Introduction
Demand has increased significantly for ores containing elements such as Te, Ge, Se and In. This is due to the fact that these elements are critical for a variety of high-technology applications, and future demand for them will continue to increase (Paradis, Reference Paradis, Simandl and Neetz2015). In addition, In and Ge are included in the latest list of Critical Raw Materials 2017 released by the European Commission. These elements seldom form primary ores but are mainly obtained as by-products of the refining of major metals from base-metal ores (Graedel et al., Reference Graedel, Gunn, Tercero Espinoza and Gunn2014; Paradis, Reference Paradis, Simandl and Neetz2015). For instance, Te and Se are largely produced from copper refining, and In and Ge from the processing of sphalerite in base metal ores. In order for the worldwide reserves/resources to be able to meet the ever-growing demand, alternative sources for these raw materials are essential. These four elements mentioned above occur in different ore types, including porphyry-epithermal deposits (Höll et al., Reference Höll, Kling and Schroll2007; Graedel et al., Reference Graedel, Gunn, Tercero Espinoza and Gunn2014; Paradis, Reference Paradis, Simandl and Neetz2015).
The Pampean Flat-Slab 27°00′–33°30′ segment in the central Andes of Argentina records a Miocene–Pliocene magmatic episode related to the eastward migration of the Andean magmatic arc (Ramos et al., Reference Ramos, Cristallini and Pérez2002). This migration was due to the flattening of the Nazca plate after the collision of the Juan Fernández Bridge, in this plate, with the Chilean trench (Barazangi and Isacks, Reference Barazangi and Isacks1976; Jordan et al., Reference Jordan, Isacks, Alrnendinger, Brewer, Ramos and Ando1983; Jordan and Allmendinger, Reference Jordan and Allmendinger1986; Gutscher et al., Reference Gutscher, Spakman, Bijwaard and Engdahl2000). From a metallogenetic point of view, the Pampean Flat-Slab segment is economically important as it hosts several porphyry and epithermal deposits, some of them world-class. From north to south, the three main metallogenic districts are Farallón Negro, Nevados de Famatina and San Luis Metallogenic Belt. The Farallón Negro district hosts two world-class porphyry deposits, Bajo de la Alumbrera (e.g. Proffett, Reference Proffett2004) and Agua Rica (e.g. Landtwing et al., Reference Landtwing, Dillenbeck, Leake and Heinrich2002; Franchini et al., Reference Franchini, Impiccini, Lentz, Ríos, Oleary, Pons and Schalamuk2011, Reference Franchini, McFarlane, Maydagán, Reich, Lentz, Meinert and Bouhier2015). Apart from the aforementioned deposits, this district hosts several epithermal systems, such as Alto de la Blenda and Capillitas, (e.g. Márquez-Zavalía, Reference Márquez-Zavalía and Zappettini1999; Márquez-Zavalía and Heinrich, Reference Márquez-Zavalía and Heinrich2016). The Nevados de Famatina district includes the Cu-Mo-Au porphyry-high-sulfidation epithermal system (Nevados de Famatina) and other epithermal deposits (e.g. Losada-Calderón and McPhail, Reference Losada-Calderón and McPhail1996). The San Luis Metallogenic Belt (Urbina and Sruoga, Reference Urbina and Sruoga2009) hosts silver-gold epithermal and gold-copper porphyry deposits. The two most important districts in the belt are La Carolina and Cañada Honda (Urbina et al., Reference Urbina, Sruoga and Malvicini1997; Urbina, Reference Urbina2005a,Reference Urbina and Rhodenb; Urbina and Sruoga, Reference Urbina and Sruoga2009; Gallard-Esquivel et al., Reference Gallard-Esquivel, Urbina, Suroga and Japas2012, Reference Gallard-Esquivel, Ibañes, Roquet, Suroga and Urbina2015). In some of the epithermal deposits mentioned above parageneses are found with Ge-, Te-, Se- and In-bearing minerals such as Alto de la Blenda (Márquez-Zavalía and Heinrich, Reference Márquez-Zavalía and Heinrich2016) and Capillitas (Marquez-Zavalía and Craig, Reference Marquez Zavalía and Craig2004) where new mineral species containing these elements (i.e. putzite, catamarcaite and ishiharaite) were identified (Paar et al., Reference Paar, Roberts, Berlepsch, Armbruster, Topa and Zagler2004a; Putz et al., Reference Putz, Paar, Topa, Makovicky and Roberts2006; Márquez-Zavalía et al., Reference Márquez-Zavalía, Galliski, Milan Drábek and Bernhardt2014). In the same way, the Cerro Negro in the Nevados de Famatina district presents a Te-bearing paragenesis (Schalamuk and Logan, Reference Schalamuk and Logan1994). The Cerro Cacho-Sierra de Umango (de Brodtkorb, Reference de Brodtkorb2009) is the type locality of two copper selenides: umangite and klockmannite (Paar et al., Reference Paar, Topa, Sureda, Stumpfl and Mühlhaus2004b).
The ‘La Carolina’ district is a volcanic complex of ~9 km2 that comprises several small mineralized areas (Urbina et al., Reference Urbina, Sruoga and Malvicini1997), including Cerro Mogote and Puesto La Estancia prospects on which this study is focused. The district has been explored intermittently for gold since the 1980s until the first decade of the present century, when the exploration was stopped. However, the district has not been explored for other commodities such as In and Ge. The aim of the present study was to characterize the mineralogy and paragenesis of the Te-Ge-Se-In-bearing minerals that occur in the epithermal mineralizations of the Cerro Mogote and Puesto La Estancia prospects. Here the results of combined optical microscopy, scanning electron microscopy (SEM) and electron microprobe analysis (EMPA) for several ore-bearing samples are presented. The results provide a better understanding of the distribution of these elements in porphyry-epithermal systems in the central Andes of Argentina.
Geological setting
The La Carolina district is located in the southern sector of the Sierras Pampeanas Orientales geological province (Caminos, Reference Caminos and Turner1979), in the Sierra de San Luis (San Luis province, Argentina) (Fig. 1). It is located at the western end (32°48′10″S, 66°3′45″W, 1750 m.a.s.l) of the San Luis metallogenetic belt, which is related spatially and genetically to Miocene-Pliocene volcanism.
(a) Location of the La Carolina district at the western end of the metallogenic belt of San Luis, in San Luis province, Argentina. (b) Geological map of the La Carolina district, showing various prospects and major vein deposits. The study area is marked by a dashed-line rectangle (after Gallard-Esquivel, Reference Gallard-Esquivel2015).
These volcanic rocks intruded and overlaid a Proterozoic–Palaeozoic basement, which comprises rocks of different metamorphic grades, and igneous rocks corresponding to different cycles of granitic plutonism in the Palaeozoic (Morosini et al., Reference Morosini, Ortiz Suarez, Otamendi, Pagano and Ramos2017). Intrusive magmatism is part of the Famatinian orogenic cycle, which extended from early Precambrian to Devonian time (Aceñolaza and Toselli, Reference Aceñolaza and Toselli1981). In the study area, the metamorphic basement comprises the high-grade Pringles Complex (Sims et al., Reference Sims, Stuart-Smith, Lyons and Skirrow1997) and the low-grade San Luis Formation (Prozzi and Ramos, Reference Prozzi and Ramos1988; Prozzi, Reference Prozzi1990). The former includes schists, gneisses, migmatites and amphibolites, and the latter phyllites, meta-quartzites and meta-volcanic rocks. The contacts between these metamorphic units consist of N to NNE-trending ductile shear zones. In addition, these rocks show a sub-vertical penetrative NNE foliation, which is attributed to compression of the rocks during the Famatinian orogeny (Ortiz Suárez et al., Reference Ortiz Suárez, Prozzi and Llambías1992; Sato et al., Reference Sato, Gonzáles and Llambías2003).
Reactivation of existing N–S, E–W and NW–SE oriented faults during the Andean orogenic cycle gave the Sierras Pampeanas of San Luis a fault-block style of deformation with a steep western hillslope where the uplifted Andean front is located. This structural pattern controlled the Miocene–Pliocene magma emplacement. In La Carolina district, structural analyses show that the early structures strongly controlled the emplacement of the volcanic rocks and associated hydrothermal mineralization (Japas et al., Reference Japas, Urbina, Sruoga and Gallard2011a,Reference Japas, Urbina, Sruoga and Gallardb; Gallard-Esquivel et al., Reference Gallard-Esquivel, Urbina, Suroga and Japas2012). This volcanic district is rhomboid in shape, and characterized by two parallel-to-foliation sets of faults (N–S and NNE, Fig. 1). Slip on the main N–S faults indicates dominant right-lateral motion whereas NNE faults show components of vertical slip. The presence of a gentle deflection in the foliation trend (~30°) resulted in a NNE releasing bend, allowing magma emplacement in this pull-apart structure. Furthermore, previous studies by Japas et al. (Reference Japas, Urbina and Sruoga2010) at Cañada Honda district confirm strike-slip structures controlling Miocene–Pliocene volcanic emplacement at the western end of the San Luis metallogenetic belt (Japas et al., Reference Japas, Urbina, Sruoga and Gallard2011a). In the La Carolina district, volcanic activity occurred between 8.2 and 6.3 Ma (Urbina and Sruoga, Reference Urbina and Sruoga2009) and consists of lavas and pyroclastics (surges and phreatic breccias) of andesitic, dacitic, latitic and trachytic composition. The magmas of intermediate composition belong to normal to high-K calc-alkaline and shoshonitic suites (Gallard-Esquivel et al., Reference Gallard-Esquivel, Ibañes, Roquet, Suroga and Urbina2015). The La Carolina volcanic field has been interpreted as a maar-diatreme system, which was disturbed by dome emplacement (Sruoga et al., Reference Sruoga, Urbina and Malvicini1996). Spatially related to this maar-diatreme system there are several small Au-Ag epithermal deposits (Urbina et al., Reference Urbina, Sruoga and Malvicini1997; Urbina and Sruoga, Reference Urbina and Sruoga2009). The ore occurrences show two main styles: (1) disseminations including stockworks, disseminated zones and veins/veinlets in volcanic and pyroclastic rocks, in the metamorphic basement, or in hydrothermal breccias; and (2) major veins hosted by the igneous-metamorphic basement (Márquez-Zavalía and Galliski, Reference Márquez-Zavalía and Galliski1994, Reference Marquez-Zavalía and Galliski2004; Urbina et al., Reference Urbina, Sruoga and Malvicini1997; Urbina, Reference Urbina2005a,Reference Urbina and Rhodenb; Urbina and Sruoga, Reference Urbina and Sruoga2009; Gallard-Esquivel et al., Reference Gallard-Esquivel, Urbina, Suroga and Japas2012).
Sampling and analytical procedures
Polished-thin and polished sections of 47 samples were taken from three drill cores of Cerro Mogote prospect (DDH51, DDH36 and DDH49) and two drill cores from the Puesto La Estancia prospect (DDH31 and DDH33, Fig. 2a). These samples were studied by transmitted- and/or reflected-light microscopy, and using a JEOL-6610LV scanning electron microscope in association with chemical microanalysis by means of energy dispersive X-ray (EDAX). Electron microprobe analyses (EMPA) were performed using a CAMECA SX100 equipped with five wavelength-dispersive spectrometers. Major elements were determined at 20 kV accelerating potential, 20 nA beam current and an acquisition time between 10 and 20 s on X-ray peak and half that time on the background. The standard deviation of the EMPA is <0.1%. In order to analyse the trace-element content of sulfides, these analytical conditions were modified in order to attain lower detection limits. In the case of pyrite, the operating conditions were 20 kV, 100 nA and 120–180 s count time. The detection limits were 250 ppm for Au, 245 ppm for Ag, 205 ppm for Sb, 160 ppm for Cu, 88 ppm for Se, 200 ppm for Te, 280 ppm for As, 200 ppm for Zn, 150 ppm for Ni, and 495 ppm for Co (95% confidence). X-ray mapping with EMPA identified zonings of trace elements (e.g. Cu, Se, Ag) that are not detectable by SEM-EDAX. The conditions for the X-ray mapping were 20 kV accelerating potential, 100 nA beam current, 2 μm scan distance, and 100 ms X-ray peak acquisition time per point.
(a) Geological map of the Puesto La Estancia and Cerro Mogote prospects, showing the locations of the drill cores from which samples were taken. (b) Sample from drill core DDH51 (92 m depth) corresponding to fractured and mineralized metamorphic host-rocks. (c) Photomicrograph under plain-polarized and transmitted light of a thin section from the sample in (b). The photo shows a vein filled with quartz (qz), pyrite (py) and illite (ilt), the latter which appears as pseudomorphs after adularia crystals. (d) Phreatic breccia from drill core DDH31 (79.5 m depth).
Operating conditions for sphalerite analyses were 20 kV and 20 nA for most elements, and 100 nA for In and Ag. The detection limits for trace elements measured in sphalerite (i.e. In, Ga, Cd, Ag, Ge) were 135 ppm for In, 114 ppm for Ga, 120 ppm for Ge, 526 ppm for Cu, 110 ppm for Ag and 646 ppm for Cd (95% confidence). The detection limits for trace elements measured in galena were 191 ppm for In, 150 ppm for Ge, 140 ppm for Ag, 350 ppm for Sb, 1600 ppm for Bi, 1050 ppm for Se, 525 ppm for Cu and 750 ppm for Zn (95% confidence).
The X-ray intensities acquired were corrected for atomic number, mass absorption and secondary fluorescence effects using the CAMECA x-phi program. The following X-ray lines and analyzing crystals (in parentheses), were used: AuLα (LLiF), AgLα (LPET), BiLα (LLiF), SbLα (LPET), PbMα (LPET), FeKα (LLiF), CuKα (LLiF), ZnKα (LLiF), CdLα (LPET), NiKα (LLiF), CoKα (LLiF), TeLα (LPET), SKα (LPET), SeLα (LTAP), AsLβ (LTAP), InLα (LPET), GaKα (LLiF). The potential X-ray emission lines interferences were taken into account (i.e. As-on-Se, Te and Se-on-Pb, and In-on-Sn and Ga) and the Virtual WDS software (Reed and Buckley, Reference Reed, Buckley and Benoit1996) was used for developing the analysis strategy. The well documented Sn-on-In interference (SnLɳ line-on-InLα line) was ruled out as the Sn content of the sphalerite studied is negligible. Regarding As-on-Se peak overlap, the intensity of this interference was corrected using the ‘overlapping option’ provided by the CAMECA SX Peak Sight Software. Moreover, the background position was set much closer to the SeLα peak position and was estimated by counting at each side of the peak. To avoid In-on-Ga peak overlap, the selected X-ray lines InLα and GaKα were analysed using LPET and LLiF crystals, respectively. To avoid Se-on-Pb peak overlap, the chosen X-ray lines were SeLα (LTAP) and PbMα (LPET). For Te-on-Pb, the selected line was TeLα because it overlaps third- and fourth-order emission lines of Pb which, essentially, are not excited under the current analytical conditions (20 kV, 100 nA). Thus, the influence of this overlap is considered to have been negligible. The standards employed were commercially available metals, sulfides, selenides and tellurides: FeS2, Ag2Te, Au, Sb2S3, PbS, Bi, InAs, CoAsS, Ni, CuFeS2, ZnS, Bi2S3, FeAsS, Cu, and CdSe. All analyses were obtained at the University of Oviedo, Spain.
Sample description and results
Sulfide mineralization occurs as disseminations to vein/veinlets and fracture infillings in both the volcanic rocks and the metamorphic basement. In the latter, graphite was observed locally in the veins and in their selvages. Moreover, the ore mineralization is also found in hydrothermal breccias, mainly as cavity infilling. Sulfide mineralization mainly consists of pyrite with smaller amounts of sphalerite and galena. Chalcopyrite and pyrrhotite occur in minor amounts and commonly as inclusions in pyrite and partially replaced by marcasite, tetrahedrite–tennantite, digenite, covellite and acanthite.
Two types of veins/veinlets and fracture infillings (Fig. 2b) have been defined on the basis of the gangue minerals that accompany the sulfides: Type-1 or quartz + sericite + illite + sulfide veins and Type-2 or quartz + carbonate + sulfide veins.
In Type-1 veins, which occur mainly in drill cores DDH51 and DDH36 from the Cerro Mogote prospect (Fig. 2a), pyrite is the dominant sulfide followed by sphalerite and galena in lesser proportions. Both quartz and pyrite are located at the vein margins, although they are sometimes the only infill. Quartz grains are heterogeneous in terms of size and show no preferential growth orientation (Fig. 2c). This type of vein generally shows grains, tabular in shape, pseudomorphed by sericite-illite which may have replaced pre-existing adularia as it has the characteristic habit of the low-temperature K-feldspar. The last infill is also illite.
Type-2 veins are characterized by the presence of abundant carbonates, which exhibit different textures and compositions: fine-grained Fe-Mn carbonates (siderite–rhodochrosite), bladed rhodochrosite and kutnahorite, or banded crystals with very variable amounts of Mn-Mg-Fe-(±Ca). The Ca content of carbonates increases with depth and time in the paragenetic sequence. Kutnahorite and dolomite represent the carbonates with the highest Ca contents, calcite not having been detected. Quartz and K-feldspar are less common, the latter occurring as tabular crystals in vein selvages and partially replaced by carbonates. In addition, diamond-shaped adularia is intergrown with carbonate crystals. Sphalerite and galena are more abundant in these veins than in the Type-1 veins. Type-2 veins are prevalent in the Puesto La Estancia prospect (drill cores DDH31 and DDH33, Fig. 2a), below ~110 m from the present erosion level, crosscutting volcanic rocks of latite-andesitic composition.
Metallic mineralization is also found in hydrothermal breccias (Fig. 2d), mainly in the shallowest parts of the Puesto La Estancia prospect (from ~110 m below the present erosion level). The hydrothermal breccias are matrix-supported (60–70% matrix), and consist of subangular to surrounded polymict clasts set in a matrix that varies from rock flour to hydrothermal massive cement (carbonate + quartz + sulfide), commonly containing vugs. The clasts are mainly fragments of volcanic rocks of latite-andesitic composition. These fragments show hydrothermal alteration that varies from phyllic to argillic alteration and/or carbonatization. Smaller numbers of clasts of mica-schist from the metamorphic basement also occur. In these breccias, the sulfides are accompanied by carbonates with compositions similar to those that infill interclast cavities. The sulfides are present either as thin crusts on the cavity walls or as semi-massive to massive filling.
Sulfide textures and chemical composition
Pyrite
Pyrite is ubiquitous and commonly occurs as subhedral to cubic grains (4 µm to ~1 mm in size), disseminated throughout the matrix of host-rocks (volcanic and metamorphic), of the breccias and within the breccia clasts. Pyrite was the first sulfide deposited although it does occur intermittently throughout the period of sulfide-carbonate deposition. Pyrite crystals exhibit several concentric overgrowth zones, some of them inclusion-rich, implying multiple episodes of deposition (Fig. 3). The inclusions consist of μm to sub-μm grains of galena, Ag-rich tetrahedrite, pearceite and acanthite. Where these inclusions were plucked during polishing, pyrite shows a pseudoporous texture. The last stage of pyrite deposition is characterized by small crystals (<50 µm) associated with bladed Mn-rich carbonate and alabandite, which grew at the grain margins of sphalerite in hydrothermal breccias (Fig. 4a,b).
(a) Photomicrograph of zoned pyrite crystals from sample DDH51-106.4, under plane-polarized and reflected light. EMPA X-ray images of As (b), S (c), Fe (d), Cu (e) and Se (f) showing the distribution of these elements in the zoned pyrite crystal. The core is As-rich with oscillatory and sector zoning, in antithetic relationship with S and Fe. The Se is concentrated in the As-rich zones. The red areas in part (f) are Se-bearing galena grains. The core is overgrown by barren pyrite followed by a Cu-rich pyrite. The analytical conditions are indicated in the text.
(a) Photomicrograph of zoned sphalerite crystals infilling a breccia cavity from sample DDH31-79.5B, under plane-polarized and transmitted light. The red bands are rich in Fe (up to 12 wt.%), and the largest amounts of In are found in the clear and yellowish Fe-poor sphalerite. Mn-carbonate is filling the interstitial cavities, with inclusions of pyrite and alabandite. The sphalerite crystals show a Mn-rich black rim at the contact with the carbonate. (b) The same image under reflected light. The dark-red bands have abundant inclusions of chalcopyrite (‘chalcopyrite disease’) and sometimes pyrrhotite (not shown). (c) Photomicrograph of a quartz-carbonate-sulfide vein from sample DDH31-197, under plane-polarized and transmitted light. The sphalerite crystals show light brown cores, In-bearing, and black rims rich in Mn. There are two stages of carbonate filling, the first one, Fe-rich (red colour) and the second, Mn-rich, the latter partially replacing sphalerite crystals. (d) Photomicrograph under plane-polarized and reflected light of a tennantite-bearing mineralization (sample DDH51-76.5).
Back-scattered electron images, X-ray mapping and EMPA of pyrite crystals from sample DDH51-106.4 reveal that cores are rimmed by at least three generations of pyrite bands (Fig. 3b–f). The results of representative EMPA, carried out on each pyrite generation, are listed in Table 1. The cores of these crystals are characterized by a high variation in As content. This variation is oscillatory (Fig. 3b,c) and there is also a differential enrichment of As in growth sectors, similar to that observed by Chouinard et al. (Reference Chouinard, Paquette and Williams-Jones2005). Based on the EMPA, As values range from 0.2 to 5 wt.%. The pyrite cores also show trace quantities of Cu (up to 1697 ppm), Ag (up to 643 ppm) and Te (up to 595 ppm), whereas Sb, Au, Ni and Co were below the limits of detection (LOD). The cores are rimmed by a growth band with few or no detectable trace elements (barren pyrite), followed by a Cu-rich band (up to 6209 ppm Cu). The last stage of pyrite growth is also poor in trace elements. The X-ray maps for Se (Fig. 3f) indicate that this element is mainly concentrated in the As-rich cores.
Selected electron microprobe analyses (wt.%) of the different growth zones of pyrite from sample DDH51-106.4 (Fig. 3) in the Cerro Mogote prospect. Other elements analysed were Au, Sb, Ni and Co, all of which were always below their detection limits.
–: below detection limit.
Electron microprobe analyses and the X-ray maps show that the main substitution is As for S in pyrite (Cook and Chryssoulis, Reference Cook and Chryssoulis1990; Simon et al., Reference Simon, Huang, Penner-Hahn, Kesler and Kao1999; Savage et al., Reference Savage, Tingle, O'Day, Waychunas and Bird2000); however, a correlation between As and Fe also exists (Fig. 3b,d). The As-rich cores are also Ag-bearing, suggesting that both ions entered the structure of pyrite as part of a coupled substitution. Chouinard et al. (Reference Chouinard, Paquette and Williams-Jones2005) suggested a possible substitution of Ag+ + As3+ = 2Fe2+.
Galena
Galena typically occurs as inclusions in, and intergrown with, early pyrite and/or sphalerite (Fig. 4b). In places, it overgrew pyrite (Fig. 3a). Electron microprobe analyses show that Ag, Bi, Se and, to a lesser extent, Sb are the most common trace elements. The largest amounts of Ag and Bi (up to 5056 and 9188 ppm, respectively) were measured in galena from core samples located at ~200 m below the present surface. In this case, the correlation observed between these elements indicates a coupled substitution of Pb2+ for Bi3+ and Ag+.
Sphalerite
In hydrothermal breccias, sphalerite commonly exhibits compositional growth banding, sometimes oscillatory, from dark red Fe-rich bands to lighter orange-yellow Fe-poor sphalerite (Fig. 4a). However, this banded sphalerite is uncommon in the veins. Sphalerite can show a black rim rich in Mn where it is in contact with Mn-rich carbonate (Fig. 4a,c). Disseminated chalcopyrite blebs are common and locally abundant (so-called ‘chalcopyrite disease’). In banded sphalerite, the blebs are abundant in the dark red Fe-rich bands, where coarser grains of chalcopyrite also occur with pyrrhotite (Fig. 4b).
The Fe content of sphalerite ranges between 0.1 and 12 wt.%, although most of the sphalerite analyses show an Fe content of <2 wt.% (Table 2, Fig. 5a). The highest values of Fe were measured in the dark-red bands of the zoned sphalerite crystals from hydrothermal breccias (Fig. 4a). The concentration of Mn is also highly variable, showing two different correlation trends between Fe and Mn (Fig. 5a): Fe-poor sphalerite from Cerro Mogote samples have, in general, a greater Mn content than sphalerite from the Puesto La Estancia prospect. In the latter, the lower Mn content of sphalerite is coincident with a significant abundance of Mn-rich carbonates in the gangue minerals. Thus, the explanation for this sphalerite poorer in Mn could be that the carbonates tend to incorporate manganese easier than the sphalerite. Only the black rim developed between sphalerite and carbonates (Fig. 4a,c) appears enriched in Mn. In the case of Cu, the majority of the analyses show Cu contents of <2 wt.%, although values up to 9 wt.% have been measured in sphalerite with chalcopyrite inclusions (chalcopyrite disease). These high values are due to submicrometre chalcopyrite inclusions having been analysed, and these analyses have not been considered. Nevertheless, Cu concentrations of tens of thousands of ppm (up to 3.6 wt.%) were measured using a LA-ICP-MS by Cook et al. (Reference Cook, Ciobanu, Pring, Skinner, Danyushevsky, Shimizu, Saini-Eidukat and Melcher2009) in samples from In-rich sphalerite from Toyoha Cu-Zn-In deposits (Japan), also showing Ag up to 1.2 wt.%.
Binary correlation diagrams (wt.%) between EMPA of sphalerite from various samples from the Puesto La Estancia and Cerro Mogote prospects. (a) Fe vs. Mn. (b) In vs. Zn. (c) In + Ga + Ge vs. Cu + Ag. Further detail in the text.
Average EMPA results of sphalerite from samples of drill cores from the Puesto La Estancia (DDH31, DDH33) and Cerro Mogote (DDH51, DDH36) prospects, La Carolina district.
Number of analyses in parentheses;
– not detected or below detection limit.
Cadmium typically ranges from 2400 to 3600 ppm. Gallium and Ge were only detected in one sample (DDH33-203), with values up to 2697 ppm and 460 ppm, respectively. Silver was detected in some analyses (~20%), with values ranging from the detection limit (LOD) to 2490 ppm (Table 2). The In content measured in sphalerite was from 135 ppm (LOD) to 1900 ppm, with two values of 3625 and 5940 ppm obtained locally in sphalerite from sample DDH33-203. As observed in Fig. 5b, the highest In contents measured were in sphalerite with the lowest Fe contents.
Chalcopyrite and tetrahedrite–tennantite group minerals
Apart from the tiny inclusions in sphalerite, chalcopyrite is locally abundant and appears to surround sphalerite and pyrite grains, partially replacing them, or occurs as fracture infillings within sphalerite (Fig. 4d). The tetrahedrite–tennantite group minerals are commonly associated with chalcopyrite and overgrew chalcopyrite and sphalerite grains (Fig. 4d), or infilled veinlets. They also form discrete inclusions in chalcopyrite, sphalerite and pyrite. Based on EMPA (Table 3), they have been classified as members of the tetrahedrite–tennantite solid solution, with minor substitution by Te and Ag (up to 3.4 wt.% and 3.2 wt.%, respectively), and as Ag-rich tetrahedrite (Moëlo et al., Reference Moëlo, Makovicky, Mozgova, Jambor, Cook, Pring, Para, Nickel, Graeser and Karup-Møller2008), with values of silver between 9 and 20 wt.% (e.g. analyses DDH31-23 and 24, Table 3). The largest amounts of Te (up to 3.3 wt.%) were measured in sample DDH33-203, which contains a telluride-rich assemblage. The Sb/(Sb + As) and Ag/(Ag + Cu) ratios (apfu) vary from 0 to 0.919 and from 0 to 0.327, respectively, and there is a correlation between the chemical composition of the tetrahedrite–tennantite group minerals and depth of the sample, the Sb- and Ag-richest varieties occurring in the shallowest samples (Table 3).
Selected EMPA results of tetrahedrite–tennantite group minerals from the Puesto La Estancia and Cerro Mogote prospects, La Carolina district.
The analyses are sorted by drill core (first row) and by the depth of the sample in metres (second row). The Sb/(Sb + As) and Ag/(Ag + Cu) ratios increase towards shallower samples. Atom ratios were calculated on the basis of 29 atoms per formula unit.
– below detection limit
n.a.: not analysed.
The largest amount of Mn was measured in tennantite from sample DDH36-179 (up to 4 wt.% Mn), although the Ag-rich tetrahedrite from sample DDH36-51 also showed significant amounts of Mn (up to 1.8 wt.%). Incorporation of Mn in synthetic tetrahedrite was reported by Makovicky and Karup-Møller (Reference Makovicky and Karup-Møller1994). Values of Mn content from natural specimens are rare in the literature, the highest values (up to 6 wt.% Mn) corresponding to samples from epithermal deposits in Romania (Damian, Reference Damian2003) and Hungary (Dobosi and Nagy, Reference Dobosi and Nagy2000).
Mineralogy and chemistry of Ag-bearing minerals
The main precious-metal minerals are silver sulfides and sulfosalts, such as acanthite, argyrodite (the Ge-bearing mineral) and the pearceite–polybasite group of minerals, in addition to Au-Ag alloy.
Acanthite is the most common Ag-bearing sulfide, occurring as rounded irregular-shaped grains included in earlier-formed sulfides such as pyrite and sphalerite, associated with galena and/or chalcopyrite with curvilinear boundaries between phases (Fig. 6a). Gold-silver alloy, as rounded micro-inclusions, is also associated spatially with acanthite. Based on petrographic observations, another type of acanthite replaced pearceite–polybasite minerals, showing a porous and dusty appearance (Fig. 6b). Quantitative microanalysis of acanthite was quite difficult because of the destabilization of the mineral under the electron beam, especially in the dusty acanthite, and the results of just a single analysis are given in Table 4.
Photomicrographs under plane-polarized and reflected light. (a) Rounded acanthite (ac) inclusions, often with galena and chalcopyrite, within sphalerite crystals. Sample DDH36-191. (b) Pearceite–polybasite (prc-plb) group minerals replacing galena. (c) Argyrodite grains (arg) filling interstitial cavities between sphalerite and quartz crystals, along with pyrite (py), chalcopyrite (ccp) and Au-Ag alloy (el). There is also covellite (cv) after chalcopyrite (same sample as in a). (d) Pyrite (py) overgrown and partially replaced by galena (gn) and sphalerite (sp). Pyrite crystals show abundant irregular and rounded inclusions of Ag-bearing minerals (black arrows). Sample DDH31-79.5. (e) Detail from part (d) showing an intergrowth between hessite (hs, greyish white with a brownish shade) and cervelleite (crv, light blue). (f) Image of the telluride-rich chalcopyrite bearing sample DDH33-203 from the Puesto La Estancia prospect.
Selected EMPA results of Ag-bearing minerals from various samples of drill cores from the Puesto La Estancia and Cerro Mogote prospects, La Carolina district.
– below detection limit.
*SEM-EDAX analyses.
Argyrodite is commonly associated with sphalerite and galena. It occurs as irregular grains, up to 40 µm in size, included or attached to the margin of sphalerite grains (Fig. 6c), or as rounded inclusions in pyrite (Fig. 6d). The EMPA show up to 2 wt.% Zn and up to 1.2 wt.% Hg (Table 4).
The minerals of the pearceite–polybasite group appear as small rounded inclusions in pyrite (Fig. 7d) or as irregular grains that replaced galena (Fig. 6b and the BSE image in Fig. 7b). Taking into account that only the chemical composition is available, classification suggested by Bindi et al. (Reference Bindi, Evain and Menchetti2007) was used here: phases with As > Sb should be named pearceite [Ag9CuS4][(Ag,Cu)6(As,Sb)2S7]; phases with Sb > As should be named polybasite [Ag9CuS4][(Ag,Cu)6(Sb,As)2S7] (Table 4).
Back-scattered electron images (BSE) of samples shown in Fig. 6. (a) Rounded and irregular inclusions of acanthite (ac), Se-bearing argyrodite (Se-arg) and Se-bearing cervelleite (Se-crv). Some inclusions contain minute grains of Au-Ag alloy (el). The BSE image, bottom right, is from sample DDH36-191; the others are from sample DDH31-79.5. (b) Detail of Fig. 6b. Galena has been partially replaced by pearceite (prc) and polybasite (plb), which are also replaced by acanthite (ac) with a porous, dusty appearance. (c) Galena surrounded by hessite (hs) and benleonardite (bnl). Sample DDH31-79.5. (d) A small grain of alburnite (alb) associated with hessite and galena. Sample DDH31-79.5. (e) Complex aggregate of tellurobismuthite (tbs), hessite (hs), stutzite (stz), sylvanite (sy), volynskite (vl) and galena (gn). Sample DDH33-203. (f) Irregular inclusions of tellurides in chalcopyrite including stutzite (stz), volynskite (vl) and altaite (alt) instead of galena. Sample DDH33-203.
With regard to gold-silver alloys: free gold is rarely detectable at the microscopic scale. The gold grains observed vary from <1 µm to 20 µm in size, and occur as inclusions within sphalerite and pyrite in association with acanthite, argyrodite and pearceite–polybasite minerals (Fig. 6c). Due to its small size there is only one EMPA result, with an Ag content of ~36 wt.%, although qualitative SEM-EDAX analyses show Ag contents of ~25 wt.%. Gold was not detected in pyrite so if there is ‘invisible gold’, it would be in amounts which are below the detection limit (250 ppm).
In the Puesto La Estancia prospect, the mineral paragenesis is locally enriched in Se and Te. The silver telluride, hessite (Ag2Te), occurs instead of acanthite. Hessite has been found intergrown with Se-rich cervelleite (Ag4TeS, Fig. 6d,e), although Se-cervelleite also occurs as inclusions in pyrite sometimes associated with μm-sized Au-Ag alloy (Fig. 7a). Moreover, Te- and Se-bearing examples of argyrodite and polybasite–pearceite group minerals, have been detected by EMPA or, in the case of very small phases, by SEM-EDAX analyses (Tables 4 and 5).
Electron microprobe analyses of Te- and Se-bearing pearceite–polybasite.
– below detection limit.
The pearceite–polybasite group minerals show variable amounts of both Te and Se (3.5–4.4 wt.% Te, 0.16–2.3 wt.% Se, Table 5). The lowest Se contents (<0.2 wt.%) were measured in the Cerro Mogote prospect (sample DDH51-102 in Table 5), although only one analysis is suitable. Moreover, the EMPA of the sample from the Puesto La Estancia prospect (sample DDH31-79.5 in Table 5) show up to 3572 ppm Au, although due to the resulting high LOD for Au (1870 ppm) in the analysis of these sulfides, most of the values were below the detection limit.
Benleonardite [Ag15Cu(As,Sb)2S7Te4] and alburnite (Ag8GeTe2S4), the Te-rich members of the pearceite–polybasite and argyrodite group, respectively, were identified by SEM imaging and only SEM-EDAX analyses are shown in Table 4. Both minerals are associated spatially with galena and hessite (Fig. 7c,d).
One of the samples from the Puesto La Estancia prospect was especially rich in Te and the paragenesis of accessory minerals is composed of telluride minerals other than hessite including: sylvanite [(Ag,Au)2Te4], petzite (Ag3AuTe2), stutzite [Ag5–xTe3, (x = 0.24–0.36)], altaite (PbTe), tellurobismuthite (Bi2Te3) and volynskite (AgBiTe2). They occur as aggregates, up to 50 µm in diameter, associated with chalcopyrite (Fig. 6f). Some of these aggregates are complex, including several different minerals or only one or two phases (Fig. 7e,f). Galena is also present in these aggregates (Fig. 7e). A compilation of the EMPA performed on these tellurides is presented in Table 6 and show anomalous Fe and Cu contents by secondary fluorescence from nearby chalcopyrite, due to the usually small size of the tellurides.
Selected EMPA results of tellurides from the Puesto La Estancia prospect, La Carolina district.
– below detection limit.
*SEM-EDAX analysis.
Discussion
The mineral paragenesis and textures observed (Fig. 8) in samples from the Cerro Mogote and Puesto La Estancia prospects suggest the existence of different pulses of fluids and fracturing supported by open-space filling and brecciation textures in mineralized veins and breccias and by the variation in the chemical conditions of fluids during mineralization. Fluctuation in pH between slightly acidic and neutral to more alkaline conditions is suggested by the presence of K-feldspar alternating with illite, and the abundance of Mn-Fe-Mg(±Ca) carbonates, especially in the Puesto La Estancia. In addition, the carbonate deposition would be favoured by an increase in oxygen fugacity (f O2) and CO2 concentration (e.g. Damian, Reference Damian2003; Canet et al., Reference Canet, Camprubí, González-Partida, Linares, Alfonso, Piñeiro-Fernández and Prol-Ledesma2009; Chinchilla et al., Reference Chinchilla, Ortega, Piña, Merinero, Moncada, Bodnar, Quesada, Valverde and Lunar2016).
Paragenetic sequence of the prospects studied (Cerro Mogote and Puesto la Estancia).
The formation of zoned pyrite, with As-rich cores and Cu-rich bands, also indicates compositional variations in fluids as it grew. Similar alternating As- and Cu-rich bands in pyrite crystals were described by Deditius et al. (Reference Deditius, Utsunomiya, Ewing, Chryssoulis, Venter and Kesler2009) from the Pueblo Viejo and Yanacocha high-epithermal deposits, and Franchini et al. (Reference Franchini, McFarlane, Maydagán, Reich, Lentz, Meinert and Bouhier2015), from the Agua Rica epithermal-porphyry deposit. Deditius et al. (Reference Deditius, Utsunomiya, Ewing, Chryssoulis, Venter and Kesler2009) interpreted these changes in fluid composition as the result of mixing of a pyrite-forming fluid and magmatic vapour that invaded the main hydrothermal system episodically. In the deposits studied here, during the early pyrite deposition, fluids would have been characterized by a sulfur fugacity above the equilibrium boundary of pyrite + As = arsenopyrite, because arsenopyrite was not deposited. During the main base-metal ore deposition, fluids would have progressed to lower sulfur fugacities that favoured the precipitation of Fe-rich sphalerite and pyrrhotite. However, a subsequent increase in sulfur fugacity would support the deposition of a new generation of Fe-poor sphalerite and the final deposition of pyrite and alabandite, in breccia cavities.
Trace elements in sphalerite
Apart from Fe, EMPA of sphalerite show that it contains variable amounts of Mn, Cu, Cd, In, Ga, Ge and Ag. In most of the samples, the In contents > LOD were in yellowish, Fe-poor sphalerite, and there is no correlation between In and other trace elements including Cu, Mn and Cd. Nevertheless, the highest In contents (up to 5940 ppm) were measured in sphalerite grains from the DDH33-203 sample that also show Ga and Ge concentrations >LOD. In this sample, there is a correlation between In and Cu + Ag, which improves if Ga and Ge are also considered (Fig. 5c). This suggests a coupled substitution mechanism resulting in monovalent cation enrichment (i.e. Ag+ and Cu+) with respective tri- and tetravalent cation enrichments (e.g. Sb3+, Ga3+, In3+, As3+, Ge4+ and Sn4+) (Cook et al., Reference Cook, Ciobanu, Pring, Skinner, Danyushevsky, Shimizu, Saini-Eidukat and Melcher2009). The Mn content of sphalerite is, in general, greater in samples from the Cerro Mogote prospect than from the Puesto La Estancia prospect, which also correlates with the abundance of Mn-rich carbonates in the latter.
Several recent studies exist of trace-element contents in sphalerite from different types of Pb-Zn deposits (e.g. Moura et al., Reference Moura, Botelho and Carvalho de Medonca2007; Cook et al., Reference Cook, Ciobanu, Pring, Skinner, Danyushevsky, Shimizu, Saini-Eidukat and Melcher2009, Reference Cook, Sundblad, Valkama, Nygård, Ciobanu and Danyushevsky2011; Ye et al., Reference Ye, Cook, Ciobanu, Yuping, Qian, Tiegeng, Wei, Yulon and Danyushevskiy2011; Belissont et al., Reference Belissont, Boiron, Luais and Cathelineau2014; Frenzel et al., Reference Frenzel, Hirsch and Gutzmer2016) that have shown significant differences in the concentrations of the elements In, Ga and, Ge in sphalerite. The authors mentioned previously the differences in formation temperatures, with greater In contents associated with magma-related deposits (skarns, granite-related mineralization, epithermal and massive sulfide deposits), whereas the presence of Ga and Ge in sphalerite is associated with low-temperature hydrothermal deposits (e.g. carbonate-replacement MVT deposits). However, Sahlström et al. (Reference Sahlström, Arribas, Dirks, Corral and Chang2017) recently published LA-ICP-MS high concentrations of Ga and Ge in In-rich sphalerite from the intermediate-sulfidation stage assemblage of the Mt Carlton high sulfidation epithermal deposit. These authors observed a positive correlation in the Cu + Ag vs. In + Ga plot similar to that observed in sphalerite of sample DDH33-203 from Puesto La Estancia. In the Mt Carlton deposit, the highest concentrations of In (up to 2169 ppm) and Ga (up to 2829 ppm) in sphalerite occur in the proximal, Cu-rich parts of the deposit (Sahlström et al., Reference Sahlström, Arribas, Dirks, Corral and Chang2017). Other examples of sphalerite enriched in In-Ga±Ge from Cu-rich assemblages of intermediate-sulfidation deposits have been also reported (e.g. Palai-Islica, Carrillo-Rosúa et al., Reference Carrillo-Rosúa, Morales-Ruano and Hach-Alí2008; Rosia Montana, Cook et al., Reference Cook, Ciobanu, Pring, Skinner, Danyushevsky, Shimizu, Saini-Eidukat and Melcher2009). The high Cu activity in the ore fluid is a strong control on In enrichment and, to a lesser degree, Ga enrichment in sphalerite, allowing the extensive incorporation of these elements in couple substitution with Cu (Sahlström et al., Reference Sahlström, Arribas, Dirks, Corral and Chang2017; Frenzel et al., Reference Frenzel, Hirsch and Gutzmer2016).
The presence of Ge and Ga in hydrothermal fluids probably derives from enrichment during the fractional crystallization processes of igneous rocks (Breiter et al., Reference Breiter, Gardenová, Kanický and Vaculovič2013), or they were derived from the country rocks, particularly from those containing organic material (Bernstein, Reference Bernstein1985; Höll et al., Reference Höll, Kling and Schroll2007). According to the latter authors, the behaviour of Ge appears to be dependent on the sulfur fugacity conditions whereby Ge enters the structure of sphalerite in low to moderate sulfur activity and forms its own phases under higher fugacity of sulfur. High-sulfidation states favour Ge concentration through the formation of the thiocomplex [GeS4]4− and thiogermanates, preferably as Cu- and Ag-sulfide minerals, e.g. germanite, renierite, briartite and argyrodite (Bernstein, Reference Bernstein1985; Paar et al., Reference Paar, Roberts, Berlepsch, Armbruster, Topa and Zagler2004a; Paar and Putz, Reference Paar, Putz, Zhao and Guo2005).
In the current study, the enrichment of Ge is mainly associated with the presence of argyrodite, whereas the Ge content in sphalerite is commonly low, below the detection limit (120 ppm). Only sphalerite from sample DDH33-203 from the Puesto La Estancia prospect shows Ge contents above the detection limit. The presence of graphite in samples from the metamorphic basement suggests that the increase of Ge and Ga in the hydrothermal fluid could be due to the leaching of country rocks, although a magmatic source cannot be ruled out.
Telluride paragenesis
The enrichment of certain trace ore elements, such as Te, Se and Bi, in the Puesto La Estancia and Cerro Mogote prospects, emphasizes a likely magmatic contribution to the mineralized fluid (Cooke and McPhail, Reference Cooke and McPhail2001). Selenium is a highly chalcophile element and substitutes readily for sulfur in sulfide minerals (Simon et al., Reference Simon, Kesler and Essene1997). Tellurium is less compatible in sulfides than Se due to the greater atomic radius of the telluride ion (Te2− = 2.11 Å) than that of the selenide (Se2− = 1.88–1.90 Å) and sulfide ions (S2− = 1.56–1.78 Å). Therefore, Te will commonly tend to form tellurides during later stages of mineralization when the 
$f_{Te_2}/f_{{\rm s}_2}$ ratio in the ore fluid increases as a result of deposition of early sulfides (Simon et al., Reference Simon, Kesler and Essene1997). An approximation to the 
$f_{{\rm Te}_2}$ and 
$f_{{\rm S}_2}$ conditions for the Ag-Au paragenesis of the Puesto La Estancia prospect is shown in Fig. 9 (after Afifi et al., Reference Afifi, Kelly and Essene1988), at 250°C. No data exist to constrain the exact temperature for the telluride precipitation, but this temperature is reasonably expected for this epithermal systems. Nevertheless, although the absolute fTe2 and fS2 values will shift with changing temperature, the topologies of these diagrams are essentially constant and they are useful for comparison of telluride assemblages (Afifi et al., Reference Afifi, Kelly and Essene1988). The low 
$f_{{\rm Te}_2}$ necessary to precipitate hessite explains the common occurrence of this telluride in the Ag-rich paragenesis in association with acanthite and Au-Ag alloy (±cervelleite). In the telluride paragenesis, the absence of Au-Ag alloy may be used to define the lower limit of 
$f_{{\rm Te}_2}$. The lower limit would correspond approximately to the hessite-γ reaction (Fig. 9) because sylvanite may be formed by the breakdown of the phase γ [(Au,Ag)1.9Te] (Affifi et al., 1988). This limit indicates an increment of ~8 log units of Te2 fugacity. The presence of both altaite and galena defines 
$f_{{\rm Te}_2}$ and 
$f_{{\rm s}_2}$ conditions on the galena-altaite reaction, within the stability field of pyrite (Fig. 9).
Telluride-sulfide stability diagram, at 250°C (after Afifi et al., Reference Afifi, Kelly and Essene1988), for different Ag parageneses observed in ore samples from the Puesto La Estancia prospect. Abbreviations: bn: bornite, ccp: chalcopyrite, hs: hessite, po: pyrrhotite, py: pyrite, stz: stutzite, γ: phase (Au,Ag)1.9Te.
The textural relationships observed in Puesto La Estancia suggest that tellurides post-date the formation of sulfide minerals (Fig. 8), which is in agreement with the interpretation of Simon et al. (Reference Simon, Kesler and Essene1997). Larger 
$f_{{\rm Te}_2}$ values in the mineralizing fluids can be produced by rejuvenation through the incorporation of magmatic fluids. Oxidized magmatic fluids can carry high levels of Te over a wide range of pH values (Cooke and McPhail, Reference Cooke and McPhail2001; Grundler et al., Reference Grundler, Brugger, Etschmann, Helm, Liu, Spry, Tian, Testemale and Pring2013), whereas the solubility of Te is low under reducing conditions at acidic to neutral pHs, with Te mainly concentrated in the vapour (Grundler et al., Reference Grundler, Brugger, Etschmann, Helm, Liu, Spry, Tian, Testemale and Pring2013). According to those authors, at mildly reducing conditions (hematite-pyrite stability) and alkaline pHs, Au-rich (≥300 ppb Au; Au transported as Au(HS)2−) solutions can also carry significant Te. In addition to that, Manske et al. (Reference Manske, Ullrich, Reynolds and O'Connor2004) suggested a contribution of magmatic vapour for the origin of the Te-rich paragenesis in the intermediate-sulfidation epithermal deposit of Rosia Montana (Romania). In the case of Puesto La Estancia, telluride mineralization is hosted by an andesitic lava with argillic alteration. X-ray diffraction shows that the altered host-rock consists of quartz, illite, kaolinite and dickite (Gallard-Esquivel, Reference Gallard-Esquivel2015). This alteration suggests more acidic pH conditions that could reduce tellurium solubility in the hydrothermal fluid. But at this level of knowledge we do not have sufficient data to confirm this.
Se- and Te-bearing pearceite–polybasite
The contents of Te and/or Se in minerals of the pearceite–polybasite group have been reported from various types of hydrothermal ore deposits (e.g. Harris et al., Reference Harris, Nuffield and Frohberg1965; Warmada et al., Reference Warmada, Lehmann and Simandjuntak2003; Jelen et al., Reference Jelen, Kovalenker and Gaber2007; Kovalenker et al., Reference Kovalenker, Kiseleva, Krylova and Andreeva2011; Voudouris et al., Reference Voudouris, Spry, Sakellaris and Mavrogonatos2011). In Argentina, Márquez-Zavalía and Heinrich (Reference Márquez-Zavalía and Heinrich2016) cited the presence of Te-bearing polybasite in the intermediate-sulfidation epithermal vein system of Alto de la Blenda. Se-bearing polybasite was reported by Márquez-Zavalía et al. (Reference Márquez-Zavalía, Bindi, Márquez and Menchetti2008) in the epithermal gold-silver deposit of Martha mine, with values of up to 3 wt.% Se. Mugas-Lobos et al. (Reference Mugas-Lobos, Márquez-Zavalía and Galliski2011) reported a Se-bearing polybasite, with 4.18 wt.% of Se, along with naumannite (Ag2Se) and Se-bearing acanthite and cervelleite from the Don Sixto deposit. Note that most of those authors reported chemical compositions that are Se-rich or Te-rich, but the two elements do not occur together. Only Warmada et al. (Reference Warmada, Lehmann and Simandjuntak2003) reported one analysis of Te-bearing polybasite with 5.5 wt.% of Te and 3.6 wt.% of Se. In the case of the pearceite–polybasite minerals from Puesto La Estancia (Table 5), both elements are present. Moreover, another difference is that these analyses correspond to pearceite (or arsenopolybasite after Hall, Reference Hall1967), with a high As content of 2.8–5 wt.%.
The structural role of Se in polybasite was studied by Bindi et al. (Reference Bindi, Evain and Menchetti2007), who defined a new mineral species of the group, ‘selenopolybasite’. Moreover, Bindi et al. (Reference Bindi, Voudouris and Spry2013) investigated the role of Te in this group of minerals, refining the structure of a Te-rich polybasite. Those authors found that the Te-for-S substitution occurs at the same structural sites where Se substitutes for S in selenopolybasite, suggesting the possibility that ‘telluropolybasite’ could be found in nature. As shown in Fig. 10, there is a stronger correlation between Se and S than there is between Te and S, suggesting that the presence of Se in the structure of polybasite is by substitution of S for Se with a nearly constant Te content. The Cu content is low (<5 wt.%) in accordance with the hypothesis of Bindi et al. (Reference Bindi, Evain and Menchetti2007) that the Cu content of the pearceite–polybasite group minerals is very low if Se and/or Te are present.
Variation diagrams showing the correlation between S (apfu) and (a) Se (apfu) and (b) Te (apfu) in the pearceite–polybasite minerals from samples of the Puesto La Estancia and Cerro Mogote prospects. Analyses are shown in Table 6.
Gold mineralization
Gold occurs mainly as an Au-Ag alloy or in tellurides. Invisible gold in pyrite has not been found, although it could be present in amounts below the detection limit (250 ppm). Trace-gold contents were commonly detected in pearceite–polybasite (Table 5). The gold content in these minerals was previously mentioned by Gamarra-Urrunaga et al. (Reference Gamarra-Urrunaga, Castroviejo and Bernhardt2013) in Pallancata deposit, Peru. These authors pointed to the presence of a precursor Au-rich, high-temperature silver sulfide. The amounts of Au measured in the silver sulfosalts from the Puesto La Estancia prospect and the common association of gold (Au-Ag alloy) with silver minerals such as acanthite, hessite or cervelleite (Fig. 7) indicates that gold deposition was synchronous (Fig. 8) with the formation of silver sulfides and sulfosalts, after the main base-metal ore deposition.
Comparison with other epithermal deposit
From a mineralogical point of view, the Au-Ag epithermal mineralization of the Cerro Mogote and Puesto La Estancia prospects, in the La Carolina District, shares many similarities with the Alto de la Blenda epithermal deposit (Márquez-Zavalía and Heinrich, Reference Márquez-Zavalía and Heinrich2016), located in the NW of Argentina within the Farallón Negro volcanic district, and the Rosia Montana epithermal deposit (Wallier et al., Reference Wallier, Kouzmanov, Pettke, Heinrich, Leary, Connor, Tamas and Vennemann2006), in Romania.
The Alto de la Blenda epithermal mineralization is hosted by veins, with multiple events of opening and brecciation, and by polymict breccias. The mineralization consists of pyrite, sphalerite, chalcopyrite, galena and the tetrahedrite–tennantite group of minerals as the main sulfides, and of quartz and Mn-rich carbonates as gangue minerals. Adularia is absent from all vein stages (Márquez-Zavalía and Heinrich, Reference Márquez-Zavalía and Heinrich2016). Sphalerite crystals also appear zoned, with yellowish and Fe-poor cores surrounded by darker and Fe-rich rims (up to 3.18 wt.% Fe). The precious-metal paragenesis comprises Au-Ag alloy, the polybasite–pearceite group of minerals (including the Te-bearing polybasite discussed above), acanthite and Ag-Cu sulfides such as mackinstriyite (Márquez-Zavalía and Heinrich, Reference Márquez-Zavalía and Heinrich2016). However, a telluride-rich paragenesis such as that studied in the Puesto La Estancia prospect has not been found in the Alto de la Blenda deposit. In the nearby Capillitas deposit, which is also part of the Farallón Negro volcanic district, Marquez-Zavalía and Craig (Reference Marquez Zavalía and Craig2004) described a complex telluride paragenesis that includes native tellurium, krennerite, calaverite, sylvanite, petzite, hessite and stützite. According to Putz et al. (Reference Putz, Paar and Topa2009), the Capillitas deposit comprises high- and intermediate-sulfidation mineralization that was overprinted by supergene processes. In the case of the Alto de la Blenda deposit and according to Márquez-Zavalía and Heinrich (Reference Márquez-Zavalía and Heinrich2016), the main sulfide assemblage together with the presence of abundant Mn-rich carbonates, beside quartz, support the classification of the deposit as an intermediate-sulfidation Au-Ag deposit (Hedenquist et al., Reference Hedenquist, Arribas and González-Urien2000) or as a carbonate-base metal-gold vein system (Corbett and Leach, Reference Corbett and Leach1998).
The Rosia Montana deposit, in Romania, is a breccia-hosted epithermal system related to significant phreatomagmatic activity due to the shallow emplacement of the Montana dacite (Wallier et al., Reference Wallier, Kouzmanov, Pettke, Heinrich, Leary, Connor, Tamas and Vennemann2006). Mineralization consists of quartz, adularia, carbonates (commonly Mn-rich), with pyrite, sphalerite, galena, chalcopyrite, marcasite, arsenopyrite, alabandite and tetrahedrite as common sulfides. In this case, sphalerite is Fe-poor. Silver sulfides and sulfosalts are abundant, e.g. acanthite, the polybasite–pearceite group of minerals, proustite or argyrodite. In addition, as was mentioned previously, there is a telluride-rich paragenesis that includes hessite, sylvanite and petzite, and Te-bearing argyrodite (Tămas et al., Reference Tămaş, Bailly, Ghergari, O'Connor and Minuţ2006). The Rosia Montana was also classified as an intermediate-sulfidation epithermal deposit (Wallier et al., Reference Wallier, Kouzmanov, Pettke, Heinrich, Leary, Connor, Tamas and Vennemann2006), with an important magmatic contribution to the mineralizing fluids.
In the case of the epithermal mineralization from Puesto La Estancia and Cerro Mogote prospects, the mineral paragenesis rich in base-metals and Ag, and the presence of Mn-Mg-Fe(±Ca) carbonates as dominant gangue minerals would lead to it being classified as a carbonate-base metal deposit (Corbett and Leach, Reference Corbett and Leach1998) or as an intermediate-sulfidation deposit (Hedenquist et al., Reference Hedenquist, Arribas and González-Urien2000). As noted above, the chemical conditions of the hydrothermal fluids varied during ore and gangue deposition in the mineralization of the Puesto La Estancia and Cerro Mogote prospects. These fluctuations may indicate the existence of different pulses of fluids (rejuvenation of the system) or variations produced by boiling, or of both, simultaneously. Fluid inclusions and stable isotope studies are needed in the La Carolina district to check this aspect.
Conclusions
The epithermal mineralization in the Cerro Mogote and Puesto La Estancia prospects, in the southeastern part of the La Carolina district (Argentina), consists of base metal and Mn-carbonate-rich mineralization, hosted in hydrothermal breccias and veins related to Mio–Pliocene maar-diatreme volcanic activity. The main conclusions of this study are:
(1) The main sulfide mineralization consists of pyrite, sphalerite and galena, with lesser amounts of chalcopyrite, marcasite, the tetrahedrite–tennantite group of minerals. Pyrite is compositionally zoned, with As-rich cores and Cu-rich rim overgrowths.
(2) Sphalerite shows a wide range of Fe contents (up to 12.5 wt.% Fe) and is compositionally zoned, with alternating Fe-rich and Fe-poor bands. The sphalerite also shows variable contents of Mn, Cu, In, Ga, Ge and Ag. Indium was detected mainly in the Fe-poor and yellowish sphalerite. The most In-rich sphalerite (up to 5940 ppm) also contains elevated concentrations of Cu, Ag, Ga and Ge, which suggests a coupled substitution mechanism resulting in monovalent cation enrichment (i.e. Ag+ and Cu+) with respective tri- and tetravalent cation enrichments (Ga3+, In3+, Ge4+).
(3) Precious-metal mineralization mainly occurs as Au-Ag alloy and silver sulfides and sulfosalts (acanthite, pearceite–polybasite group minerals, Ag-rich tetrahedrite). Local chemical variations produced Ge-bearing minerals (argyrodite) and/or Se-Te-bearing minerals (hessite, Se-cervelleite, Te-Se-pearceite–polybasite, benleonardite, alburnite). The higher-fugacity of Te produced a Au-Ag±Bi±Pb telluride assemblage (hessite, sylvanite, petzite, tellurobismuthite, volynskite, altaite).
(4) The present study is another example of how epithermal deposits can be mineral sources of trace elements such as In, Ge, Te, Se and Ga which, potentially, could increase the prospectivity of these deposits.
Acknowledgements
This study was supported by the ‘Proyecto de Ciencia y Técnica P-3-2-0414, of the National University of San Luis’ and by the Project CGL2016-76532-R from the MINECO of Spain. The authors thank Mr Miguel Angel Fernández, EMPA technician, for his assistance. They also thank the reviewers and the Associate Editor for their suggestions which have improved the content and clarity of the paper.
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