A Fluid Inclusion and Critical/Rare Metal Study of Epithermal Quartz-Stibnite Veins Associated with the Gerakario Porphyry Deposit, Northern Greece

: The Gerakario Cu-Au porphyry deposit in the Kilkis ore district, northern Greece, contains epithermal quartz-stibnite veins on the eastern side of the deposit, which crosscut a two-mica gneiss. Metallic mineralization in these veins consists of stibnite + berthierite + native antimony + pyrite + arsenopyrite, and minor marcasite, pyrrhotite, chalcopyrite, löllingite, and native gold. Bulk geochemical analyses of the ore reveal an enrichment in critical and rare metals, including Ag, Au, Bi, Ce, Co, Ga, La, and Sb. Analysis of stibnite with LA-ICP-MS showed an enrichment in base metals (As, Cu, Pb), as well as weak to moderate contents of critical and rare metals (Ag, Bi, Ce, La, Re, Sm, Th, Ti, Tl). A statistical analysis of the trace elements show a positive correlation for the elemental pairs Ce-La, Ce-Sb, and La-Sb, and a negative correlation for the pair Bi-Sb. Fluid inclusions in the A-type veins of the porphyry-style mineralization show the presence of ﬂuid boiling, resulting in a highly saline aqueous ﬂuid phase (35.7 to 45.6 wt.% NaCl equiv.) and a moderately saline gas phase (14 to 22 wt.% NaCl equiv.) in the system H 2 O-NaCl-KCl at temperatures varying between 380 ◦ and 460 ◦ C and pressures from 100 to 580 bar. Mixing of the moderate saline ﬂuid with meteoric water produced less saline ﬂuids (8 to 10 wt.% NaCl equiv.), which are associated with the epithermal quartz-stibnite vein mineralization. This process took place under hydrostatic pressures ranging from 65 to 116 bar at a depth between 600 and 1000 m, and at temperatures mainly from 280 ◦ to 320 ◦ C.


Introduction
Critical raw materials (CRM) are integral components of a resilient and sustainable economy and society [1,2]. The 2020 European Union CRM list comprises the metals: Be, Bi, Co, Ga, Ge, Hf, In, Li, Nb, Sb, Sc, Sr, Ta, Ti, V, and W, as well as the group of rare earth elements (REE) and platinum group elements (PGE) [3]. A sustainable supply of mineral raw materials needs accessible deposits and efficiently productive mines [4]. Advances in ore exploration further contribute to achieving this supply chain.
Alkaline-to peralkaline-carbonatite igneous rocks, sedimentary uranium and phosphorite ores, and placer-type REE deposits are the main sources for critical and rare metals [5][6][7]. The exploitation of critical and rare metals mainly as by-products from porphyry-epithermal systems could support this effort [8,9]. Geological setting of the Cenozoic magmatic rocks and the related ore types in the Kilkis ore district, northern Greece (modified after References [23,24,[31][32][33]). The studied area in Gerakario is also shown.
The most important Sb deposits in the region are found at Rizana, Philadelphio, and Gerakario [23,31,32] (Figure 1). The Rizana (also known as Lachanas) shear-zone hosted deposit is found in sheeted quartz veins crosscutting two-mica gneiss and schist of the Vertiskos unit [28,[36][37][38]. Sericitization and silicification are observed in the basement rocks [36]. The ore mineralization is enriched in Sb and W and the ore assemblage includes stibnite, wolframite, sphalerite, pyrite, and berthierite, and traces of chalcopyrite, arsenopyrite, marcasite, and native antimony, arsenic, and gold [36,37]. Gangue minerals are quartz and barite, while alteration minerals include quartz, sericite, chlorite, calcite, and dolomite [36]. Between the 1930s and 1950s, 9000 tons of stibnite ore, with up to 40% of Sb in the produced concentrate, were extracted from underground mines [28]. Wolframite was also mined between the 1910s and 1940s. The measured reserves of stibnite (0.3 wt.% Sb in average) are 5000 t, and the indicated reserves vary between 50,000 and 100,000 t, including also 1000 t of wolframite [28].
At Philadelphio, Sb mineralization occurs in shear-zone hosted massive and discordant stibnite veins, crosscutting the metamorphic rocks of the Vertiskos unit [29] Figure 1. Geological setting of the Cenozoic magmatic rocks and the related ore types in the Kilkis ore district, northern Greece (modified after References [23,24,[31][32][33]). The studied area in Gerakario is also shown.
The most important Sb deposits in the region are found at Rizana, Philadelphio, and Gerakario [23,31,32] (Figure 1). The Rizana (also known as Lachanas) shear-zone hosted deposit is found in sheeted quartz veins crosscutting two-mica gneiss and schist of the Vertiskos unit [28,[36][37][38]. Sericitization and silicification are observed in the basement rocks [36]. The ore mineralization is enriched in Sb and W and the ore assemblage includes stibnite, wolframite, sphalerite, pyrite, and berthierite, and traces of chalcopyrite, arsenopyrite, marcasite, and native antimony, arsenic, and gold [36,37]. Gangue minerals are quartz and barite, while alteration minerals include quartz, sericite, chlorite, calcite, and dolomite [36]. Between the 1930s and 1950s, 9000 tons of stibnite ore, with up to 40% of Sb in the produced concentrate, were extracted from underground mines [28]. Wolframite was also mined between the 1910s and 1940s. The measured reserves of stibnite (0.3 wt.% Sb in average) are 5000 t, and the indicated reserves vary between 50,000 and 100,000 t, including also 1000 t of wolframite [28].
The Gerakario area has been explored for Cu, Au, Mo, and base metals between the 1970s and the 1990s [39]. The exploration of the Cu-Au porphyry deposit included soil geochemistry, geophysical surveys, and drilling [39,40]. Stibnite is hosted in quartz veins found at the periphery of the porphyry deposit. Stibnite was mined in the 1930s with underground galleries and wells, but the amount of the extracted ore is unknown. Probable and indicated reserves are up to 0.13 Mt of ore, grading 0.3% Cu and 1.4 g/t Au for the porphyry deposit [28]. Estimations on Sb resources and reserves are yet to be determined. In the present study, we investigate the distribution of the critical and rare metals in the Gerakario deposit, with bulk geochemical analysis of the quartz-stibnite veins and trace elemental analysis of stibnite by laser ablation inductively coupled plasma mass spectrometry (LA-ICP-MS). Emphasis is given on the elements: Ag, Au, Bi, Cd, Ce, Co, Ga, Gd, Ge, Hg, In, La, Nb, Nd, Re, Sb, Se, Sm, Ta, Te, Th, Ti, U, V, and W. Then, we evaluate the distribution of the critical and rare metals in stibnite by applying Pearson's correlation. Finally, on the basis of the microthermometric data collected from the A-type veins (porphyry stage) and the quartz-stibnite veins (epithermal stage), we reconstruct the history of the ore-related fluid evolution history. The results provide new data on the critical and rare metals endowment of the quartz-stibnite epithermal veins and a genetic model of the Gerakario porphyry-epithermal system.

Porphyry Cu-Au Mineralization
The porphyry mineralization at Gerakario (N 41.117023°, E 22.929289°) is genetically associated with syenite and hosted in syenite, granodiorite, and the surrounding metamorphic rocks [39]. Ore textures include disseminations and A-and D-type veins [39]. According to Frei [42], the porphyry type mineralization is found as disseminations with pyrite-chalcopyrite, and stockworks of A-type veins with magnetite-pyrite-chalcopyrite, spatially associated to potassically altered syenite. In addition, disseminations and D-type veins with pyrite and minor chalcopyrite are found in the sericitic alteration, which also affected the syenite, the granodiorite, and the metamorphic rocks [39,43]. The gneiss in contact with the syenite is strongly sheared and extensively altered [39]. Near the surface, the porphyry mineralization is significantly oxidized. In the oxidation zone, pyrite was replaced by goethite and jarosite, chalcopyrite by malachite, and magnetite by hematite [39,43,44].

Epithermal Sb Mineralization
In the eastern part of the porphyry system, Sb-rich mineralization (Ν 41.114297°, Ε 22.935334°) is hosted in epithermal quartz veins crosscutting the two-mica gneiss (Figures 2 and 3a). The quartz-stibnite veins are continuous, up to 10 cm in width, and

Porphyry Cu-Au Mineralization
The porphyry mineralization at Gerakario (N 41.117023 • , E 22.929289 • ) is genetically associated with syenite and hosted in syenite, granodiorite, and the surrounding metamorphic rocks [39]. Ore textures include disseminations and A-and D-type veins [39]. According to Frei [42], the porphyry type mineralization is found as disseminations with pyrite-chalcopyrite, and stockworks of A-type veins with magnetite-pyrite-chalcopyrite, spatially associated to potassically altered syenite. In addition, disseminations and D-type veins with pyrite and minor chalcopyrite are found in the sericitic alteration, which also affected the syenite, the granodiorite, and the metamorphic rocks [39,43]. The gneiss in contact with the syenite is strongly sheared and extensively altered [39]. Near the surface, the porphyry mineralization is significantly oxidized. In the oxidation zone, pyrite was replaced by goethite and jarosite, chalcopyrite by malachite, and magnetite by hematite [39,43,44].

Epithermal Sb Mineralization
In the eastern part of the porphyry system, Sb-rich mineralization (N 41.114297 • , E 22.935334 • ) is hosted in epithermal quartz veins crosscutting the two-mica gneiss (Figures 2 and 3a). The quartz-stibnite veins are continuous, up to 10 cm in width, and locally branched. They consist of massive stibnite with minor of berthierite, native anti-Appl. Sci. 2022, 12, 909 6 of 20 mony, pyrite, and arsenopyrite (Figure 3b-d). Traces of marcasite, pyrrhotite, chalcopyrite, löllingite, and native gold are also present [45]. Gangue minerals include quartz and minor calcite. Traces of valentinite (Sb 2 O 3 ) are related to supergene oxidation. Stibnite is the predominant ore mineral in the epithermal quartz veins (<5 cm in width) (Figure 3b). Quartz and calcite occur on the walls of the epithermal veins, and as veinlets (<2 cm in width) with traces of stibnite. A spatially limited hydrothermal halo consisting primarily of sericite is observed in the surrounding two-mica gneiss. Appl. Sci. 2022, 12, x FOR PEER REVIEW 6 of 21 locally branched. They consist of massive stibnite with minor of berthierite, native antimony, pyrite, and arsenopyrite (Figure 3b-d). Traces of marcasite, pyrrhotite, chalcopyrite, löllingite, and native gold are also present [45]. Gangue minerals include quartz and minor calcite. Traces of valentinite (Sb2O3) are related to supergene oxidation. Stibnite is the predominant ore mineral in the epithermal quartz veins (<5 cm in width) (Figure 3b). Quartz and calcite occur on the walls of the epithermal veins, and as veinlets (<2 cm in width) with traces of stibnite. A spatially limited hydrothermal halo consisting primarily of sericite is observed in the surrounding two-mica gneiss.

Fieldwork and Sampling
Fourteen samples (Ger 1 to Ger 14) were collected from the hydrothermally altered syenite and the surrounding metamorphic rocks at Gerakario. The sampling targeted the A-veins related to the porphyry system. In addition, eight samples (Ger 15 to Ger 22) were collected from the epithermal quartz-stibnite veins in the underground galleries.

Microscopy
Optical microscopy study was done at the Department of Mineralogy-Petrology-Economic Geology, Aristotle University of Thessaloniki (AUTh). In total, 15 polished sections were prepared and studied using a Leitz LaborLux 11 Pol dual reflected-transmitted light polarizing microscope (Leica Microsystems, Wetzlar, Germany) coupled.

Fieldwork and Sampling
Fourteen samples (Ger 1 to Ger 14) were collected from the hydrothermally altered syenite and the surrounding metamorphic rocks at Gerakario. The sampling targeted the A-veins related to the porphyry system. In addition, eight samples (Ger 15 to Ger 22) were collected from the epithermal quartz-stibnite veins in the underground galleries.

Microscopy
Optical microscopy study was done at the Department of Mineralogy-Petrology-Economic Geology, Aristotle University of Thessaloniki (AUTh). In total, 15 polished sections were prepared and studied using a Leitz LaborLux 11 Pol dual reflected-transmitted light polarizing microscope (Leica Microsystems, Wetzlar, Germany) coupled.

Bulk Chemical Analysis
Trace element bulk geochemical analysis, including REEs, was conducted by inductively coupled plasma atomic emission spectroscopy (ICP-AES) by dissolving samples in Aqua Regia. The geochemical analyses were carried out at MSALABS, Langley, BC, Canada. The full dataset is given in Table S1.

Scanning Electron Microscope
The polished sections were studied with a JEOL JSM-840A scanning electron microscope (SEM) (JEOL Ltd., Tokyo, Japan) equipped with an OXFORD INCA 300 energydispersive system (EDS) (Oxford Instruments Ltd., Abingdon, UK) at the Faculty of Sciences, AUTh. The operating conditions were a 20 kV accelerating voltage and 0.4 mA probe current, 80s analysis time, and a beam diameter of~1 µm, in the back-scattering electron (BSE) mode. Internal empirical corrections were performed to compensate for peak overlap. SEM-EDS micro-analysis was targeted on the mineral chemistry of stibnite and on the minerals found as micro-scale inclusions in it. Additionally, the antimony content was used as an internal standard in LA-ICP-MS analyses for stibnite. The average values of the conducted SEM-EDS analyses are given in Table S2.

LA-ICP-MS
Following electron microscopy study, two polished sections from the stibnite mineralization were analyzed by LA-ICP-MS. Trace element concentrations in stibnite were measured using a PerkinElmer ELAN DRC-e ICP (PerkinElmer Inc., Waltham, MA, USA) mass spectrometer combined with a New Wave UP193-FX excimer laser ablation system (New Wave Research, Inc., Fremont, CA, USA) at the Geological Institute, Bulgarian Academy of Sciences, Sofia, Bulgaria. The ablation was conducted in He medium. In order to maximize sensitivity, the ICP-MS was optimized daily with respect to the oxide production rate of ThO/Th (0.5%). Operating conditions of the laser system include 5 Hz repletion rate, 35 µm spot size, and energy density on analyzed minerals and standards of 5.0 to 5.2 J/cm 2 . The nebulizer gas flow rate was 0.8 L/min, while auxiliary and make-up gas flows rates were 0.92 L/min. The analysis time was 100 s (background: 40 s, laser-on the sample: 60 s). The acquisition dwell time was set to 0.02 s for 74 Ge, 82 Se, 115 In, 125 Te, and 202 Hg, to 0.03 s for 107 Ag, to 0.04 s for 197 Au, and to 0.01 s for all other elements. The monitored isotopes include: 27 Al, 31 P, 34 S, 49 Ti, 51 V, 53 Cr, 55 Mn, 57 Fe, 59 Co, 60 Ni, 65 209 Bi, 232 Th, and 238 U. The targeted areas in the polished sections were predefined to try and avoid mineral inclusions. Repeated external standardization was conducted by analyzing NIST SRM 610 glass standard, and the USGS Mass 1 sulfide standard.
Data reduction was performed by using the Sb contents of stibnite measured by SEM-EDS as internal standards and the SILLS software [46]. During data reduction, peakshaped fluctuations of the intensity signal of some isotopes were investigated in order to exclude the influence of other minerals on the chemical composition of the studied minerals. The full list of the LA-ICP-MS data, including elements ascribed to nano-scale mineral inclusions, is included in Table S3.
For the statistical analysis of the bulk geochemistry and the LA-ICP-MS analytical results, univariate analysis (minimum, maximum, standard deviation, and average), and bivariate analysis (Pearson's correlations: Table S4)

Fluid Inclusion Micro-Thermometry
Seven doubly-polished wafers of quartz in the veins from the Gerakario porphyry and epithermal mineralization, were prepared at the University of Hamburg, Germany, and were studied for fluid inclusions. A LINKAM THM-600/TMS 90 heating-freezing stage (Linkam, Surrey, UK) coupled to a Leitz SM-LUX-POL microscope (Leica Microsystems, Wetzlar, Germany) was used for the microthermometric measurements at the Department of Mineralogy-Petrology-Economic Geology, AUTh. Ice (H 2 O) and organic reference substances with known melting points were used to calibrate the stage. The upper limit of heating was at 600 • C, with a precision of the measurements ±1 • C during heating and ±0.2 • C during freezing. The software packages FLUIDS [47] and SoWat [48] were used for the estimation of the fluid compositions and properties. Densities were calculated from equations proposed by Driesner [49].

Mode of Occurrence of Stibnite
Stibnite in the epithermal veins is massive and forms granular aggregates ( Figure  3b). In some cases, stibnite inclusions (<100 μm in size) are found in quartz. Berthierite is commonly found as small inclusions in stibnite ( Figure 5a) and locally as thin lamellae

Mineral Chemistry of Stibnite
Stibnite exhibits weak to moderate trace elemental contents (Table 2, Figure 6). The full analytical dataset is given in Supplementary Materials (Table S2). Base (As, Cu, Pb) and critical and rare metals (Ag, Bi, Ce, La, Re, Sm, Th, Ti, Tl) are incorporated in stibnite

Statistical Analysis of Trace Elements Concentrations in Stibnite
Pearson product-moment correlation coefficients for stibnite are described by significant positive correlation (p < 0.01; value = 0.919) defined for the elemental pair Ce-La, and by positive correlations (p < 0.05; values: 0.563-0.589) for the pairs Ce-Sb and La-Sb (Table S3). A negative correlation (p < 0.05; value: −0.564) was defined for the elemental pair Bi-Sb (Table S3).

Fluid Inclusions Petrography
A study of fluid inclusions from the Gerakario porphyry system by Tombouloglou [44] revealed that the potassic alteration and the Cu precipitation took place from an initial magmatic fluid with high homogenization temperatures (Th = 350-600 • C) and high salinities (45-70% wt.% NaCl equiv.). The subsequent sericitic alteration and sulfide mineralization were formed by boiling fluids with lower salinities (38-45% wt.% NaCl equiv.) at lower temperatures (350-400 • C). Inclusions along healed cracks with homogenization temperatures <350 • C were characterized as secondary [44].
To further constrain the character of the ore fluids and the formation conditions of the Gerakario deposit, a fluid inclusion study was conducted on quartz from A-type veins related to the potassic alteration of the porphyry mineralization, and from the epithermal stibnite-quartz veins. Quartz in the veins is semi-transparent and anhedral, with the grains forming triple junctions at angles of~120 • (Figure 7a), implying extensive recrystallization [51]. This is typical of early high temperature quartz veins in many porphyry copper systems and suggests that the fluid inclusions migrated to grain boundaries [52]. The continuous and multiple flows of fluids caused re-opening of the veins and dynamic recrystallization of the quartz and commonly destroy a large part of the fluid inclusion assemblages [51,52].    Abbreviations: AVG = average value, AVG. Detection Limit = Average detection limit, b.d.l. = below detection limit, MIN = minimum value, MAX = maximum value, n = number of analyses, n.a. = not applicable, STDEV = standard deviation.
In the present study, most of the fluid inclusions are arranged in clusters (Figure 7a-c) that have escaped recrystallization. These inclusions are characterized by similar shapes and sizes and constant liquid to vapor ratios, and consequently are classified as primary, on the basis of the criteria proposed by Roedder [53] and Goldstein and Reynolds [54]. Fluid inclusions distributed along the growth zones of quartz are extremely rare and too small for microthermometry. The maximum length of the primary inclusions reaches 32 µm. In addition to primary fluid inclusions, rare secondary inclusions occur along healed cracks. In several inclusions, post-entrapment phenomena (necking down or leaking) are common, and no measurements were performed on them.
Based on the phase ratios observed on the inclusions from the Gerakario porphyry system and the epithermal stibnite veins at room temperature, in combination with their behavior during heating and freezing, three types of primary fluid inclusions were identified.
Type 1 inclusions consist of two-phases a liquid aqueous phase and a vapor phase where the vapor bubble occupies 30-40% of the volume of the inclusion. These inclusions homogenize into the liquid phase and are found in the porphyry-and the epidermal-related veins (Figure 7b,c).
Type 2 inclusions comprise three or four phases (Figure 7b,d,e), one liquid, one vapor (occupying 30 to 40% of the volume of the inclusions), and one or rarely two solid phases halite and sylvite. In exceptional cases, another solid unidentified phase was observed (Figure 7d). Type 2 inclusions homogenize into the liquid phase by bubble disappearance.
Type 3 fluid inclusions are two phases, liquid-vapor inclusions where the latter occupies 80-90% of the volume of the inclusion (Figure 7f). These inclusions homogenize into the vapor phase and rarely contain one or two opaque minerals, which are likely hematite and chalcopyrite (Figure 7e). Fluid inclusions of type 2 and 3 are found only in the porphyry system. Appl

Microthermometry
Initial melting temperatures of ice (Te) of fluid inclusions from porphyry type mineralization, range from −33.0 to −46.4 °C. This indicates that, in addition to NaCl, other salts, such as KCl, MgCl2, and/or CaCl2, are dissolved in the fluid [55]. The final ice melting temperatures (Tm) of the Type 1 inclusions range between −19.4 and −10.8 °C , indicating a moderate to relatively high salinity of 14.8 to 22 wt.% NaCl equiv. [56]. In type 3 fluid inclusions, Tm range from −16.5 to −12 °C demonstrating moderate to relatively high salinities of 14.4 to 19.8 wt.% NaCl equiv. in the H2O-NaCl-KCl system. Type 1 inclusions homogenize (Th) from 382° to 496 °C ( Figure 8, Table 3), while type 2 inclusions homogenize with the disappearance of the vapor bubble after the disappearance of the solid phases (more commonly halite than sylvite). In rare cases, another unidentified solid phase was observed, which is probably a chloride complex of Mg or Ca. Homogenization temperatures in the Type 2 inclusions range from 381° to 458 °C ( Figure 8, Table 3). Based on the solid phase homogenization temperatures (271-386 °C) and using the data for the system H2O-NaCl [56], the salinity of the type 2 inclusions range from 35.7 to 45.6 wt.% NaCl equiv. Type 3 fluid inclusions homogenize at temperatures from 381° to 504 °C (Figure 8). Homogenization temperatures of the fluid inclusions of 1, 2, and 3 types in the porphyry style mineralization overlap between 380° and 460 °C, with a distinct maximum at ~430 °C (Figure 8).

Microthermometry
Initial melting temperatures of ice (Te) of fluid inclusions from porphyry type mineralization, range from −33.0 to −46.4 • C. This indicates that, in addition to NaCl, other salts, such as KCl, MgCl 2 , and/or CaCl 2 , are dissolved in the fluid [55]. The final ice melting temperatures (Tm) of the Type 1 inclusions range between −19.4 and −10.8 • C, indicating a moderate to relatively high salinity of 14.8 to 22 wt.% NaCl equiv. [56]. In type 3 fluid inclusions, Tm range from −16.5 to −12 • C demonstrating moderate to relatively high salinities of 14.4 to 19.8 wt.% NaCl equiv. in the H 2 O-NaCl-KCl system. Type 1 inclusions homogenize (Th) from 382 • to 496 • C ( Figure 8, Table 3), while type 2 inclusions homogenize with the disappearance of the vapor bubble after the disappearance of the solid phases (more commonly halite than sylvite). In rare cases, another unidentified solid phase was observed, which is probably a chloride complex of Mg or Ca. Homogenization temperatures in the Type 2 inclusions range from 381 • to 458 • C (Figure 8, Table 3). Based on the solid phase homogenization temperatures (271-386 • C) and using the data for the system H 2 O-NaCl [56], the salinity of the type 2 inclusions range from 35.7 to 45.6 wt.% NaCl equiv. Type 3 fluid inclusions homogenize at temperatures from 381 • to 504 • C (Figure 8). Homogenization temperatures of the fluid inclusions of 1, 2, and 3 types in the porphyry style mineralization overlap between 380 • and 460 • C, with a distinct maximum at~430 • C (Figure 8).     High-salinity fluid inclusions (type 2) usually coexist with vapor-rich inclusions (type 3) within the same assemblage, demonstrating similar homogenization temperatures (Figures 7b,d and 8). This indicates a simultaneous heterogeneous trapping of two fluids, a saline brine (36-46 wt.% NaCl equiv.) and a low-density vapor-rich fluid with lower salinity (14-22 wt.% NaCl equiv.), which suggests fluids were trapped during boiling [53,56,57]. Fluids along the boiling curve do not require pressure correction; therefore, the homogenization temperatures represent the actual trapping temperatures of the fluid [57].
The initial melting temperatures of ice in the fluid inclusions of the quartz-stibnite epithermal veins vary between −38.7 and −49.9 °C. This indicates that, in addition to NaCl, other salts, such as KCl, MgCl2, and/or CaCl2, were involved in the ore-forming fluid [55]. The final ice melting temperatures of the type 1 inclusions range from −6.9 to −5.0 °C indicating relatively low salinities (7.9 to 10.4 wt.% NaCl equiv.) [56]. Homogenization temperatures vary from 256° to 326 °C, with a maximum at 290 °C (Figure 8). High-salinity fluid inclusions (type 2) usually coexist with vapor-rich inclusions (type 3) within the same assemblage, demonstrating similar homogenization temperatures (Figures 7b,d and 8). This indicates a simultaneous heterogeneous trapping of two fluids, a saline brine (36-46 wt.% NaCl equiv.) and a low-density vapor-rich fluid with lower salinity (14-22 wt.% NaCl equiv.), which suggests fluids were trapped during boiling [53,56,57]. Fluids along the boiling curve do not require pressure correction; therefore, the homogenization temperatures represent the actual trapping temperatures of the fluid [57].
The initial melting temperatures of ice in the fluid inclusions of the quartz-stibnite epithermal veins vary between −38.7 and −49.9 • C. This indicates that, in addition to NaCl, other salts, such as KCl, MgCl 2 , and/or CaCl 2 , were involved in the ore-forming fluid [55]. The final ice melting temperatures of the type 1 inclusions range from −6.9 to −5.0 • C indicating relatively low salinities (7.9 to 10.4 wt.% NaCl equiv.) [56]. Homogenization temperatures vary from 256 • to 326 • C, with a maximum at 290 • C (Figure 8).

Conditions of Formation of the Porphyry Cu-Au Deposit at Gerakario
The porphyry Cu-Au deposit and the epithermal quartz-stibnite veins at Gerakario are related to the emplacement of a syenite intrusion in two-mica gneiss of the Vertiskos unit during the Miocene (22 ± 0.8 Ma; U-Pb zircon ages [42]), in an extensional structural regime. The mineralization shares many similarities in its geotectonic setting, structural control, magma evolution, hydrothermal alteration, and physicochemical parameters of the hydrothermal fluids with the adjacent Vathi porphyry-epithermal system, which is genetically related to a quartz monzonite [32,33].
At Gerakario, the fast ascension of the syenite magma and its crystallization at shallow depths caused exsolution of hydrous fluids and silicate melts that resulted in hydraulic fracturing, increasing the permeability of the host rocks. This mechanism favored the formation of the potassic hydrothermal alteration and the deposition of the Cu-Au mineralization in the A-type veins, along fractures, under boiling conditions. Phase separation was favored by a rapid drop in temperature and pressure in the veins, resulting in a saline brine (36-46 wt.% NaCl equiv.) and a co-existing lower salinity (14-22 wt.% NaCl equiv.) low-density vapor-rich fluid that homogenize over the same temperature range, between 380 • and 460 • C (Figure 9).
According to Brathwaite et al. [58], aqueous fluid inclusions with moderate salinity (up to 20 wt.% NaCl equiv.) represent a fluid extracted from the magma. In this case, the fluid is cooled to conditions between plastic and brittle deformation, creating inclusions enriched in the liquid (Type 1) and vapor phases (Type 3) at Gerakario, with moderate salinity, without forming liquid inclusions with halite [58].
The densities of the hydrothermal fluids at the Gerakario porphyry deposit are >0.90 g.cm −3 for the fluids with high salinity (type 2 fluid inclusions) and <0.78 g.cm −3 for the moderate salinity fluids (type 1 and 3 fluid inclusions). The trapping pressures of the fluid inclusions can be estimated considering that the fluids were trapped under boiling conditions in the system NaCl-KCl-CaCl 2 -H 2 O. Based on homogenization temperatures and the equation of Archer [59], the minimum trapping pressures for type 2 inclusions in A-type quartz veins range from 100 to 350 bar, and for type 3 inclusions from 240 to 580 bar. These pressures indicate a maximum ore formation depth of~2 km under lithostatic conditions.

Genesis and Geochemistry of the Epithermal Quartz-Stibnite Veins at Gerakario
The epithermal veins formed from a fluid of low to moderate salinity (7.9 to 10.4 wt.% NaCl equiv.) with homogenization temperatures ranging mainly from 280 • to 320 • C, with a maximum at 290 • C (Figure 9). This fluid resulted from the mixing of a high to moderate salinity fluid exsolved from the porphyry system, and meteoric water, at the final stage of the magmatic-hydrothermal system in an epithermal environment. Due to the shallow depth of formation of these veins, the pressure correction should be <10 • C (e.g., Bodnar et al. [60]). For this reason, the homogenization temperatures (280-320 • C, with a maximum of 290 • C) correspond to the minimum temperatures of the formation of the epidermal veins. Therefore, for hydrostatic pressures in the range of 65 to 116 bar, a depth of 600 to 1000 m under hydrostatic conditions is proposed for the stibnite mineralization.
Hydrothermal carbonates (e.g., calcite) mainly host REEs in the epithermal systems [21]. In these cases, REE fractionation is dependent upon the composition of the mineralizing fluids and the co-precipitating of other ore, gangue, and alteration minerals [21]. During precipitation of calcite, medium and heavy REEs are preferentially incorporated in its crystal lattice, while light REEs, especially La, are enriched in the residual fluid [21]. Thus, significant contents of La and Ce, and rarely Pr, Nd, and Sm are incorporated in stibnite, which formed after calcite [21]. Leaching of carbonate wall rocks and of rock-forming minerals from the magmatic fluids may introduce REEs to the circulating hydrothermal system [21]. A similar mechanism has been proposed for the REE enrichment detected in the oxidation zone of the adjacent Vathi porphyry Cu-Au±Mo deposit [32] (Figure 1).
In addition, REE incorporation in minerals is related to specific physicochemical factors, including the structure of the lattice and complexation (i.e., the combination of Hydrothermal carbonates (e.g., calcite) mainly host REEs in the epithermal systems [21]. In these cases, REE fractionation is dependent upon the composition of the mineralizing fluids and the co-precipitating of other ore, gangue, and alteration minerals [21]. During precipitation of calcite, medium and heavy REEs are preferentially incorporated in its crystal lattice, while light REEs, especially La, are enriched in the residual fluid [21]. Thus, significant contents of La and Ce, and rarely Pr, Nd, and Sm are incorporated in stibnite, which formed after calcite [21]. Leaching of carbonate wall rocks and of rock-forming minerals from the magmatic fluids may introduce REEs to the circulating hydrothermal system [21]. A similar mechanism has been proposed for the REE enrichment detected in the oxidation zone of the adjacent Vathi porphyry Cu-Au ± Mo deposit [32] (Figure 1).
In addition, REE incorporation in minerals is related to specific physicochemical factors, including the structure of the lattice and complexation (i.e., the combination of individual atom groups, ions or molecules to create one large ion or molecule [61]), as well as sorption and desorption [21]. Magmatic fluids are generally depleted in REEs, while meteoric fluids are slightly enriched in light REEs [62].
The anatomy of the quartz-stibnite veins at Gerakario, the ore assemblage, the bulk geochemistry, and the fluid inclusion study suggest that the ore mineralization was developed from intermediate to low sulfidation hydrothermal fluids, in a fault-induced epithermal stage set at the periphery of the Cu-Au porphyry system. The same could be suggested for all the base metals vein sets found in the vicinity of the Gerakario porphyry system. Epithermal, high to low sulfidation veins are commonly found peripheral to porphyry systems and porphyritic intrusions [19,63]. Epithermal veins are associated with several porphyry deposits in Greece (e.g., Pagoni Rachi, Maronia, Vathi) [24,33,64]. However, the veins in these deposits do not host massive stibnite [24]. Epithermal veins with massive stibnite and realgar are found distal to porphyritic intrusions located at Chios island and the Agia area (Mavrovounio mountain). In those deposits, a zoning proximal to the intrusions containing Sn and Pb-Zn-Cu sulfides was identified by Voudouris et al. [24].

Mineral Chemistry of Stibnite and Nano-Scale Inclusions
The trace elemental study of stibnite by means of LA-ICP-MS needs further development [16]. To our knowledge, this study presents for the first time the mineral chemistry of stibnite from epithermal veins found in the periphery of a porphyry system [16]. Stibnite (Stb1) at Gerakario is enriched in base metals (As, Cu, Pb) and bears weak to moderate contents of critical and rare metals (Ag, Bi, Ce, La, Re, Sm, Th, Ti, Tl) (Table 2, Figure 6). However, it is depleted in Au, Hg, Se, and Te with concentrations below detection limits ( Table 2). The depletion of Hg in stibnite contrasts to the Hg enrichment in stibnite from SE China [16]. In addition, the depletion of Au +1 as solid solutions in stibnite and the presence of native gold in interstices of the quartz-stibnite veins [45] indicate that Au precipitation slightly followed Sb precipitation. Thus, it could be suggested that the precipitation of massive stibnite depleted the H 2 S content of the mineralizing fluids, and enhanced the precipitation of native gold (Au 0 ) in the quartz-epithermal veins [65].
The concentrations of As, Cu, and Pb in stibnite can be attributed to the stoichiometric substitutions of Sb (2Sb 3+ ↔ Cu ++ Pb 2++ As 3+ ), as well as, in some cases, to invisible nanoparticles or to higher incorporation of an element in a specific sector zone, as the LA-ICP-MS depth profiles locally consist of a series of peaks of slightly varying size (Figure 10a,b) [16]. In addition, Cu and Pb exhibit a more consistent distribution in stibnite relatively to the As distribution (  In Stb1, the spiky pattern for As shows the presence of nano-scale inclusions of arsenopyrite in stibnite or that As is incorporated in higher amounts in a specific stibnite sector zone.

Conclusions
The epithermal quartz-stibnite veins of Gerakario are genetically related to a Cu-Au porphyry deposit hosted mainly in a syenite intrusion of Miocene age. Disseminated pyrite and chalcopyrite, and stockworks of A-type veins containing magnetite-pyrite-chalcopyrite, are found in the potassic alteration of the porphyry system. Minor pyrite and chalcopyrite occur as disseminations and in D-type veins in the sericitic alteration. The epithermal quartz veins include stibnite, berthierite, native antimony, pyrite, arsenopyrite, and traces of marcasite, pyrrhotite, chalcopyrite, löllingite, and native gold. Enrichment of these veins in critical and rare metals includes Ag, Au, Bi, Ce, Co, Ga, La, and Sb. The laser ablation ICP-MS analysis of stibnite show elevated concentrations of Figure 10. Selected time-resolved laser ablation ICP-MS depth profiles of stibnite from the epithermal quartz-stibnite veins at Gerakario. (a) In Stb1, the distribution patterns of As, La, Pb, Cu, and Sb are similar, suggesting their affiliation with stibnite. (b) In Stb1, the spiky pattern for As shows the presence of nano-scale inclusions of arsenopyrite in stibnite or that As is incorporated in higher amounts in a specific stibnite sector zone. The depth profile of La exhibits a similar pattern to those of Sb, As, Cu, and Pb (Figure 10a,b). The crystal lattice of stibnite does not include proper sites for REE accommodation, especially for La [21]. Thus, following the suggestions of Wang et al. [21], lanthanum in stibnite at Gerakario may occur in fluid inclusions or in lattice defects. The rest of the critical and rare metals, including Ag, Bi, Ce, Re, Th, Ti, and Tl, which are detected in stibnite, display depth profiles close to background values. Regarding Ce and La contents, possible matrix-derived interferences (i.e., 121 Sb 18 O(±H) for La and Ce) could not be excluded and the distribution of these elements needs further investigation.
The depletion of stibnite in Hg, Se, and Te, and the enrichment in La could suggest that it was deposited during the late stages of the mineralizing events in the porphyryepithermal system at Gerakario. In addition, the other Fe-Cu-Pb-As vein mineralization found in the periphery of the porphyry system [39] (Figure 2), and the enrichment of As, Cu, and Pb in stibnite, indicate the predominance of base metals in the mineralizing fluids related to the epithermal stage.

Conclusions
The epithermal quartz-stibnite veins of Gerakario are genetically related to a Cu-Au porphyry deposit hosted mainly in a syenite intrusion of Miocene age. Disseminated pyrite and chalcopyrite, and stockworks of A-type veins containing magnetite-pyrite-chalcopyrite, are found in the potassic alteration of the porphyry system. Minor pyrite and chalcopyrite occur as disseminations and in D-type veins in the sericitic alteration. The epithermal quartz veins include stibnite, berthierite, native antimony, pyrite, arsenopyrite, and traces of marcasite, pyrrhotite, chalcopyrite, löllingite, and native gold. Enrichment of these veins in critical and rare metals includes Ag, Au, Bi, Ce, Co, Ga, La, and Sb. The laser ablation ICP-MS analysis of stibnite show elevated concentrations of As, Cu, and Pb, and enrichments in Ag, Bi, Ce, La, Re, Sm, Th, Ti, and Tl. Correlation coefficients for the elemental pairs Ce-La, Ce-Sb, and La-Sb in stibnite indicate positive correlations, while the pair Bi-Sb shows a negative correlation. The formation of A-type veins in the potassic alteration of the porphyry system is ascribed to fluid boiling at temperatures between 380 • and 460 • C at a depth <2 km. The epithermal quartz-stibnite veins were deposited under a lower temperature range (280-320 • C) at a depth between 600 and 1000 m.