Polymetallic mineralization

The deposits are characterized by conspicuous metal zoning and polymetallic mineralization. From the centre to margin of the mine district, the following zonings are recognized Sn-W-Bi-Cu zone, Cu-As-Zn zone, and Zn-Pb-Cu-As zone (Nakamura, 1970). 

Ishiyama, T., Matsueda, H. and Nakamura, T. (1987) Polymetallic mineralizations in the Jokoku-Katsuraoka mining area, southern Hokkaido. Mining GeoL, 37, 1-14. 

Ohta, E. (1991) Polymetalic mineralization at the Toyoha mine, Hokkaido, Japan. Mining Geology, 41, 279-295. 

Six sulphide species were observed in the non-ferromagnetic heavy mineral concentrates (NFM-HMCs) of bedrock samples arsenopyrite pyrite > chalcopyrite > bismuthinite = molybdenite = cobaltite. Chalcopyrite, pyrite and bismuthinite do survive in near-surface till but only in minor amounts (<8 grains/sample). Although the Co-rich composition of arsenopyrite is possibly the strongest vector to Au-rich polymetallic mineralization in the study area, sandsized arsenopyrite is absent in C-horizon tills, suggesting that arsenopyrite more readily oxidizes than chalcopyrite and pyrite in till, and therefore is an impractical indicator mineral to detect mineralization using surficial sediments at NICO. 

Bowman, J.R. 1998. Stable-isotope systematics of skarn. In Lentz, D.R. (ed.) Mineralized intrusion-related skarn systems, 99-145. Mineralalogical Association of Canada Short Course 26. Choi, S. 1983. Skarn evolution and iron-tungsten mineralization and the associated polymetallic mineralization at the Ulsan mine, Republic of Korea. Unpublished PhD. Dissertation, Waseda University, 271 p. Choi, S., So, C., Youm, S. Kim, M. 1999. Stable isotopeand fluid inclusion studies of iron-tungsten mineralization at Ulsan skarn deposit (Abstract). Economic and Environmental Geology, 32, 148-9. 

The aim of this contribution is study the metals distribution, and specifically the indium distribution into the polymetallic mineralization stages from the Pinguino deposit sulfide veins. 

The polymetallic veins are poorly exposed at surface and are characterized by the presence of gossans with remnants of breccias with quartz matrix and oxidized sulfide clasts. Hypogene polymetallic mineralization is characterized by the presence of massive and banded sulfide veins and sulfide breccias up to 13 m thick. This mineralization is developed In... 

Yang, X-M, Lentz, D.R., McCutcheon, S.R. 2003. Petrochemical evolution of subvolcanic granitoid intrusions within the late Devonian Mount Pleasant Caldera, southwestern New Brunswick, Canada comparison of Au versus Sn-W-Mo-polymetallic mineralization systems. Atlantic Geology, 39, 97-121. 

Ore deposits associated with volcanic rocks generally exhibit polymetallic (Cu, Pb, Zn, Sn, W, Au, Ag, Mo, Bi, Sb, As and In) mineralization. Sulfur isotopic values of sulfides from these deposits are close to 0%o, suggesting a deep-seated origin of the sulfide sulfur. Clay deposits (pyrophyllite, sericite and kaolinite) are associated with both felsic volcanic rocks and ilmenite-series granitic rocks of late Cretaceous age in the San-yo Belt. 

During the Miocene age, polymetallic vein-type (xenothermal-type, subvolcanic-type) and gold-quartz vein-type (mesothermal-hypothermal-type) mineralizations occurred mainly in middle to western part of Japan. They are described in section 1.6.1. In section 1.6.2, Hg and Sb vein-type deposits are described. 

Hirabayashi (1907) defined Kuroko as an ore which is a fine compact mixture of sphalerite, galena, and barite. This definition can be applied to black ore , but not to yellow ore or siliceous ore because these minerals are not abundant in these ores. Kinoshita (1944) defined Kuroko deposit as a deposit genetically related to the Tertiary volcanic rocks, consisting of a combination of Kuroko (black ore), Oko (yellow ore), Keiko (siliceous ore), and/or Sekkoko (gypsum ore) (Matsukuma and Horikoshi, 1970). The deposit is generally defined as a strata-bound polymetallic sulfide-sulfate deposit genetically related to Miocene bimodal (felsic-basaltic) volcanism (T. Sato, 1974). 

The Fe "/Zn + ratio of coexisting stannoidite, sphalerite and tennantite-tetrahe-drite from the Tada, Omodani and Ohmidani deposits is low, compared with that from the other deposits such as the Ashio, Akenobe and Ikuno deposits (Fig. 1.182). The Tada, Omodani and Ohmidani deposits are characterized by polymetallic (Zn-Cu-Ag-Au Zn-dominated) mineralization, and tungsten is not recovered from these deposits. On the other hand, the Akenobe, Ikuno and Ashio deposits are characterized by polymetallic (Cu-An-Pb-Sn-W-Ag-Au-Bi) mineralization, and tungsten is recovered from these deposits. 

Nakamura, T. (1970) Mineral zoning and characteristic minerals in the polymetallic veins of the Ashio copper mine. In Tatsumi, T. (ed.), Volcanism and Ore Genesis. Tokyo U. Tokyo Press, pp. 231-246. 

During the middle Miocene, Kuroko deposits, polymetallic vein-type deposits, gold-quartz vein-type deposits and Sb and Hg vein-type deposits were formed (see sections 1.3 and 1.6). Many vein-type deposits were formed not only in and nearby the Japanese Islands, but also at middle Miocene in northwest USA (Basin and Range Lipman, 1982), and elsewhere in the circum-Pacific regions (e.g., Peru). It is probable that large amounts of CO2 effused into the atmosphere from hydrothermal solution associated with this widespread mineralization and volcanic gas from subduction zones, causing an increase in temperature. 

These deposits are characterized by polymetallic (Cu, Pb, Zn, Au, Ag, etc.) mineralization and formation in extensional stress fields. Ore fluids responsible for these ore deposits are dominated by seawater origin, considering isotopic and chemical composition of ore fluids. 

Fortune Minerals Ltd. 2008. Annual Report. Goad, R.E., Mumin, A.H., Duke, N.A., Neale, K.L., Mulligan, D.L. Camier, W.J. 2000. The NICO and Sue-Dianne Proterozoic, Iron Oxide-hosted, Polymetallic Deposits, Northwest Territories Application of the Olympic Dam Model in Exploration. Exploration and Mining Geology, 9 (2), 123-140. 

This type contains a variety of ores, including(a) gold-pyrite ores, (b) gold-copper ores, (c) gold-polymetallic ores and (d) gold oxide ore, usually upper zone of sulphide zones. The pyrite content of the ore varies from 3% to 90%. Other common waste minerals are quartz, aluminosilicates, dolomite etc. 

Some metals are irreversibly adsorbed, probably via incorporation into the mineral phases, such as amorphous iron oxyhydroxides, as shown in Figure 11.6d. Some of these amorphous phases form by direct precipitation from seawater. As noted earlier, hydrothermal fluids are an important source of iron and manganese, both of which subsequently precipitate from seawater to form colloidal and particulate oxyhydroxides. Other metals tend to coprecipitate with the iron and manganese, creating a polymetallic oxyhydroxide. It is not clear the degree to which biological processes mediate the formation of such precipitates. Since the metals are incorporated into a mineral phase, this type of scavenging is better referred to as an absorption process. 

In this chapter, we consider the mineral composition of the hydrogenous minerals and how they fitrm. The evaporite minerals have already been covered in Chapter 17. The hydrothermal minerals (polymetallic sulfides) are discussed further in Chapter 19. 

Some of the discharged sulfide particles settle onto the chimney s exterior, where they are buried by the outward growth of anhydrite. Sulfide precipitation within the chimneys, causes copper, zinc, and iron sulfides to deposit and partially replace the anhydrite. Chimneys can build to several meters in height and their orifices range in diameter from 1 to 30 cm. Both the smoke and the chimneys are composed of polymetallic sulfide minerals, chiefly pyrrhotite (FeS), pyrite (FeS2), chalcopyrite (CuFeS2), and sphalerite or wurtzite (ZnS). 

Fig. 3. Mineralization linked to the ring structures I - Urkuveem (Mo with Ag and Bi, greisen type), II -Keyukveem (polymetallic), III - Kitivelgin (Au, arsenic-antimony association), IV - Belaya Sopka (Sn, cassiterite-sulfide association), V - Shestakovka (Sn with Ag and Bi, cassiterite-silicate association). Total productivities Pj, m %) for more promising catchment areas (outlined) and/or linear and ring structures are numbered.

Indium concentrations in the polymetallic veins show a wide range (3.4 to 1184ppm In, Table 1). Based on the correlation coefficients of ore geochemistry, significant Indium (up to 1184 ppm) is related to the Ps2 mineralization stage and closely associated with Fe-rich sphalerite, but also with ferrokesterite. There are important In anomalies in Psi (up to 159.4 ppm) that are related to the Sn minerals, cassiterite, ferrokesterite and stannite (Crespi 2006). 

The rocks at Morila record an intimate interplay between magmatism, contact metamorphism (and metasomatism), deformation, and mineralization. The spatial, temporal, and textural associations between contaminated post-D2 intrusions, contact metamorphism, and polymetallic post-D2 mineralization strongly suggests an intrusion-related origin for Morila. Other controls on Au mineralization include ... 

The granitic rocks of the NPSG are the youngest granitic rocks in the Long Lake area and are associated with several styles of mineralization an early base metal (Zn, Cu, Pb) and granophile element (Mo, Sn, W, In) polymetallic vein system is associated with the emplacement of the NPSG (Fyffe Pronk 1985), and later uranium vein mineralization, that resulted from... 

The Mount Pleasant Mine Property is located in Charlotte County, southwestern New Brunswick, Canada. The mineralization is divided into two main groups consisting of porphyry-type tungsten-molybdenum deposits, and vein and replacement-type tin polymetallic bodies. The deposits at Mount Pleasant are described in some detail in Kooiman et al. (1986) and Sinclair et al. (2006). Their petrogenetic character is discussed in Yang et al. (2003), Inverno Hutchinson (2006) and Sinclair et al. (2007). 

Novak and Valcha (1964) in drusy cavities of hydrothermal polymetallic veins as the latest mineral, Hora Svate Katering in the Krusne Hory Mountains, Czechoslovakia. 

The rest of the chapter is organized as follows. In Section 6.07.2 we discuss the chemical composition of hydrothermal fluids, why they are important, what factors control their compositions, and how these compositions vary, both in space, from one location to another, and in time. Next (Section 6.07.3) we identify that the fluxes established thus far represent gross fluxes into and out of the ocean crust associated with high-temperature venting. We then examine the other source and sink terms associated with hydrothermal circulation, including alteration of the oceanic crust, formation of hydrothermal mineral deposits, interactions/uptake within hydrothermal plumes and settling into deep-sea sediments. Each of these fates for hydrothermal material is then considered in more detail. Section 6.07.4 provides a detailed discussion of near-vent deposits, including the formation of polymetallic sulfides and... 

Mexico, the leading silver producer, obtains about half of its output from mines in which silver is the principal ore metal. Many of the mines are epithermal fissure veins, and most host a polymetallic assemblage whose exploitation is economically dependent on the high silver values. Although acanthite [Ag2S] and native silver predominate in some veins, in others much of the silver occurs in silver sulfosalts and as silver substitutions in tetrahedrite [(Cu,Fe,Ag)i2Sb4Si3] and other minerals. 

The Shanbaidu polymetallic deposit comprises genetically related but spatially separate iron and lead-zinc skam deposits in the contact zone of quartz-diorite and limestone. The ore minerals are mainly magnetite, hematite, galena and sphalerite. The ore bodies are found at depths of 5-40 m, and the surface of the area is covered by 5-15 m of transported exotic overburden. Thermally-released Hg, data from samples collected at depths of 30, 60 and 80 cm in the soil along a traverse crossing both ore deposits are shown in Fig. 13-9. In the samples from 60 and 80 cm, clear anomalies mark the positions of the mineralisation. In the samples from 30 cm, however, the background is... 

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