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Geology and Geochemistry of theDongping Gold Telluride Deposit, HeibeiProvince, North ChinaZhang Zhaoghong a & Mao Jingwen ba Institute of Geology , Chinese Academy of Geological Sciences, 26Baiwanzhuang Road, Beijing, 100037, People's Republic of Chinab Institute of Mineral Deposits , Chinese Academy of GeologicalSciences, 26 Baiwanzhuang Road, Beijing, 100037, People's Republicof ChinaPublished online: 06 Jul 2010.

To cite this article: Zhang Zhaoghong & Mao Jingwen (1995) Geology and Geochemistry of theDongping Gold Telluride Deposit, Heibei Province, North China, International Geology Review, 37:12,1094-1108, DOI: 10.1080/00206819509465441

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International Geology Review, Vol. 37, 1995, p. 1094-1108. Copyright © 1995 by V. H. Winston & Son, Inc. All rights reserved.

Geology and Geochemistry of the Dongping Gold Telluride Deposit, Heibei Province, North China

ZHANG ZHAOGHONG

Institute of Geology, Chinese Academy of Geological Sciences, 26 Baiwanzhuang Road, Beijing 100037, People's Republic of China

AND MAO JINGWEN

Institute of Mineral Deposits, Chinese Academy of Geological Sciences, 26 Baiwanzhuang Road, Beijing 100037, People's Republic of China

Abstract

The Dongping gold telluride deposit, located on the northern margin of the China-Korea platform, is one of the largest gold deposits in China. The deposit is spatially and temporally associated with the Shuiquangou complex (comprising calc-alkaline, weakly alkaline, and alkaline rocks) and genetically related to the weakly alkaline rocks.

The Dongping deposit is a system of quartz-filled fractures and K-feldspar-altered rocks. The ore veins consist mainly of quartz, K-feldspar with minor pyrite, tellurides, gold, sphalerite, chalcopyrite, galena, specularite, calcite, sericite, and barite. Mineralization in the deposit can be divided into five stages, with gold mineralization occurring in two major stages—in stage II as native gold (Au) in specularite-quartz veins, and in stage III as native gold and gold tellurides associated with base-metal sulfides and disseminated pyrite in altered K-feldspar rocks. The proportion of gold that is native is more than 90%. Pyrite is the most common sulfide mineral and can be recognized as three generations. All pyrites of the three generations have a cubic shape, which may suggest a low -forming environment.

Introduction

THE DONGPING GOLD TELLURIDE deposit, dis­covered in 1985, is located in Chongli County, northern Hebei Province, about 160 km north­west of Beijing. The exploration program for the No. 1 and No. 2 ore veins developed a reserve of 35 metric tons of gold and was conducted in 1986 by the No. 8 Party of the Police Gold Army; other veins now are being explored. At the time of its discovery and early exploration, Dongping proved to be a new type of deposit for China; subsequently, more than 10 gold deposits similar to the Dongping—especially the Hegou, Zhongshangou, and Huangtuliang— were discovered in the Shuiquangou complex, with gold reserves totalling about 100 metric tons. The Dongping gold deposit proper is char­acterized by enrichment in tellurides. With respect to its genesis, some researchers postu­lated a relationship to alkaline rocks and regarded Dongping as an alkaline-rock-related gold deposit (Bonham, 1984, 1988; Head et al., 1987). After summarizing a large amount of information reported from the gold telluride

and tellurium deposits of the world, Zhang and Li (1994) proposed that the Dongping deposit is related to a high-tellurium geochemical field and has no relationship to any special lithologic characteristic.

In this paper, we review the geology and geochemistry of the Dongping gold telluride deposit in detail. We present a discussion both of the ore-forming physico-chemical conditions and of the possible relationship between the alkaline rocks and the deposit.

Regional Geology The Dongping gold deposit is located in an

uplifted region of the basement, south of the Shangyi-Chongli-Chicheng deep fault, which marks the boundary between the Inner Mongolian axis and the Yanshanian subsidence belt. The regional stratigraphic sequence is an Archean amphibolite facies of metamorphic rocks of the Shanggan Group, overlain by Pro-terozoic marine sedimentary systems of the Changcheng and Jixian formations, and then

0020-6814/95/159/1094-15 $10.00 1094

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DONGPING GOLD TELLURIDE DEPOSIT, CHINA 1095

FIG. ] . Geological sketch map of the Shuiquangou complex and the distribution of gold deposits.

by Jurassic volcanic-sedimentary rocks. The Archean metamorphic rocks of the Shanggan Group are the country rocks of the ore-hosting Shuiquangou complex, and consist of gneiss, plagio-amphibolite, and granulite.

Three cycles of tectono-magmatic activities have been recorded—Archean-Proterozoic, Hercynian-Indonian and Yanshanian. Most intrusions are distributed along the southern side of the Shangyi-Chongli-Chicheng deep fault.

The Te contents of the Archean metamorphic rocks of the Shanggan Group vary from 0.5 ppm to 1.2 ppm, 500 to 1200 times the clarke (1 ppb) (Greenland, 1967). This implies that the inves­tigated area is a high-Te geochemical field. The Te contents of the Shuiquangou complex range from 0.1 to 0.7 ppm, averaging 0.265 ppm, which is 100 to 700 times the clarke.

The Shuiquangou Complex

The Shuiquangou complex outcrops across a subrectanglar 400-km2 area, striking approx­imately E-W (Fig. 1). The western and middle parts of the Shuiquangou complex formerly were covered by an Upper Jurassic sequence of volcanic-sedimentary rocks. The complex is intruded by several Yanshanian-age granite plu-tons (180 to 160 Ma) so it can be inferred that

the emplacement of the Shuiquangou complex occurred earlier than did the Yanshanian period. Radiometric K-Ar, Ar-Ar, and Rb-Sr isochron ages of the Shuiquangou complex have a wide spread, from 150 to 309 Ma. The youngest ages probably are the result of alteration.

On the basis of intrusive sequences, mineral paragenetic associations, and the characteris­tics of accessory minerals, Zhang (1995a, 1995b, 1995c) divided the Shuiquangou com­plex into four associations—a pyroxene diorite association, an amphibole-monzonite associa­tion, a syenite association, and an alkali-feldspar/syenite association. Each association consists of several types of rocks, although there are no clear boundaries between the dif­ferent associations. The main characteristics of the four associations are listed in Table 1.

There are many enclaves in the complex, especially in the contact zone between it and the surrounding country rocks. Almost all of the enclaves are xenoliths of the country rocks that now are rich in K-feldspar and poor in amphi-bole and biotite compared to the original rocks.

Zhang (1995a, 1995b, 1995c) used the Ritt-man Index (a) and the total alkali-silica dia­gram of Mutschler (1991) to separate the Shuiquangou complex into three series—a calc-alkaline, a weakly alkaline, and an alkaline series. Pyroxene diorite, quartz alkali-feldspar

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1096 ZHANG ZHAOCHONG AND MAO JING WEN

TABLE 1. Main Characteristics of the Four Associations of the Shuiquangou Complex

Association

Pyroxene diorite

Amphibole-monzonite

Syenite

Alkali-feldspar syenite

Types of rocks

Biotite-pyroxene, diorite, and monzodiorite

Amphibole-mon-zonite, pyroxene amphibole mon-zonite, amphibole monzonite, monzonite

Syenite, aegirine-augite syenite, alkali-feldspar syenite, quartz alkali-feldspar syenite

Syenite, alkali-feld­spar syenite, quartz alkali-feldspar sye­nite, alkali-feldspar granite

Mineralogy

Biotite, augite, andesine, oligoclase, apatite, magnetite

Perthite, microcline, oligoclase, amphibole, pyroxene, apatite, titanite, magnetite

Perthite, microcline, albite, oligoclase, aegirine, biotite, quartz, garnet, titanite zircon, magnetite

Perthite, microcline, albite, oligoclase, amphibole, quartz, garnet, titanite, zircon, allanite, bastnaesite, magnetite, ilmenite

Texture and structure

Subeuhedural grained texture; massive structure

Subeuhedral grained texture, perthitic texture; massive structure

Subeuhedral texture edulcora-tion border, poikilitic, perthitic, resorption texture; massive structure

Subeuhedral grained, hetero-granular, perthitic, poikilitic texture; massive structure

syenite, and alkali-feldspar granite belong to the calc-alkaline series; amphibole-monzonite, syenite, aegirine-augite syenite, and alkali-feldspar syenite belong to the weakly alkaline or to the alkaline series. Amphibole monzonite, syenite, and alkali-feldspar syenite are the host rocks for the gold deposits in this area. Based on the study of rare-earth elements (REE), trace elements, and stable isotopes, Zhang (1995a, 1995b, 1995c) suggested that the primitive magma was derived from a mixed source of crust and mantle.

Deposit Geology The Dongping gold deposit is located on the

southern side of the contact zone of the Shui­quangou complex (Fig. 2). The host rocks for gold mineralization in the deposit are mainly syenite and alkali-feldspar syenite. Many min­eralized veins have been discovered in the mine, but only five attain economic concentrations. These ore veins, developed in a group of en echelon, tensile-shear faults, vary from several hundred to more than one thousand meters in length. A single orebody is tens to more than 100 m in length, 0.24 to 5.10 m in width, and several to more than 400 m deep. The main ore

veins strike from 0 ° to 35° NE, and dip NW at 30° to 55° . Each ore vein consists of several gold orebodies. A single gold orebody generally includes the auriferous quartz vein and the K-feldspar-altered rocks around the vein, but some orebodies contain only K-feldspar-altered rocks. The boundaries between the country rocks and gold orebodies is obscure and can be determined only by chemical analysis.

The No. 1 vein, consisting of one main vein and several branch veins, is the largest in the Dongping gold deposit and has a reserve of 22.5 metric tons of gold. The main vein strikes NNE to N-S, and some of the branch veins strike NW. The shape of the No. 1 vein becomes more complex from the surface downward (Fig. 3). At shallow depths, the orebodies consist of auriferous vein quartz and the related K-feld­spar-altered rocks, and at deeper levels they contain auriferous vein quartz, branch veins, and K-feldspar-altered rocks. The shape of the No. 1 vein at depth is complex and feather-like. The No. 70 vein, which differs from the No. 1 ore vein in terms of the shape of the orebodies, contains discontinuous auriferous vein quartz. The orebodies usually contain K-feldspar-altered rocks over a width of about 10 meters.

Five hydrothermal stages can be recognized from mineral associations and crosscutting

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DONGPING GOLD TELLURIDE DEPOSIT, CHINA 1097

FIG. 2. Simplified geological map of the Dongping mine.

relationships: Stage I is white quartz-K-feld-spar-pyrite. The white quartz is coarse grained with a greasy luster; the K-feldspar is red and coarse grained and occurs along both sides of the quartz vein; and the pyrite is disseminated as euhedral crystals. The gold grade of Stage I is quite low.

Stage-II veins are intersected by the veins of Stage I, and consist of gold, specularite, and quartz; the specularite aggregates have a sheared or radial structure. Stage II is an impor­tant stage in gold mineralization. Native gold is about 1 mm in diameter and fills in fissures in quartz and specularite.

Stage III—a gold, polymetallic sulfide, and quartz stage—is the most important stage of gold mineralization. The quartz is grayish white, fine-grained, and semitransparent; pyrite occurs in veinlets and also in isolated masses; and telluride minerals, including cal-averite, tellurium, altaite, and tellurobis-muthite, are developed in Stage III. The most common telluride is calaverite. Some tellurides are associated with galena and some occur as fillings in fissures of quartz.

Stage IV consists of a gray chalcedony-like quartz and pyrite. The quartz is gray, dense, and chalcedonic on both sides of the main mineral­ization vein of Stage III. Its width ranges from 5 cm to 20 cm and yellow bands can frequently be seen in it. Most of the quartz veins of this stage are found deep within the No. 70 ore vein. The gold grade in this stage is low.

FIG. 3. The shape of the No. 1 gold body at different levels.

Stage V is a carbonate and barite stage. The carbonate-bante veins are fissure fillings and have irregular shapes, intersecting all the early quartz veins. However, they do not contain gold.

Mineralogy

Quartz and K-feldspar are the most abundant gangue minerals in the ores, with quartz occur­ring in all hydrothermal stages. Native gold occurs as grains as large as 2 mm in diameter and generally is accompanied by calaverite, pyrite, specularite, chalcopyrite, and galena. There are three gold settings—fissure fillings, gold enclosed in other minerals, and gold trapped in crystals. The ratio of these three occurrences is 43:21:36, respectively. Gold grains at shallow depths often are larger than those at deeper levels. The tellurides at shallow levels also are more abundant than those at depth, and the Te/(Au+Ag) ratio in the ores

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1098 ZHANG ZHAOCHONG AND MAO JING WEN

TABLE 2. Changes in Chemical Compositions in the Varied Alteration Zones

Major oxides

SiO2

TiO2

Al2O3 Fe2O FeO MnO MgO CaO Na2O K2O P 2 O 5 H2O

A

63.78 0.18

16.88 2.44 1.28 0.05 0.41 1.47 5.16 5.04 0.11 0.26

B

588 2

183 17 10 0.6

14 14 92 60

1 16

A

65.77 0.05

18.86 0.69 0.20 0.03 0.06 0.50 5.66 7.68 0.1 0.2

B

592 0.3

199 5 1.5 0.2 0.8 5

98.5 89 0.8

12

c

+ 4 - 1.7 +16 -12 - 8.5 - 0.4 -13.2 - 9 - 6.5 +29 - 0.2 - 4

A

70.75 0.05

15.36 0.59 0.11 0.02 0.02 0.07 1.77

10.73 0.1 0.26

B

632 0.3

161 4 0.8 0.1 0.3 0.6

30.5 122

0.8 15

C

+44 - 1.7 -22 -13 - 9.2 - 0.5 -13.7 -13.4 -61.5 +62 - 0.2 - 1

A

93.09 0.01 4.32 0.62 0.010 0.03 0.02 0.09 0.08 1.18 0.1 0.08

Quartz vein B

760 0

41 4 0.7 0.2 0.2 0.8 1.3

12.4 0.7 4

C

+172 - 2 -142 - 13 - 9.3 - 0.4 - 0.4 - 13.2 - 90.7 - 47.6 - 0 . 3 - 12

Abbreviations: A = wt%; B = atomic numbers of element in the standard rock cell; C - difference from the primary rock; (+) and (-) represent " in" and "out" repectively.

declines from the surface downward. Electron microprobe analyses indicate that the gold per­centage in native gold ranges from 93.4% to 97.3%.

Sulfides are the major metallic minerals in the ores, but their amount is generally less than 5% by volume. Pyrite is the most abundant sulfide. Chemical analysis of pyrite indicates that the Te content ranges from 21 to 1100 ppm, with an average of 408 ppm.

Wall-Rock Alteration

The most important feature of wall-rock alteration in the Dongping gold deposit is an intense K-feldspathization, which occurs widely in the form of a distinctive red rock. Besides feldspathization, silica, pyrite, sericite, albite, carbonate, and barite alterations occur. The K-feldspathization and pyrite and silica alterations are closely associated with gold mineralization.

K-feldspathization can be divided into three stages. In the first, K-feldspar is coarse-grained and is accompanied by gold mineralization; this coarse-grained alteration is developed exten­sively in the mine. The second stage is bronze-colored and occurs along both sides of the quartz veins. Second-stage alteration actually forms an ore, because it contains 3.29 g/t of gold on average. The third stage consists of a reddish-pink and medium fine-grained feldspar that occurs outside of the second-stage K-feld­

spathization. The third stage alteration also has produced an ore, in which the gold grade can reach up to 49 g/t. The second and third stages generally extend 2 to 3 m and sometimes up to 10 m outside the vein.

Changes in major elements in the alteration zones are presented in Table 2 and Figure 4. The following conclusions can be derived from Fig­ure 4:

(1) There is an increase of SiO 2 from the primary rocks through a weak alteration zone, an intense alteration zone, and then the quartz vein. This implies that S iO 2 was introduced into the country rocks from the hydrothermal ore-forming fluid.

(2) Al and Na change in parallel, increas­ing in the weak alteration zone and decreas­ing in the intense alteration zone; this implies that the changes can be related to the formation of albite:

CaAl2Si2O8 + 4SiO 2 + 2Na+ = 2NaAlSi3O8 + Ca2+. (1)

(3) Fe3+, Fe2+, Ca2+, and Mg2+ decrease in the various alteration zones, especially in the weakly altered zone, indicating that these ions were probably removed from the pri­mary rocks and that they supplied the mate­rial base for the later formation of pyrite and carbonate minerals.

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DONGPING GOLD TELLURIDE DEPOSIT, CHINA 1099

FIG. 4. Changes in chemical compositions of various alteration zones. Legend: 1 - syenite; 2 - weak K-feldspathization zone; 3 = intense K-feldspathization zone; 4 = quartz vein.

Fluid-Inclusion Studies Fluid inclusions were observed in the quartz

of the quartz veins, calcite of the calcite-barite vein, sphalerite, and K-feldspar. Thirteen repre­sentative quartz samples and one calcite sample were chosen for measurement of homogeniza-tion temperatures. The shapes of inclusions varied from irregular, ellipsoidal, and spindle­like to polygonal; some inclusions even had negative crystal shapes. The inclusions ranged from 5 to 15 µm in diameter.

The inclusions can be classified into four types (or assemblages), based on the number and volume proportions of phases present:

(1) Liquid inclusions, consisting almost entirely of a liquid phase, are rare in the Dongping deposit.

(2) Vapor inclusions, with vapor phase ratios from 60% to 85%, occur mainly in the early metallogenic veins.

(3) Two-phase inclusions (aqueous solu­tions and vapor) are the most common type, with phase ratios ranging from 10% to 25%.

(4) Liquid CO2 inclusions commonly occur in groups.

Homogenization temperatures (Th) of the primary fluid inclusions in the Dongping deposit range from 120° to 350° C (there are no pressure corrections for the Th values). Th

values of the quartz-K-feldspar-pyrite stage range from 315° to 350° C; thegold-polymetal sulfides-quartz stages range from 240 ° to 285 ° C; and the late carbonate-barite stage ranges from 120° to 185° C. The Th values of the other stages have not been measured, because their inclusions are too small.

Only large and clearly visible two-phase inclusions were used to determine fluid com­positions, and in most cases heating runs were made immediately after freezing. The tempera­ture of melting of the last crystals of ice have been converted to equivalent wt% NaCl using the equations provided in Potter et al. (1978). The salinities range from 1.5 to 10.0 equiv. wt% NaCl, averaging 5.33 equiv. wt% NaCl. There is

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1100 ZHANG ZHAOCHONG AND MAO JINGWEN

TABLE 3. Compositions of the Liquid and Vapor Phase of the Fluid Inclusions in the Investigated Area

Mines

Dong-ping

Zhong-shangou

Xiashang lai

Zhaojia-gou

Hegou

Jingia-zhuang1

Description

Stage I, quartz

Stage II, quartz

Stage III, quartz

stage IV

Polymetallic sulfides—quartz

Polymetallic sulfides—quartz

Polymetallic sulfides—quartz

Polymetallic sulfides—quartz

Polymetallic sulfides—quartz

Polymetallic sulfides—quartz

Polymetallic sulfides—quartz

Unit

µg/g mol%

µg/g mol%

µg/g mol%

µg/g mol%

µg/g mol%

µg/g mol%

µg/g mol%

µg/g mol%

µg/g mol%

µg/g mol%

µg/g mol%

K+

1.01 3.99

0.90 5.39

1.23 5.34

3.36 6.22

0.75 4.19

2.75 7.10

1.75

11.54

2.51 12.05

1.82 5.35

0.25 1.56

0.75 4.28

Na+

1.69 11.20

6.33 64.40

6.67 49.13

10.76 48.08

0.77 7.28

4.38 19.00

1.46

16.15

3.46 28.25

5.28 26.17

0.12 1.30

1.89 18.47

___ Liquid phase ______

Ca2+

5.53 21.17

0.00 0.00

0.00 0.00

0.00 0.00

2.89 15.89

5.92 14.80

3.97 25.38

1.58 7.53

2.14 6.14

1.48 9.61

1.70 9.68

Mg2+

1.88 11.96

0.03 0.23

0.00 0.00

0.06 0.26

3.12 28.70

0.31 1.30

0.31 3.23

0.62 4.90

1.01 4.78

0.25 1.56

0.39 3.60

1.29 1.99

3.08 7.49

4.11 7.25

6.52 6.98

1.86 4.19

1.50 1.60

0.57 1.54

1.29 2.45

5.41 6.37

12.22 32.99

18.84 44.14

F-

1.75 14.88

0.17 2.11

0.28 2.64

0.22 1.25

1.44 17.66

5.75 31.90

1.38 19.24

1.13 11.86

0.57 3.64

1.90 27.53

0.33 2.70

Cl-

8.06 34.82

3.08 20.37

7.47 35.64

12.85 37.21

3.56 22.08

8.62 24.30

3.10 22.31

6.21 32.96

14.84 47.55

3.49 25.45

2.71 17.12

CO2

22.39 1.03

1.87 1.71

1.09 2.88

1.77 3.77

7.46 0.50

63.44 1.88

2.87 0.35

35.45 1.38

25.58 3.77

48.58 2.17

102.43 5.10

CH4

0.36 0.05

0.00 0.00

0.00 0.00

0.17 0.97

0.47 0.09

0.06 0.01

0.04 0.02

0.08 0.01

0.18 0.07

1.06 0.13

0.05 0.01

______Vapor phase CO

0.00 0.000

0.02 0.08

0.05 0.17

0.33 1.10

0.00 0.00

0.00 0.00

0.00 0.00

0.00 0.00

0.00 0.00

4.74 0.13

0.51 0.04

H2

0.12 0.12

0.00 0.00

0.00 0.00

0.00 0.00

0.11 0.16

0.17 0.11

0.10 0.27

0.10 0.01

0.01 0.03

0.64 0.63

0.06 0.07

______

O2

0.00 0.00

0.00 0.00

0.00 0.00

0.00 0.00

0.00 0.00

0.00

0.00

0.00 0.00

0.00 0.00

0.00 0.00

0.00 0.00

0.00 0.00

N2

0.00 0.00

0.01 0.00

0.01 0.05

0.05 0.17

0.00 0.00

0.00 0.00

0.00 0.00

0.00 0.00

2.34 0.55

0.00 0.00

3.40 0.03

H2O

883 98.81

43.80 98.20

17.57 96.73

17.99 93.99

607 99.25

1352 98.00

334 99.37

1035 98.52

265 95.58

886.01 96.74

779.25 94.77

1Data from the Jingjiazhuang deposit are from Peng et al. (1992); other data, except for Dongping, are from Wang et al. (1994).

no apparent variation in salinity with time or depth.

The CO2 concentration has been used to estimate the pressure during deposition. Pres­sures range from 500 to 690 bars. The depth of mineralization can be inferred to range from 1.67 to 2.30 km from the surface at a rate of pressure increase of 250 to 300 bar per kilometer.

The compositions of liquid- and vapor-phase fluid inclusions in the Dongping gold deposit are presented in Table 3. Compositions of other gold deposits in this area also are listed for comparison. K+ and Na+ are the major positive ions in all the gold deposits of the area, and Mg2+

and Ca2+ are minor. Cl- is the dominant negative ion in the Dongping and the other gold telluride deposits in this area, whereas instead of Ch is the dominant negative ion in the Jing-

FIG. 5. S-isotope compositions of the Dongping gold

deposit.

jiazhuang sulfide-rich gold deposit, where tel-lurides are not present.

Based on the compositions of the fluids (Table 3), some physico-chemical parameters of the Dongping gold deposit can be calculated: pH = 6.08-7.49; Eh = 0.58-0.86; 10 - 3 2-103 0 5 . The values calculated from the

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DONGPING GOLD TELLURIDE DEPOSIT, CHINA 1101

TABLE 4. Lead-Isotope Compositions of the Shuiquangou Complex, Archean Metamorphic Rocks, and Galenas from Dongping

No.

1 2 3 4 5 6 7 8 9 10 11 12 13 14 15 16

Lithology

Amphibole monzonite Aegirine-augite syenite Alkali-feldspar syenite Amphibole monzonite

Syenite Syenite

Plagioamphibolite Feldspar in plagioamphibolite

Feldspar in migmatite Galena Galena Galena Galena Galena Galena Galena

206Pb/204Pb

16.4565 17.3904 17.3541 17.231 17.379 17.362 14.48 14.32 14.30 17.5492 17.4545 17.6299 17.5744 17.55 17.45 17.6924

207Pb/204Pb

15.2701 15.4723 15.3199 15.3226 15.297 15.324 14.79 14.81 14.94 15.5109 15.4426 15.5526 15.5052 15.51 15.44 15.5552

208Pb/204Pb

36.5329 37.3901 37.0841 37.1771 37.389 37.132 34.3314 34.0925 36.1972 37.6320 37.415 37.7699 37.5446 37.63 37.42 37.7912

expression of Bortnikov et al. (1988) range from 10-8.50 to 10-5.43.

Stable-Isotope Studies The S- and Pb-isotope compositions of min­

erals have been studied and reported on in detail elsewhere (Jiang et al., 1992; Song, 1991; Song and Gou, 1992), and only a brief summary of the results is provided here. The δ34S values of pyrites and galenas range from -4.2 to -16.3 per mil (Fig. 5). This is similar to the values of -4.2 to -15.3 per mil from the Emperor mine (Ahmad et al., 1987). The δ34S∑S value, calcu­lated from the model of Ohmoto (1972), is approximately zero, suggesting that S was derived from a deep source during the hydro-thermal events.

The Pb-isotope compositions of galenas from the Dongping deposit, the Shuiquangou com­plex, and the Archean metamorphic rocks of the Shanggan Group are listed in Table 4. There is a close overlap between the Pb-isotope com­positions of galena and the Shuiquangou com­plex, but no overlap between those of galena and the Archean metamorphic rocks of the Shanggan Group. The projected points of the galenas (Fig. 6) are located between the two lead lines of the mantle and the orogenic zone pro­posed by Zartman and Doe (1981). These pro­jected points suggest two mixing sources for Pb.

The H- and O-isotope compositions in both minerals and fluid inclusions are listed in Table 5. The values in quartz were calculated from the fractional equation of quartz-H2O by Zhang (1989), 1000 2.01, and those in calcite from the fraction equation of calcite-water by Field (1985) —

There are many granite-aplite dikes in the Dongping mine, believed to be the last products of the magma that shares the same source as the Shuiquangou complex. Their H- and O-isotope compositions may represent those of the pri­mary magma water. The δD values of inclusions in quartz range from -74 to -101.3; the δ18O values for inclusions in quartz of Stage I fall within the range of 3.57 to 3.70 per mil. The δ18O values of Stages III and IV range from 0.60 to 1.75 per mil and from -0.56 to -0.26 per mil, respectively; and the δ18O value of the carbon-ate-barite stage is -13.20 per mil. Therefore, the δ18O values for inclusions gradually decrease from the magma stage (granite-aplite) to the late hydrothermal stage (carbonate-barite). This implies that meteoric water emerged dur­ing the process of mineralization in the Dong­ping area. Compared with the δ18O values of the primary rocks, the δ18O values of the altered rocks are lower—7.0 per mil in the weakly altered rock and 3.9 per mil in the intensely altered rock (δ18O values in primary rocks are

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1102 ZHANG ZHAOCHONG AND MAO JINGWEN

FIG. 6. Lead-isotope compositions of galena from the Dongpingand the Shuiquangou complex plotted on the lead structural model of Zartmanand Doe (1981). The filled circles represent the galena from the Dongpingand the open circles represent the Shuiquangou complex.

TABLE 5. H- and O-Isotope Compositions of the Dongping Deposit

No.

1 2 3 4 5 6 7 8 9 10 11

Mineral

Quartz Quartz Quartz Quartz Quartz Quartz Quartz Quartz Calcite

Description

Granite-aplite Stage I Stage I

Stage III Stage III Stage III Stage IV Stage IV

Carbonate-barite vein Weakly altered rock

Intensely altered rock

T(°C)

450 330 280 270 245 240 200 210 180

δ18O (‰,)

11.8 10.1 11.75 9.1

10.49 11.60 11.50 11.20 0.2 7.0 3.9

δD

- 74

- 91.2

- 89.3 - 81

-101.3 - 97

8.19 3.70 3.57 0.60 0.88 1.75

- 0.56 - 0.26 -13.20

- 74

- 91.2

- 89.3 - 81

-101.3 - 97

about 7.5 per mil)—a result of the effects of meteoric water.

The δ18O and δD values for mine ore fluids and granite-aplites are plotted in Figure 7. It is apparent that the fluid inclusions, except for the carbonate-barite state, fall within the two lines of magmatic water and meteoric water (the calculated positions for the two lines are shown in Fig. 7). This reflects the H- and 0-isotope compositions of the fluid-inclusion water, except that the carbonate-barite stage cannot result from a single type of original water (magmatic or meteoric), but rather results from a mixture of the two. The H- and O-isotope compositions of the inclusions in the quartz of granite-aplite dikes falls in the mag-matic-water range. The fluid inclusions of the carbonate-barite stage plot on the developed

line of meteoric water. This implies that the water of the final hydrothermal stage consists of meteoric water (e.g., Craig, 1961).

Thermodynamic Analyses of Formation of Tellurides

For tellurides, ideal Te2 gas is adopted as the most appropriate reference state, because Te2 is the most abundant species over geologically significant ranges in temperature (Afifi et al., 1988a, 1988b). The stability of metal tellurides with respect to their corresponding native ele­ments and sulfides is a function in part of the fugacity of tellurium in the system.

The formation of some common tellurides is bounded by the following reactions:

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FIG. 7.δ18O vs δD diagram of the Dongping mine. The left and right curved lines represent the developed lines of meteoric water and magmatic water, respectively. The calculated conditions for the two developed lines from the equation of mass equilibrium at 250° C and various ratios of W / R are as follows; the initial δ18O and δD values of rocks are 7.5 per mil and -100 per mil, respectively, and the initial δ18O and δD values of magmatic water are 8.10 per mil and -75 per mil, respectively. The initial δ18O and δD values of meteoric water are -15.8 per mil and -101 per mil, respectively, and the rocks contain about 1% water. Abbreviations: MWL = meteoric water line (Craig, 1961); SMOW = standard mean ocean water; MW = magmatic water; MMW = metamorphic water.

Au + Te2(gas) = AgTe2, (2)

4Ag + Te2(gas)=2Ag2Te, (3)

2PbS + Te2(gas)=2PbTe + S2(gas), (4)

(5)

For the general reaction, we use the well-known relationship:

(6)

Thus, we can hold the relationship between and temperature at a constant from free-

energy data. This enables us to establish the temperature diagrams of Figure 8, which indi­cate that low temperature favors the formation of all tellurides at constant It can be used to explain the presence of most tellurides in epithermal deposits.

If the temperature is constant, we can estab­lish the diagram in Figure 9. For AuTe2, we convert eq. (6) at the constant temperature:

Because C is constant, does not change upon a change of However, most of the tellurides coexisting with corresponding metal sulfides are controlled not only by temperature, but also by (see eq. (4)).

For reaction (4), we can convert eq. (6) to derive the following expression:

For all tellurides with the corresponding metal sulfides, their expression will be:

(7)

Eq. (7) indicates that the tellurides with the corresponding metal sulfides show inclined lines as various slopes on the diagram (Fig. 9). The formation of calaverite is con­trolled by the fugacity of Te2 at constant tem­perature. The formation of the tellurides with

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1104 ZHANG ZHAOCHONG AND MAO JING WEN

FIG. 8. temperature diagram showing the location of some telluride reactions at constant buffers: Legend: 1 = gold-calaverite; 2 = galena-altaite, = magnetite-pyrite-hematite.

the corresponding sulfides is controlled by the ratio of at constant temperature. A low

favors the formation of tellurides at the same It can be used to explain why most gold

telluride deposits contain minor sulfides. The compositions of fluid inclusions indicate

that Cl- is the major negative ion. The gold may have been carried as a chloride complex, such as AuCl2 or AuCl4 (Seward, 1984; Hayashi and Ohmoto, 1991). Thus, the process of gold mobility can be expressed as:

(8)

(9)

The equilibrium constants of reactions (8) and (9) are determined by the following expressions:

then

(10)

(11)

and the total Au contents are carried as gold chloride complexes:

(12)

Eq. (12) indicates that the total dissolved Au content is a function of Cl- concentration, pH, and temperature, whereas K is a function of temperature. That means that high Cl- con­centration, high temperature, high and low pH favor mobility. The magmas of the Shui-quangou complex, containing high Cl- con­tents, were formed under high (Zhang, 1995a, 1995b, 1995c). The primary fluid

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DONGPING GOLD TELLURIDE DEPOSIT, CHINA 1105

FIG. 9. The stabilities of some sulfides and tellurides as a function of the fugacities in the Dongpingand two other ore deposits. Legend: 1 = Dongping; 2 = Emperor gold mine, Fiji; 3 = Boulder County, Colorado. Abbreviations: Bn = bornite; Cp = chalcopyrite; Po = pyrrhotite; Py = pyrite.

derived from the magmas, perhaps inheriting these features, has a high capacity for leaching gold from the wall rocks.

The Te contents in the pyrite of the Dongping deposit are quite high. It can be inferred that the Te may exist mainly in the sulfides. When the sulfides are dissolved in an acid solution, the Te in the rocks may be released:

Fe(S, Te)2 + 4H+ = Fe2+ + H2S + H2Te. (13)

Reaction (13) indicates that an acid environ­ment favors Te mobility. When the temperature decreases, Au-chloride complexes are replaced by Au-sulfur complexes, such as Au(HS)-

2and AuHS. However, the fugacity of sulfur in the fluid is very low, so that part of the gold may have been carried as an Au tellurium complex, such as Au (HTe)-

2 because of the geochemical similarity between sulfur and tellurium.

Discussion and Conclusion

The Dongping gold telluride deposit is hosted by weakly alkaline rocks and is relatively rich in tellurides. Some researchers have classified the deposit as an Au-Te or alkaline type (Bonham,

1984, 1988; Cox and Bagby, 1986; Head et al., 1987). Other examples of this type may include Mount Kare and Porgera, Papua New Guinea (Richards et al., 1991; Richards and Kerrich, 1993; Richards and Ledlie, 1993); Emperor, Fiji (Anderson and Eaton, 1990); Tongyoung, Korea; Golden Sunlight, Zortman-Landusky, and Gies, Montana; and Cripple Creek (Thompson et al., 1985) and the telluride deposits of Boulder County, Colorado. The most distinctive features of these deposits are their association with alkalic intrusive complexes and the occurrence of Au-Ag tellurides, roscoelite, and fluorite. Some investigators have proposed a direct infusion of metals and other components into the hydrothermal sys­tem via magmatic fluids (e.g., Ahmad et al., 1987), whereas others have preferred to believe that remobilization from earlier stages of mag­matic hydrothermal mineralization was respon­sible (Moyle et al., 1990; Richards and Kerrick, 1993; Richards and Ledlie, 1993). Compared with the gold deposits mentioned above, the Dongping gold deposit is lacking in roscoelite and fluorite. Many gold telluride deposits in China are not spatially and temporally related to alkaline rocks; examples include the Xiaoyin-

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1106 ZHANG ZHAOCHONG AND MAO JING WEN

pan gold deposit hosted in the metamorphic rocks of the Shanggan Group and the gold telluride deposits in the Xionger-Xiaoqinling region (Ren et al., 1993). However, such Au-Te deposits share some common features: similar crystal forms of pyrite (mainly {100}), high percentage of gold in the form of native gold (more than 90%), relatively low sulfide con­tents in ores (generally less than 5 vol%), and high Cl- concentration in the fluid. These fea­tures suggest similar ore-forming processes among Au-Te deposits.

The pyrites of all gold telluride deposits in this area, including those hosted in the Shui-quangou complex and Archean metamorphic rocks, have similar crystal forms—cube {100} with very minor representation of other crystal forms—whereas the crystal forms of pyrites of the sulfide-rich gold deposits, such as the Zhangquanzhuang and Jinjiazhuang, are {100}+{210}. The crystal form of pyrite can indicate the mineralization circumstances (Cheng et al., 1987): {100} is indicative of conditions of low S2 fugacity and high tempera­ture gradients; {210} forms under conditions of intermediate temperatures, low temperature gradient, and high S2 fugacity; and {111} forms under conditions of low temperature, slight alkalinity, hypabyssal fluids, and high As con­tents. All of this implies that the pyrites of the Dongping and other gold telluride deposits hosted in the Shuiquangou complex were formed under conditions of low and high temperature gradients. The low in the fluid resulted in a high ratio, which would favor the formation of tellurides.

The ratio of native gold in total gold is high in the Dongping mine. Such a high ratio also is present in the other gold telluride deposits in China, such as Lishui (Jiangsu), Shanggong, and Beilin (Henen). This phenomenon can be explained by the following equation of Bortnikov et al. (1988):

(14)

where NAg is the atomic percentage of silver in the Au-Ag solid solution and T is the tempera­ture in degrees Kelvin. Eq. (14) is valid at temperatures above 478.15K. Under conditions of constant temperature, if we exert the deriva­

tive on both sides of eq. (14) we can conclude that:

(15)

From eq. (15) we can conclude that log decreases with the NAg ; that is, is positively correlated with the gold percentage of native gold. Therefore, the percentage of native gold in the gold telluride deposits with high is high.

Cl- is the major negative ion in the mineral­ization fluid in the Dongping gold telluride deposit. It has been reported that Cl- also is the dominant negative ion in many other gold tellu­ride deposits, e.g., Emperor, Fiji (Ahmad et al., 1987); Porgera, Papua New Guinea (Richards and Kerrich, 1993); Lishui, Jiangshu province (Wang et al., 1985); and Shanggong, Henai province (Ren et al., 1993). The high Cl- and low concentration in the fluid may indi­cate a low a high concentration in the fluid would favor gold mobility. There is one factor connecting all Au-Te types of deposit in China, including the Dongping: they are located in high-Te geochemical fields. The S- and Pb-iso-tope compositions of Dongping indicate that S and Pb components originated from a mixed source of magma and metamorphic rocks. Therefore, the high Te content of the Shui­quangou complex and Archean metamorphic rocks is a base for the formation of Te-rich hydrothermal solutions. The mobility of greater amounts of tellurium from the source became another factor leading to the increase of Thermodynamic analyses indicate that a low pH value favors Te mobility from the source; phys­ico-chemical conditions favoring gold mobility include a low pH, high temperature, high and high Cl- concentration. The early hydro-thermal fluids evolved from magmas of the Shuiquangou complex may provide beneficial conditions for mobility of Au and Te. Thermo­dynamic analyses also indicate the existence of beneficial physico-chemical conditions for the precipitation of tellurides: relatively low tem­perature, high and a high ratio. The tellurides of the Dongping deposit were formed at the medium-late stage of hydrothermal activity, when the temperature decreased to about 250°C. The high percentage of gold in native gold indicates a high whereas a low

leads to a high ratio. Therefore, a

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DONGPING GOLD TELLURIDE DEPOSIT, CHINA 1107

favorable environment exists for the precipita­tion of tellurides in the Dongping deposit.

For other gold telluride deposits not hosted in an alkaline complex, such as the Xiaoyinpan gold telluride deposit, common features indi­cate that they also have favorable conditions for Te mobility and for the precipitation of tel­lurides. However, many gold deposits that formed in high-Te geochemical fields, but in which tellurides are absent, may have had unfavorable conditions for Te mobility or for the precipitation of tellurides: these include the Zhangquanzhuang and the Jingjiazhuang gold deposits, which are in the same geochemical field as the Dongping deposit, but have values that are too high. However, the presence of some gold deposits hosted in the alkaline complex, but lacking tellurides, indicates that the existence of an alkaline complex is not a unique condition for the formation of tellu­rides. The discussion above indicates that the three necessary conditions for the formation of tellurides are: (1) a high-Te geochemical field; (2) favorable physico-chemical conditions for Te mobility (low temperature); and (3) favor­able physico-chemical conditions for the pre­cipitation of telluride (low temperature, high

and a high The alkaline magmas of the Shuiquangou

complex contributed to the formation of the Dongping gold telluride deposit in several ways. They: (1) provided the heat source; (2) supplied a portion of the ore-forming fluids (water, vol­atile components, and Cl -); (3) served as the source of Au and Te (remobilization from the consolidated Shuiquangou complex leached by the convecting fluid); and (4) provided favor­able conditions for Au and Te mobility.

The study of many Au-Te deposits implies that, for the most part, alkaline magmas play similar roles in Au-Te mineralization (Mut-schler et al., 1985; Porter and Ripley, 1985; Saunders and May, 1986; Anderson and Eaton, 1990; Moyle et al., 1990; Richards et al., 1991; Russell, 1991; Richards and Kerrich, 1993; Richards and Ledlie, 1993). These similarities can be useful in explaining the affinity of many gold telluride deposits with alkaline rocks.

Acknowledgments

This paper represents part of a Ph.D. thesis completed by Z. C. Zhang in the Graduate

School of the Chinese Academy of Geological Sciences. We thank the management of the Dongping Gold Mine for logistical support for field work at the Dongping deposit.

Professor Z. N. Li is acknowledged for help­ful advice and guidance extended to the first author (Z. C. Z.). Fluid-inclusion and stable-isotope analyses were conducted at the Institute of Mineral Deposits, Chinese Acad­emy of Geological Sciences (CAGS), and chemi­cal analysis was performed in the Institute of Rock and Mineral Analyses, CAGS.

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