not genetically related to the Jurassic magmatism,although it is still possible that heat from cooling intrusions associated with the formation of the E ’huling Formation (ca.144to 129Ma;Su 2013)drove the hydrothermal system.

Sources of metals and ore-forming fluids

The δ18O H2O values of ore fluids were calculated using the quartz –water equilibrium fractionation of Clayton et al.(1972)using the final homogenization temperatures of prima-ry fluid inclusions.The fluids of stage 1quartz had a δ18O H2O value of about +5.3‰(Zuo et al.2009;Lu 2012),

slightly

Fig.9Rb –Sr isochron of sphalerites from the Lengshuikeng Ag –Pb –Zn ore

district

Fig.10Zircon U –Pb concordia plots and calculated weighted mean 206

Pb/238U ages for sample T13quartz syenite porphyry from the Lengshuikeng ore district.Data are from Table 4

lower than the values of the primary magmatic water (δ18O H2O =+5.5to +9.0‰;Taylor 1974).As the δ18O H2O values in stage 1are close to the range of primary magmatic waters,a contribution of magmatic water cannot be ruled out during this stage.The δ18O H2O values of the stage 2fluids range from +1.2to +4.5‰(average=+4.0‰),whereas the δD values range from ?78to ?63‰,with an average of ?70‰(Zuo et al.2009;Lu 2012).Compared to the stage 1fluids,the stage 2fluids clearly shift toward the composition of meteoric water.The δ18O H2O values of stage 3quartz are between ?3.1and +4.4‰(average ?0.6‰;Zuo et al.2009;Lu 2012),indicating that the fluids were dominated by meteoric water.The δD values in stage 3fluids have a narrow range from ?84to ?53‰(Zuo et al.2009;Lu 2012),which are close to that of Mesozoic meteoric water in Jiangxi Province,east-central China (?60‰;Zhang 1989).

The range of δ34S values for sulfides in the Lengshuikeng ore district is close to the range (mainly ?3to 3‰)of δ34S values for magmatic sources (Ohmoto and Rye 1979;Wang et al.2014a ).The δ34S values of sulfides in the porphyry-hosted and stratabound ores are similar,which support a common hydrothermal fluid forming both ore types (Fig.7).In some samples,pyrite has high δ34S,suggesting that part of the sulfur was derived from the regional Precambrian base-ment rocks (δ34S average value of 5.5‰)through dissolution and leaching,similar to the scenario reported from the Jinshan deposit,Jiangxi Province (Zeng et al.2002).The δ34S values in Lengshuikeng permit the inference that the sulfur was derived mainly from magmatic sources,with minor contribu-tions of heavy sulfur from the country rocks.

The Lengshuikeng hydrothermal carbonates are character-ized by a wide variation of δ18O SMOW from 10.9to 17.9‰.

Table 4LA –ICP –MS zircon U –Pb analytical data for the quartz syenite porphyry in the Lengshuikeng ore district Spot number Content (ppm)

Ratios

Age (Ma)

Pb U

207

Pb/206Pb 1σ207

Pb/235U 1σ

206

Pb/238U 1σ

208

Pb/232Th 1σ

232

Th/238U 1σ

206

Pb/238U 1σ

T10.1124980.02130.00010.14080.00500.04780.00170.00580.00010.890.01581361T10.282790.02160.00020.14690.00880.04920.00290.00600.0001 1.500.03201381T10.4793,1600.02200.00010.15100.00180.04970.00060.00590.00000.990.01091401T10.5461,9680.02160.00010.14730.00220.04940.00070.00680.00010.610.00581381T10.6712,9300.02130.00010.14330.00180.04870.00060.00610.00000.890.00801361T10.793900.02110.00020.14450.00740.04960.00250.00600.00010.810.00831351T10.10321,3360.02250.00010.15350.00230.04940.00070.00690.00000.600.00511441T10.11261,1100.02140.00010.13940.00250.04730.00080.00720.00010.580.00501361T10.12481,9540.02220.00010.16180.00220.05280.00070.00620.00000.840.00741421T10.14612,3490.02240.00010.14610.00200.04740.00060.00620.0000 1.000.00891431T10.18

40

1,606

0.0213

0.0001

0.1403

0.0021

0.0479

0.0007

0.0052

0.0000

1.22

0.0105

136

1

Fig.11Summary of

geochronological data for the Lengshuikeng District.All data noted in the text

The wide variation of the oxygen isotope composition of the Lengshuikeng carbonates are considered to be related to wa-ter–rock interaction combined with the temperature depen-dence on mineral-fluid oxygen isotope fractionation(Santos and Clayton1995;Biondi and Santos2013).Theδ18O SMOW versusδ13C PDB plot illustrates the various processes affecting CO2and carbonate ions in the Lengshuikeng District(Fig.8). Except for the Carboniferous limestone sample,all the other samples from the Lengshuikeng District plot within or near the fields of continental carbonates(Fig.8).As the homoge-nization temperatures of fluid inclusions in dolomites from primary ores are relatively low(from150to270°C;Lu2012), the variation of carbon and oxygen isotopic composition of the Lengshuikeng hydrothermal carbonates are similar with those of the manganese–iron carbonate sedimentary country rocks.This feature indicates that the carbonate from the Lengshuikeng is dissolved from the local car-bonate country rocks.

Evolution of the Lengshuikeng District

Since the Middle Jurassic,possibly from170to155Ma,the paleo-Pacific plate subducted underneath the SCB generating I-type magmas(Wang et al.2013b)along the NE-trending compressive faults and thrust nappe structures,especially in the Lengshuikeng ore district(Jahn et al.1976;Chen1999; Jiang et al.2011).However,the paleo-Pacific plate did not subduct successively toward to the northwest but instead slab rollback occurred at the beginning of Late Jurassic,possibly lasting until Early Cretaceous.This was followed by the formation of an intra-arc rift along the Shihang-Hang zone. Injection of anomalously high-temperature magma into the crustal regions may have induced partial melting of the crustal rocks,generating A-type magmas(Wang et al.2013b). Therefore,it is likely that the southern Hunan to northern Guangxi region is part of an intra-arc rift or back-arc exten-sional zone induced by the subduction of paleo-Pacific plate. Thus,the Lengshuikeng ore district is considered to be related to the tectonic transition regime from a shallow-dipping com-pressional stress regime to a steep-dipping extensional stress regime during the Early Cretaceous(Mao et al.2013).

The Lengshuikeng granite porphyry was emplaced along NNE-striking faults at shallow depths,and subsequent hydro-thermal fluid activity led to strata-and fracture-controlled Pb, Zn,and Ag mineralization.The stratabound Ag–Pb–Zn ore bodies are associated with stratabound fractures,whereas the porphyry-hosted Ag–Pb–Zn ore bodies are associated with NNE-striking F2reverse faults.The Lengshuikeng ores are similar to the structurally controlled epithermal deposits such as the Swayaerdun gold deposit in the southwestern Chinese Tianshan metallogenic belt(Chen et al.2012a).Some of the features of the Lengshuikeng Ag–Pb–Zn deposits are similar to epithermal deposits,such as those in the Cerro de Pasco and Colquijirca carbonate replacement epithermal deposits, Peru(Bendezúet al.2003,2007;Baumgartner and Fontboté2008;Baumgartner et al.2009),carbonate replacement epithermal deposits in the Kamariza ore district,Lavrion,Greece(Voudouris et al.2008),and other epithermal deposits(Thiersch et al.1997;Aramburu 2008;Tassinari et al.2008;Duuring et al.2009a,b;Chen et al.2012b).

The average Au/Ag ratios of pyrite–chalcopyrite(early-stage)and silver minerals–galena–sphalerite(middle-stage) assemblages in the porphyry-hosted ores are0.02and 0.0008,respectively(Meng et al.2007).The Au/Ag average ratios of pyrite–chalcopyrite–sphalerite(early-stage)and silver minerals–galena–sphalerite(middle-stage)assem-blages in the stratabound ores are0.001and0.0004, respectively(Meng et al.2007).The low Au/Ag ratios in ores in Lengshuikeng Ag–Pb–Zn deposits are similar to those of epithermal deposits,such as the range from 0.0001to1in the Lake City II,Summitville,Red Mountain(USA),Julcani(Peru),Lepanto(Philippines), Kushikino and Hishikari(Japan),Ametistovoe and Balei (Russia)(Charoy and Gonzalez-Partida1984;Berger and Bonham1990;Izawa et al.1990;Nekrasova et al.1997; Pal'yanova2008).

Conclusions

The mineralization in the Lengshuikeng ore district is mainly fracture-controlled epithermal type of Ag–Pb–Zn deposits. The mineralization age of126.9±7.1Ma is close to that of the volcano-sedimentary rocks of the E’huling Formation,and therefore it is possible that heat from cooling magmas associ-ated with the formation of the E’huling Formation drove the hydrothermal system.Hydrogen,oxygen,and carbon isotope data from porphyry-hosted and stratabound ores at Lengshuikeng indicate that the ore-forming fluids were de-rived from meteoric water,whereas sulfur isotopes do not preclude the possibility that a magmatic fluid contribution also existed.

Acknowledgments This research is jointly supported by China Bureau of Geological Survey project(Nos.1212011085472,1212010533105, 1212010981048),Fundamental Research Funds for the Central Universities(No.2652013034),and the111Project(No.B07011).This study also contributes to the1000Talents Award to M.Santosh from the Chinese Government.We thank Emmanuel John M.Carranza(James Cook University,Australia)and Gregory A.Davis(University of Southern California,USA)for their valuable time,suggestions,and comments to improve the various versions of the manuscript.We thank Paul Duuring,University of Western Australia,Australia,and Huayong Chen,Guangzhou Institute of Geochemistry,CAS,China,for their crit-ical reviews and constructive comments.The authors also thank Drs. Georges Beaudoin,Patrick Williams,Rolf Romer,and Thomas Bissig for their great contributions to this paper.

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Qiu JT,Yu XQ,Wu GG,Liu JG,Xiao MZ(2013)Geochronology of igneous rocks and nappe structures in Lengshuikeng deposit,Jiangxi Province,China.Acta Petrol Sin29:812–826,in Chinese with English abstract

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学习活动2-5：性格测试(向性指数)

学习活动2-5 性格测验（1） 指导语：请你在回答下列问题时认真地加以完成，凭你的第一感觉选择最符合你实际情况的选项。对下列问题，若认为符合你的情况，请打“√”，若不符合请打“×”，若难以判断请打“△”： 1．你很介意细节吗？ 2．你能立即下决心吗？ 3．你能慎重地花时间去做一些实际的事情吗？ 4．你会事后改变决心吗？ 5．与思考相比，你更喜欢行动吗？ 6．你忧郁吗？ 7．你能从失败中吸取教训吗？ 8．你无忧无虑吗？ 9．你寡言少语吗？ 10．你感情外露吗？ 11．你经常欢笑吗？ 12．你情绪经常起伏不定吗？ 13．你对待事物专心致志吗？ 14．你有忍耐心吗？ 15．你喜欢讲理和追根究底吗？ 16．你议论时易激动吗？ 17．你十分谨慎小心吗？ 18．你动作麻利吗？ 19．你的工作表详尽吗？ 20．你喜欢令人注目、抛头露面的工作吗？ 21．你对工作有热情吗？ 22．你总是异想天开吗？ 23．你清高吗？ 24．你对身边的物品漫不关心吗？

25．你乱花钱吗？ 26．你喜欢发言吗？ 27．你挑剔吗？ 28．你爱开玩笑吗？ 29．你易被教唆吗？ 30．你固执倔强吗？ 31．你牢骚满腹吗？ 32．你很介意他人对自己的看法吗？ 33．你想得到他人的批评吗？ 34．你把自己的事情委托给别人吗？ 35．你不愿意被别人指挥、命令吗？ 36．你能管理好他人吗？ 37．你能直率地听进别人的意见吗？ 38．你机灵吗？ 39．你隐瞒什么吗？ 40．你能立即同情他人吗？ 41．你过于相信他人吗？ 42．你难以忘记仇恨吗？ 43．你腼腆、害羞吗？ 44．你喜欢独处吗？ 45．你愿意花精力去交朋友吗？ 46．你在众人面前能平静地讲话吗？ 47．你经常避开众人的焦点吗？ 48．你能轻松爽快地与意见不同的人交往吗？ 49．你好帮助别人吗？ 50．你毫不吝惜地把东西送给他人吗？ 每个问题画好“√”或“×”或“△”后，填入下面表格的“转记栏”中，然后与“对照栏”中的“√”或“×”对照。在“V标记栏”中把仅与“对照栏”中的“√”或“×”相同的画上“○”标记。

证据法简答题(很全面的)

证据制度与诉讼制度的关系。 答：(1)控诉式诉讼制度与神示证据制度的关系；（2）纠问式诉讼与法定证据制度关系；（3）混合式诉讼与自由心证的关系。 2．简述我国证据制度的基本原则及其要求。 答：我国证据制度所坚持的客观真实的原则，是证据制度的基本原则。这种客观真实的证据制度，要求重证据、重调查研究、不轻信口供，要求查明案件事实真相，以便正确地据实处理。我国的证据制度为充分确实的证据制度，案件对证据的具体要求，在质上就是要求确实可靠，在量上就是要求全面细致、充分，达到了两个方面的统一，案件的真实性就可以保证。 3．简述证据学的具体研究方法。 答：1）借鉴和创新的研究方法；2）定性和定量的分析研究方法；3）系统、全面研究的方法；4）比较研究方法；5）实证研究的方法。 4．简述证据内容与证据形式的关系。 答：司法公正是核心，证据的内容和形式应为之服务。因此，在证据的内容与关系上应有的观点是：（1）坚持有真实内容的证据，原则上应使其有合法的证据形式，这有利于查明案件事实直相，从而保证案件正确处理。（2）重视对人权的保护，对于证据收集采用过程中的违法行为，一律依法严处；坚持按程序办案，坚持惩治违法行为，以实现诉讼程序公正。（3）对严重违法收集的证据，基于可靠性程序差，必须限制采用。 5．简述法定证据制度产生的历史条件。 答：法定证据制度是对神示证据制度的否定，是历史上一大进步。它的出现是人类文化科学的发展对司法经验总结的结果；同时又是和当时的政治斗争形势联系在一起的，是中央集权君主制的产物。为了结束地方封建割据的分裂状态，加强中央集权的统治，封建君主实行这项法律制度，有利于把司法权掌握在自己手中，从而打击封建割据势力。 6．简述自由心证证据制度产生的历史条件。 答：自由心证制度的形成有其特定的历史过程。为了与诉讼制度的变革相适应，1791年法国宪法会议正式废除法定证据制度，建立了自由心证制度。首先，资产阶级思想家崇尚人的理性的良心，指出“人生而自由”的观点。 7．简述自由心证理论的主要内容。 答：自由心证理论的主要内容有两点：一是法官的理论性和良心；二是心证达到确信的程度。两根支柱，一是抽象的理性；一是抽象的良心。其中心则是“自由”，即法官根据理性和良心自由地判断，在内心达到真诚确信的程度。自由心证制度的核心内容，就是对于各种证据的真伪、证明力的大小以及案件事实如何认定，法律并不作具体规定，完全听凭法官根据理性和良心的指示，自由地判断。 8．我国奴隶制度时期证据制度的特点。 答：奴隶制度的证据制度特点是：1）法官认定案件主要依据审判时间经验的总结；2）神示证据制度消失的较早。我国古代奴隶制各个王朝的证据制度，主要是根据审判实践经验形成的，比较重视与案情有拳客观材料，要求法官据证推断；3）除重视采用当事人的证词外，还重视其他证据的作用。 9．我国封建制度时期证据制度的特点。 答：封建制度时期证据特点是：1）坚持口供至上的原则，定罪必须取得被告人认罪的供词。2）审讯是可以依法刑讯。刑讯的程度，违法刑讯应否负刑事责任和负什么刑事责任，历代封建王朝的法律则有不同的规定。3）诬告者反坐，伪证者罚。4）疑罪惟轻兼从赎，实行有罪推定。5）重视勘验检查。6）据众证定罪的制度。7）集成和发展了“以五声听狱讼，求民情”的主观臆断的审判方法。 10．简述新中国证据制度发展的四个阶段。 答：第一阶段是从1931年至1949年的创建期，属于新民主主义时期，属于新民主主义时期。在革命根据地的法律中，已经建立起了先进的证据原则和制度。第二阶段是从1949年至1966年的发展期。中华人民共和国成立之后，人民政府在废除国民党伪法统和总结革命根据地司法工作经验的基础上建立了新

名词(可数名词和不可数名词)

专题一名词 主要考查三个方面： 1、联系上下文，考查同义词、近义词辨析； 2、可数名词的单复数、不可数名词、抽象名词、名词词 组的意义和用法； 3、名词的固定搭配和习惯用语。 ◆名词的数 规则名词的复数形式

可数名词复数形式的不规则变化

常见的不可数名词

不可数名词的量化 a block of一块； a bottle of一瓶 a group of一群； a pile of一堆 a pair of一组/双/对； a piece of一片/张/块既可作可数名词又可作不可数名词的词

【2016 广东】 The broken ______may cut into your hand if you touch it, you should be careful. A. glass B. glasses C. candle D. candles 【2016广西来宾】

—There are many ____ about this farm. —Yes, lots of ____ are planted on it. A. photo; potato B. photos; potatos C. photos; potatoes D. photoes; potatoes 1. Help yourself to some_______. There are lots of vitamins in them. A. tomato B. tomatoes C. tomatos D. potatos you take a plane, you cannot take ______ onto the plane with you. A. knife B. knifes C. knives D. a knives 3. The _______ have caught the two_______ already. A. policeman; thief B. policemen; thiefs C. policemen; thieves D. policeman; thieves 【2016重庆】It’s sports time. Most students in Class 1 are playing football on the playground. A. boy B. boys C. boy’s D. boys’ 【2015攀枝花】All the are from ． A. men doctors; Germany B. men doctors; German C. man doctors; Germany D. man doctor; German 【2015广安】 —How many can you see in the picture —Two． A. dog B. child C. sheeps D. sheep 【2015天河】

我的性格测试

不知道自己前面的路该怎么走，这是给自己列的一些计划，不知道自己是否可以走下去。 1.科班出生，电气自动化方面的发展，女生适合设计（CAD,protel,C语言学的比较好），营销（自动化相关产品的营销，销售助理其实是没有前途的职业），管理。 2凭证上岗，考取一些相应的证书，凭这些证书找到合适的工作。例如，会计证，报关报检证， 单证员等。 3去一些大型商场工作，混两年估计也是什么楼层主任，或是什么的啦。。（这个得牺牲自己的法定节假日）家人团聚的机会。 但是我自己的性格适合什么工作呢？ 回忆一下从小到大，哪些事情让自己有成就感？找出10个。 确定1，他是什么？ 2.为什么会让自己有成就感？ 3.我的感受是什么？ 4.它对我意味着什么? 归纳共性 对未来职业的了解，-------------方式，人物访谈。 1，这个职业具体是做什么的？ 2,对从业者有什么能力要求？时间安排，晋升途径，收入状况，

3，这个职业你喜欢它什么？ 4以我目前的状况来看，如果从事该职业，你有什么建议？ 把自己的特质与目标工作匹配起来， 确定哪些可以降， 哪些要坚持。。。 ESTJ 管家型——掌控当下，让各种事务有条不紊地进行 报告接收人: 才储成员677110 日期: 2012-09-07 一、你的MBTI图形

MBTI倾向示意图(类型：ESTJ 总倾向：45.9) 外向（E） （I）内向 实感（S） （N）直觉 思考（T） （F）情感 判断（J） （P）知觉 倾向示意图表示四个维度分别的倾向程度。从中间往两侧看，绿色指示条对应下面坐标的哪个区间。 本报告地址不会长期有效，请复制报告内容到本地或自己的博客。

证据法教学大纲

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可数名词和不可数名词

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性格倾向性测试题

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19．怒时，不加抑制。是（否） 20．为取得别人赞赏而改善工作。是（否） 21．喜欢兴奋而紧张的劳动。是（否） 22．常回想自己的过去。是（否） 23．愿意做群众运动的领袖。是（否） 24．喜欢公开演说。是（否） 25．使梦想变为事实。是（否） 26．很讲究写应酬信。是（否） 27．做事粗糙。是（否） 28．深思熟虑。是（否） 29．能将强烈的情绪（喜、怒）表现出来。是（否）30．不拘小节。是（否） 31．对人十分关心。是（否） 32．与观点不同的人和睦相处。是（否） 33．喜欢猜疑。是（否） 34．轻信人言，不假思索。是（否） 35．愿意谈书本道理，不愿做实际工作。是（否）36．读书不求甚解。是（否） 37．常写日记。是（否） 38．在人群活动中肃静无哗。是（否） 39．不得已而动作。是（否） 40．不愿回想自己的过去。是（否）

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(4) 在特殊疑问句中，用how many修饰可数名词 There are three pens on the desk. (对划线部分提问) →How many pens are there on the desk? 不可数名词 (一)定义：不能以数目计算，不可以分成个体的概念、状态、品质、感情或表示物质材料的 东西，如water, tea, bread等。它没有复数概念，它的前面不能用补丁冠词a/an. 表特指时可用定冠词the修饰。 ①Water is very important to life. 水对生命来说十分重要。 ②The bread on the table is Mark’s. 桌子上的面包师Mark的。 (二)特点 (1) 不可数名词前面可以有much, a little, a lot of等修饰词：much bread, a little tea (2) 不可数名词不能用数词修饰，需要借助单位词来表示数量： a piece of paper 一张纸，a piece of bread一片面包，a cup of tea一杯茶 (3) 不可数名词变复数：量词变复数形式，作主语时谓语动词用复数 two pieces of bread 两片面包，three cups of tea 三杯茶 (4) 对不可数名词的修饰词提问，疑问词用how much. There is some milk in the glass. (对划线部分提问) →How much milk is there in the glass? 练习： 一、根据句意及所给单词填空。 1. ________(this) are my English books. 2. My aunt Jane and my mother are ___________(sister). 3. I have two ___________(watch). They are on the desk. 4. I have some __________(photo) of my family. 5. Do you like these ____________(dictionary)? 6. Those are _________(bus). 7. I have lots of________(tomato) here. 8. The________(leaf) on the tree turn-yellow. 二、选择填空： 1. —Mom, I want___. ——Here you are. A. a bread B. a piece of bread C. some breads D.breads 2. The _____ has two ______. A. boys, watches B. boy, watch C. boy, watches D. boys, watch 3. There are lots of _____ in the basket on the table. A. tomatos B. tomato C. tomatoes D. tomatoss 4. —_____apples do we need to make fruit salad? —Let me think...We need three apples. A. How long B. How often C. How much D. How many 5. "Lily, Let's make vegetable salad. How many _____ do we need?" "One is enough." A. oranges B. potato C. tomatoes. 6. Would you like _____ to eat now? A. some B. anything C. something D. thing 7. I'm so hungry. Please give me _____ to eat.

证据法的概述

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（一）要考虑其政治经济背景 （二）要考虑文化传统的背景 （三）要考虑诉讼制度的背景 四、证据法学的科学体系和内容 当今世界有两个有关证据法科学体系和内容的代表性的著作。一个是由美国著名的证据法学家华尔兹教授所著的刑事证据大全。这本书主要是讲究适用，从应用的角度来安排证据法律体系。这本书的证据法学的体系共有十九章。 第一章，证据法的渊源。 第二章，审判程序和证据的种类 第三章，审判的记录，包括审判笔录的功能、内容和制作。特别是在法庭上对各种人证的调查、讯问的方法和规则。 第四章，关于证据的相关性 第五章，排除传闻证据的规则 第六章，排除传闻证据的例外 第七章，证人可靠性的质疑 第九章，用不恰当的方法所收集到的证据，特别是辨认证据的排除。 第十章，武力搜查，没有理由的搜查、扣押以及意思权证据的保护。 第十一章，供述证据 第十二章，面证权 第十三章，证明责任和特定的规则 第十四章，司法认知 第十五章，证人能力 第十六章，各种文字材料和文字证据