The Gersdorﬀite-Bismuthinite-Native Gold Association and the Skarn-Porphyry Mineralization in the Kamariza Mining District, Lavrion, Greece

: Vein-type Pb-Ni-Bi-Au-Ag mineralization at the Clemence deposit in the Kamariza and “km3” in the Lavrion area, was synchronous with the intrusion of a Miocene granodiorite body and related felsic and maﬁc dikes and sills within marbles and schists in the footwall of (and within) the Western Cycladic detachment system. In the Serpieri deposit (Kamariza area), a porphyry-style pyrrhotite-arsenopyrite mineralized microgranitic dike is genetically related to a garnet-wollastonite bearing skarn characterized by a similar base metal and Ni (up to 219 ppm) enrichment. The Ni–Bi–Au association in the Clemence deposit consists of initial deposition of pyrite and arsenopyrite followed by an intergrowth of native gold-bismuthinite and oscillatory zoned gersdorfﬁte. The zoning is related contribution to the ore-forming ﬂuids, although remobilization and leaching of metals from previous mineralization and/or host rocks, through the late involvement of non-magmatic ﬂuid in the ore system, cannot be excluded. evaluates the primary mineralogical and chemical characteristics of the breccia/vein and carbonate-replacement mineralization at the Clemence (Kamariza district) and the “km3” district, which both host Ni-Au-Bi ores, and provides preliminary information on their potential genetic relationship to rocks in the Lavrion district The present study also describes the and in and describes a new A comparison chalcocite, covellite, hematite, löllingite,

Contacts between the upper and lower units are considered to be part of the Western Cycladic detachment system (Figure 1) [20,21]. A Miocene I-type granodiorite intrusion is exposed at Plaka (Figure 1), and was synchronous with the extensional detachment faulting [7,23,24]. Several occurrences of granite and granodiorite porphyry laccoliths, pipes, dikes and sills are exposed throughout the Lavrion district [1,7,16,24]. East to west trending diorite and granite dikes and sills crosscut the lower marble and the Kamariza schists in the Kamariza area. According to Marinos and Petrascheck [1], the largest dikes are found north of the "Serpieri 1" shaft, between the "Serpieri 1", "Ilarion 1" shafts, and south of the Ilarion orebody ( Figure 1b). The dikes are locally boudinaged, thus testifying to an emplacement before the activation of the WCDS. The mafic dikes are equigranular to porphyritic rocks consisting of plagioclase and biotite with interstitial quartz and albite. They have undergone propylitic alteration ( Figure 2a) and are characterized by chlorite, carbonates, actinolite, pyrite, and chalcopyrite that replaced primary minerals and/or which occur in veinlets and as disseminations in the groundmass. Adjacent to the marbles and the orebodies, the mafic dikes are pervasively altered to quartz-sericite ± kaolinite ± carbonates, and contain disseminated or vein sulfides. Felsic dikes at the Serpieri mine consist of primary plagioclase, biotite, and muscovite associated with quartz and orthoclase, the latter in micrographic intergrowth (Figures 2a, and 3a,b). Allanite-(Ce) and synchysite-(Ce) (CaCe[CO 3 ] 2 F) are included in plagioclase and in late magmatic quartz (Figure 3c,d). Biotite was partly replaced by chlorite. Figure 4 shows the geochemical characteristics of mafic and felsic igneous rocks in the Kamariza district. The Serpieri magmatic rocks analyzed in the present study (Table 1), plot in the calc-alkaline to high-K calc-alkaline field (Figure 4a) of Pecerrillo and Taylor [25], and are classified as microgranite in the TAS classification diagram of Middlemost [26] ( Figure 4b). Based on the discrimination diagrams of Schand [27] and Maniar and Piccoli [28], they are I-type granitoids and metaluminous to slightly peraluminous with ASI < 1.1 (Figure 4c,d), and can be considered subvolcanic equivalents of the Plaka granite.  Marinos and Petraschek [1] and Scheffer et al. [22]).  Ba  917  913  895  Ce  50  56  67  Cu  2  3  6  La  25  25  37  Nd  24  29  29  Pb  12  17  24  Rb  85  85  94  Sr  442  413  419  Zn  12  12  166  Zr  156 162 157 (b) carbonate-sericite-quartz veinlets with pyrrhotite (Po) and arsenopyrite (Apy) crosscutting microgranite in the Serpieri mine; (c) skarn mineralization at the contact between microgranite porphyry dike, hosting arsenopyrite (Apy) mineralization, and the lower Kamariza marble; (d) vein-style Pb-Zn-As-Ni-Au-Bi mineralization between marble and schist from the Clemence mine; (e) hand specimen of banded vein-style mineralization from the Clemence mine, consisting of initial deposition of pyrite (Py) and arsenopyrite (Apy), followed by the deposition of the assemblage of gersdorffite (Grf), bismuthinite (Bmt), gold (Au) and galena (Gn), and finally by the deposition of fluorite (Fl); (f) brecciated marble cemented by galena (Gn) and gersdorffite (Grf) mineralization. The Ni-arsenate annabergite (Anb) is a supergene alteration product of gersdorffite ("km3" deposit).

Figure 2.
Field photos and hand specimens of granitoids and Ni-bearing ores in the Lavrion district. (a) Propylitic-and kaolinite-sericite-altered microdiorite dike from the Jean Baptiste deposit; (b) carbonate-sericite-quartz veinlets with pyrrhotite (Po) and arsenopyrite (Apy) crosscutting microgranite in the Serpieri mine; (c) skarn mineralization at the contact between microgranite porphyry dike, hosting arsenopyrite (Apy) mineralization, and the lower Kamariza marble; (d) vein-style Pb-Zn-As-Ni-Au-Bi mineralization between marble and schist from the Clemence mine; (e) hand specimen of banded vein-style mineralization from the Clemence mine, consisting of initial deposition of pyrite (Py) and arsenopyrite (Apy), followed by the deposition of the assemblage of gersdorffite (Grf), bismuthinite (Bmt), gold (Au) and galena (Gn), and finally by the deposition of fluorite (Fl); (f) brecciated marble cemented by galena (Gn) and gersdorffite (Grf) mineralization. The Ni-arsenate annabergite (Anb) is a supergene alteration product of gersdorffite ("km3" deposit). In the Serpieri deposit, microgranite dikes are crosscut by porphyry-style sericite-chlorite-calcite ± quartz stockworks hosting sulfide mineralization consisting of pyrrhotite, arsenopyrite, pyrite, and galena (Figures 2b and 5a,b). The veinlets are related to carbonate-sericite alteration of the host rock, which overprints secondary biotite and K-feldspar, being part of an earlier potassic alteration event in the system. The skarn occurrence is located along the contact of a microgranitic body and the lower marble of Kamariza ( Figure 2c). It is a garnetitic skarn, with andradite, wollastonite, apatite, and magnetite being part of the prograde mineral assemblage ( Figure 3e). Calcite, actinolite, epidote, chlorite, quartz, and hematite, as well as pyrite, chalcopyrite, and pyrrhotite formed during the retrograde stage ( Figure 3f). Adjacent to the skarn the microgranite is carbonate-sericite altered and contains pyrrhotite and arsenopyrite ( Figure 2c).
The nickeliferous assemblage from Clemence mine is composed of vein-type mineralization, which developed at the contact between marbles and schists of the Kamariza unit [4] (Figure 2d). The mineralization also replaced marbles, where it forms extensive manto and chimney bodies. The mineralization in the Clemence vein is characterized by open space filling and mineralogical zonation. Pyrite, arsenopyrite, and sphalerite dominate in the outer parts of the vein, whereas galena and fluorite occur in its center (Figure 2e). Paragenetic relationships in the vein suggest initial deposition of pyrite, arsenopyrite, stannite, and Fe-rich sphalerite, followed by gersdorffite, bismuthinite, and native gold, then by chalcopyrite, tennantite/tetrahedrite, bournonite, enargite, and Fe-poor sphalerite, and finally by galena containing exsolved grains and inclusions of semseyite, boulangerite, native antimony, Ag-rich tetrahedrite, stephanite, and miargyrite ( Figure  5c-i). Quartz is the main gangue mineral in the early stage of ore deposition followed by fluorite, the latter of which accompanies galena. In the "km3" district, the nickeliferous assemblage is associated with veins of calcite and galena that crosscut brecciated upper marble of the Kamariza Unit (Figure 5j-l).  In the Serpieri deposit, microgranite dikes are crosscut by porphyry-style sericite-chlorite-calcite ± quartz stockworks hosting sulfide mineralization consisting of pyrrhotite, arsenopyrite, pyrite, and galena (Figures 2b and 5a,b). The veinlets are related to carbonate-sericite alteration of the host rock, which overprints secondary biotite and K-feldspar, being part of an earlier potassic alteration event in the system. The skarn occurrence is located along the contact of a microgranitic body and the lower marble of Kamariza ( Figure 2c). It is a garnetitic skarn, with andradite, wollastonite, apatite, and magnetite being part of the prograde mineral assemblage (Figure 3e). Calcite, actinolite, epidote, chlorite, quartz, and hematite, as well as pyrite, chalcopyrite, and pyrrhotite formed during the retrograde stage ( Figure 3f). Adjacent to the skarn the microgranite is carbonate-sericite altered and contains pyrrhotite and arsenopyrite ( Figure 2c).  [26]; (c) A/CNK vs A/NK plot from Shand [27] that discriminates metaluminous, peraluminous, and peralkaline compositions. A/NK = molar ratio of Al2O3/(Na2O + K2O); A/CNK = molar ratio of Al2O3/(CaO + Na2O + K2O); (d) ASI vs SiO2 plot discriminating metaluminous, peraluminous and S-from I-type compositions (after Maniar and Piccoli [28]). ASI = Al/(Ca-1.67P + Na + K). Literature data are from Stouraiti et al. [29], Skarpelis et al. [24] and Bonsall et al. [5].
The nickeliferous assemblage from Clemence mine is composed of vein-type mineralization, which developed at the contact between marbles and schists of the Kamariza unit [4] (Figure 2d). The mineralization also replaced marbles, where it forms extensive manto and chimney bodies. The mineralization in the Clemence vein is characterized by open space filling and mineralogical zonation. Pyrite, arsenopyrite, and sphalerite dominate in the outer parts of the vein, whereas galena and fluorite occur in its center (Figure 2e). Paragenetic relationships in the vein suggest initial deposition of pyrite, arsenopyrite, stannite, and Fe-rich sphalerite, followed by gersdorffite, bismuthinite, and native gold, then by chalcopyrite, tennantite/tetrahedrite, bournonite, enargite, and Fe-poor sphalerite, and finally by galena containing exsolved grains and inclusions of semseyite, boulangerite, native antimony, Ag-rich tetrahedrite, stephanite, and miargyrite (Figure 5c-i). Quartz is the main gangue mineral in the early stage of ore deposition followed by fluorite, the latter of which accompanies galena. In the "km3" district, the nickeliferous assemblage is associated with veins of calcite and galena that crosscut brecciated upper marble of the Kamariza Unit (Figure 5j-l).

Ore Mineralogy
Previous work by Voudouris et al. [4] described the mineralogy and mineral chemistry of metallic minerals from the Clemence deposit in detail. Additional information is given here: in summary, pyrite (Figure 5c,d) has Co and Ni contents below detection limits. It includes small grains of stannite (Cu 2 FeSnS 4 ) (Figure 5d). Arsenopyrite contains 41.10 to 43.15 wt.% As, which corresponds to 29.90-31.06 atomic % As. Early sphalerite is Fe-rich (up to 24.7 mole % FeS) and associated with arsenopyrite, whereas late sphalerite is Fe-poor (2.9 mole % FeS) and associated with the Cu-As-bearing association that includes chalcopyrite, tennantite, and enargite. Galena contains inclusions of gersdorffite, semseyite, bismuthinite, bournonite, native antimony, and native gold (Figure 5e-i). It also contains exsolved grains of boulangerite, Ag-rich tetrahedrite, stephanite (Ag 5 SbS 4 ), and miargyrite (AgSbS 2 ) (Figure 5h). Bismuthinite is included in gersdorffite and galena (Figure 5e-g). Native gold commonly forms grains up to 150 µm in size enclosed in gersdorffite, but can also be found as intergrowths with bismuthinite and/or as isolated grains enclosed in galena (Figure 5e,g). It contains 11.50 to 18.56 wt.% Ag [2]. Gersdorffite occurs as zoned idiomorphic crystals enclosed in galena, and as rims on pyrite and arsenopyrite (Figure 5d,f). It displays oscillatory zoning in terms of Fe, Ni, and As content, varying from~1.5 to 9.0 wt.%,~24 to 32 wt.% and 47 to 60 wt.%, respectively ( Table 2, Figures 6 and 7). There is an almost perfect linear correlation between Fe-Ni and As-S in the gersdorffite structure (Figure 7c,d). Gersdorffite from the Clemence deposit contains up to 0.2 wt.% Se, which likely substitutes for sulfur in the structure. At the "km3" locality, gersdorffite contains~0.5-2 wt.% Fe, 46-48 wt.% As, and~31-34 wt.% Ni ( Table 2). Millerite (NiS) is found in association with gersdorffite as small inclusions or as euhedral needle-shaped crystals enveloped by galena ( Figure 5j). As-bearing ullmannite, Ni(Sb,As)S, occurs as inclusions in gersdorffite (Figure 5k (Table 3).

Discussion
The genesis of the Pb-Zn-Ni-As-Bi-Au and the Pb-Ni-Co-As-Mo-Ag associations from the Clemence and "Km3" deposits, respectively, is still a matter of debate. Both styles of mineralization share some similarities with the so-called "five element" deposits that are characterized by the elemental association Ag-Ni-Co-As-Bi ± U [30,31]. The characteristic feature of these deposits is the presence of native silver in association with Ni-Co-Fe-Sb sulfarsenides, and Ni-Co-Fe arsenides, with the best examples containing the element association Ag-Ni-Co. In some respects, there are some common features of the studied mineralization and the five elements association but there are differences, including the absence of dendritic native silver and bismuth. The Kamariza veins are Pb-Zn-Cu-dominant and contain relatively little Ag-Bi-Co. Therefore, they do bear some resemblance to, but are not, classical five element veins.

Discussion
The genesis of the Pb-Zn-Ni-As-Bi-Au and the Pb-Ni-Co-As-Mo-Ag associations from the Clemence and "Km3" deposits, respectively, is still a matter of debate. Both styles of mineralization share some similarities with the so-called "five element" deposits that are characterized by the elemental association Ag-Ni-Co-As-Bi ± U [30,31]. The characteristic feature of these deposits is the presence of native silver in association with Ni-Co-Fe-Sb sulfarsenides, and Ni-Co-Fe arsenides, with the best examples containing the element association Ag-Ni-Co. In some respects, there are some common features of the studied mineralization and the five elements association but there are differences, including the absence of dendritic native silver and bismuth. The Kamariza veins are Pb-Zn-Cu-dominant and contain relatively little Ag-Bi-Co. Therefore, they do bear some resemblance to, but are not, classical five element veins.
A magmatic contribution for metals in the Lavrion area was proposed by Voudouris et al. [4] and Bonsall et al. [5], mainly based on the close spatial relationship of the deposits with porphyritic dikes of granodioritic to andesitic composition. A genetic relationship between nickel sulfides and sulfarsenides, native bismuth, bismuthinite, pyrrhotite, and precious metals (Au, Ag) with granitoid intrusions was reported previously from several ore deposits (e.g. Ulsan Fe-W deposit in S. Korea [32], Cradock in South Africa [33] and Erzgebirge, Germany [34]). For the multi-stage Ag-Bi-Co-Ni-U and Cu-Bi vein mineralization at Wittichen, Schwarzwald, SW Germany, which consists of Ni sulfarsenides, native Bi and various Bi sulfosalts, Staude et al. [35] suggested a granitic source for the occurrence of Bi in all stages and leaching from the host rock (redbeds) of some ore-forming elements (e.g. Ag, Co and Ni) at temperatures from around 300 to <100 • C. Remobilization and leaching of Co, Ni, Fe, and As from mafic/ultramafic wall rocks was favoured for the ore at Bou Azzer, Morocco [36] and Cobalt, Ontario, Canada [37]. However, at Bou Azzer, where no Bi-bearing minerals were reported, acidic magmatic fluids under moderately reducing conditions at high fluid/rock ratios leached Co, Ni, Fe, and As from serpentinites [36]. At the neighboring Imiter Ag-Hg deposit, Morocco, Essaraj et al. [38] distinguished two mineralizing events: The first is related to magmatic intrusions and comprises uneconomic Co-Ni-As ores that were superimposed by an economic, Ag-rich mineralization, deposited by basinal brines, which leached the metals from the basement rocks. Similarly, the likely source of Ni and Au in the Ni-Sb-Ag-Au association, as exemplified by the presence of ullmannite, allargentum, Au-rich silver, and Au-bearing dyscrasite, from the Kutná Hora Pb-Zn-Ag ore district (Czech Republic), was the serpentinized ultramafic bodies, which were cut by the "silver" lodes in the south of the ore district [39]. The scenario of remobilization and leaching of metals from previous mineralization and/or host rocks, including the metabasite boudins found in the Lavrio schists, through the late involvement of non-magmatic fluid in the ore system, was recently favoured by Scheffer et al. [40], for at least the Pb-Zn-Ag vein-style mineralization in the Lavrion district.
Oscillatory zoning is common in sulfides (e.g. pyrite, arsenopyrite, sphalerite, molybdenite and fahlores) [41][42][43]. Oscillatory zoning in gersdorffite was reported from the San Juan de Plan deposit, Spain [44], the high-grade Ni-Co-Fe-As hydrothermal vein ores from Dobšiná (Slovakia) [45], and from Pb-Ag-Zn deposits within the Rogozna ore field, Serbo-Macedonian metallogenic province [46]. The oscillatory variations in As, Ni, and Fe content of individual micro-zones observed within the Clemence gersdorffite suggest physical or chemical fluctuations within the bulk system and disequilibrium in the ore fluids [47].
On the basis of arsenopyrite composition (30.8 to 32.7 at. % As) for the pyrite-arsenopyrite assemblage at the Clemence deposit, a temperature range of 400-450 • C is deduced at f S 2 = 10 −6 to 10 −8 atm, using the calibrations of Kretschmar and Scott [48] and Sharp et al. [49] (shaded area, Figure 8a). It should be mentioned that the arsenopyrite geothermometer of Kretschmar and Scott [48] may overestimate temperatures when compared to those derived from fluid inclusion data, and underestimates sulfur fugacity since, according to the work of Sharp et al. [49], it is also a function of pressure. However, the lower limit of this temperature range is in accordance with the early quartz in the Kamariza district, which crystallized between 300 and 400 • C [4]. These temperatures are in agreement with those recorded during post-orogenic exhumation and mark the ductile-brittle transition [21,22]. Fluid inclusions in fluorite from the Clemence deposit associated with galena and homogenized at between 233 and 275 • C [4]. It is suggested here that the initial ore deposition at Clemence took place at about 350 to 400 • C at log f S 2 = −10 to −8. This range of temperature and f S 2 corresponds to deposition of pyrite-arsenopyrite-gersdorffite in equilibrium with Fe-rich sphalerite within the stability field of bismuthinite and native gold, and then by a decrease in the Fe content of sphalerite from about 25 to 3 mol % FeS, and by the deposition of enargite (arrow, Figure 8b). A subsequent path of decreasing temperature (from about 350 to 200 • C) probably occurs along the tennantite-enargite/luzonite boundary with contemporaneous deposition of galena (Figure 8b).
Previous work by Voudouris et al. [4] suggested that the association between bismuthinite and native gold in the gold-bearing galena ores within the Clemence deposit may have been caused by the sulfidation of maldonite in response to an increase in f S 2 , and that the presence of sulfarsenide minerals associated with native gold and bismuthinite from reduced hydrothermal fluids. If this was the case, maldonite should be part of a very early low-sulfidation and strongly reduced assemblage in the Kamariza district, in the stability field of pyrrhotite, arsenopyrite and/or löllingite (all three phases are present in Kamariza ore). Maldonite was not observed as part of the present study, although its presence in Lavrion ore was reported in association with native bismuth and native gold by Wendel and Markl [8] and Rieck [52]. However, Solomos et al. [3] argued for a contemporaneous deposition of chalcopyrite with bismuthinite, native bismuth, and maldonite (which was later decomposed to native gold and native bismuth) for oxidized Au-Bi ores in the Ilarion deposit in the Kamariza district. Native gold also occurs as isolated grains within galena but not in contact with bismuthinite, thus suggesting that the hydrothermal fluids were probably buffered along the boundary Au + Bi 2 S 3 /Au 2 Bi during gold deposition.
The discovery of a new, previously unknown skarn and porphyry-style mineralization in the Kamariza district gives new information on the origin of the sulfide mineralization in the Lavrion district. It also allows for a direct comparison with the major skarn and porphyry deposits of the neighboring Plaka area, since both skarn occurrences contain pyrrhotite, pyrite, and magnetite. Sulfide and oxide mineralogy are used to constrain f O 2 and f S 2 values of hydrothermal solutions during the evolution of the Serpieri skarn-porphyry style mineralization at 400 • C/0.5 kb and 275 • C (vapor saturation), in accordance with the temperatures estimated by fluid inclusion temperatures determined by Voudouris et al. [4] for the Kamariza district (Figure 8c,d). Early-stage skarn and contemporaneous porphyry-style mineralization formed at around 400 • C/0.5 kb at logf S 2 = −8 and −7 and logf O 2 = −27 ( Figure 8c). These values are consistent with the stability of the assemblage magnetite-pyrite-pyrrhotite in the ore system. During the retrograde stage of mineralization (e.g. at~275 • C), the logf S 2 = −11 and −9 and logf O 2 = −33 to −31 are constrained by the stabilities of pyrite, chalcopyrite, hematite, and galena ( Figure 8d). The mineral stability field in the Fe-As-S system, as well as the isopleth contours of As in arsenopyrite (at. %; dash-dotted lines) in equilibrium with vapor, were derived from Kretschmar and Scott [48] and Sharp et al. [49]. The iron content in sphalerite (moles % FeS; dotted lines) is drawn according to the data of Scott and Barnes [50]. Stability fields of native bismuth/bismuthinite and native gold + bismuthinite/maldonite and other sulfidation reactions involving sulfides, sulfarsenides, sulfosalts and native elements were derived from Barton and Skinner [51]. The conditions of formation during the precipitation of arsenopyrite and pyrite are indicated by the shaded area in Figure 5c. An evolution towards higher sulfur fugacities and then along the enargite/tennantite boundary with decreasing temperatures is indicated by the arrow in Figure 5b. Previous work by Voudouris et al. [4] suggested that the association between bismuthinite and native gold in the gold-bearing galena ores within the Clemence deposit may have been caused by the sulfidation of maldonite in response to an increase in fS2, and that the presence of sulfarsenide minerals associated with native gold and bismuthinite from reduced hydrothermal fluids. If this was the case, maldonite should be part of a very early low-sulfidation and strongly reduced assemblage in the Kamariza district, in the stability field of pyrrhotite, arsenopyrite and/or lӧllingite (all three phases are present in Kamariza ore). Maldonite was not observed as part of the present study, although its presence in Lavrion ore was reported in association with native bismuth and The mineral stability field in the Fe-As-S system, as well as the isopleth contours of As in arsenopyrite (at. %; dash-dotted lines) in equilibrium with vapor, were derived from Kretschmar and Scott [48] and Sharp et al. [49]. The iron content in sphalerite (moles % FeS; dotted lines) is drawn according to the data of Scott and Barnes [50]. Stability fields of native bismuth/bismuthinite and native gold + bismuthinite/maldonite and other sulfidation reactions involving sulfides, sulfarsenides, sulfosalts and native elements were derived from Barton and Skinner [51]. The conditions of formation during the precipitation of arsenopyrite and pyrite are indicated by the shaded area in Figure 5c. An evolution towards higher sulfur fugacities and then along the enargite/tennantite boundary with decreasing temperatures is indicated by the arrow in This study suggests that both the Kamariza skarn and the associated microgranites (porphyry-style veinlets) are mineralized with base metal sulfides (e.g. pyrite, chalcopyrite, pyrrhotite, arsenopyrite, sphalerite and galena), which is the same metallic mineral assemblage that characterizes the manto-and vein/breccia-style mineralization in the Lavrion district. Carbonate-replacement mineralization is especially enriched close to the contacts between dikes and the surrounding marbles and schists. It is suggested here that these intrusive bodies fed the deposit with metals and volatiles, as has been proposed previously [2][3][4][5].
In the "km3" district, deposition of Ni sulfides was followed by formation of gersdorffite, the presence of which indicates an increase in the As content and a decrease in the Ni activity of the hydrothermal fluid. Late galena associated with fluorite rims gersdorffite in both the Clemence deposit and "km3" district, demonstrating a common fluid evolution along the detachment system in the Lavrion district.

Conclusions
The famous Lavrion Pb-Zn-Ag-Au district hosts several Ni-Bi-Pb-bearing deposits that formed synchronously with the intrusion of a Miocene granodiorite body and related felsic and mafic dikes and sills within marbles and schists of the Attic-Cycladic blueschists. At the Seprieri deposit (Kamariza district), a porphyry-style pyrrhotite-arsenopyrite mineralized granitic sill/dike is genetically related to a garnet-and wollastonite-bearing mineralized skarn characterized by base metal sulfides and enriched in Mo, Sn, and Ni. At the neighboring Clemence deposit, oscillatory zoned gersdorffite is associated with native gold and bismuthinite within a vein-type Pb-Ni-Bi-Au-Ag mineralization, which contains arsenopyrite, pyrite, chalcopyrite, tennantite, enargite, and galena. Variable As, Ni, and Fe contents in gersdorffite indicate fluctuations in arsenic and sulfur fugacities in the hydrothermal fluid. An evolution towards higher sulfur fugacity in the mineralization is evident by the late deposition of enargite in the ore system. Gersdorffite-bearing ore from "km3" is associated with vaesite, millerite, ullmannite, and polydymite, enclosed in galena. Our data further support a magmatic contribution to the ore-forming fluids, although remobilization and leaching of metals from previous mineralization and/or host rocks, through the late involvement of non-magmatic fluid in the ore system, cannot be excluded.
Funding: This research was partly funded by LABEX Ressources21, Nancy, France.