We present data available on rare metal and indium distributions in cassiterite and associated minerals from thirteen Sn ± W granite-related ore deposits in the western Variscan Belt (Massif Central and Armorican Massif, France; Galicia, Spain; and SW England). Cassiterite and associated minerals including sulfides and titanium oxides were analysed using an electron probe micro-analyzer (EPMA). Significant indium contents were only measured in cassiterite from hydrothermal vein-type mineralizations associated with peraluminous granites of Montbelleux, Abbaretz (French Armorican Massif) and Marcofán (Galicia); they correlate with the highest Nb, Ta and Fe substitutions. Two coupled substitutions are proposed: (1) 2 (Sn4+, Ti4+) ↔ (Fe3+, In3+) + (Nb5+, Ta5+) and (2) Fe2+ + (Nb, Ta)5+ ↔ In3+ + (Ti, Sn)4+ depending on Fe valence state. Sulfides (stannite, chalcopyrite, pyrite, arsenopyrite and sphalerite) and rutile associated with cassiterite contain significant amounts of indium, even when cassiterite is indium-free, suggesting preferential partitioning into the sulfides.
The element indium (In) was discovered by Ferdinand Reich and Theodor Richter in 1863 at the Bergakademie Freiberg in polymetallic Ag-base metal ores of the local Freiberg district (Erzgebirge, Germany) with a spectrograph (Seifert & Sandmann, 2006). Indium is a chalcophile element used in industry for its semiconductor and optoelectronic performance. Due to its softness, In alloys can be plated onto metal or evaporated onto glass in a variety of high-tech applications, including screens and monitors, infrared detectors, high-speed transistors, diodes, and photovoltaics. Indium is present as traces in the Earth’s crust, but does not form primary ore deposits, and is currently extracted as a by-product of Zn, Sn and Cu deposits (Werner et al., 2017). The growing use of In in high-tech applications and a restricted supply dependent on only a few present-day producers (e.g., China, Korea, Japan, Canada, Zhang et al., 2015) created challenges to In sourcing worldwide (EU Commission, 2014; Werner et al., 2017).
During the two last decades, mineralogical studies of ore deposits in numerous countries have shown that In is a dispersed element present in various deposit types (Schwartz-Schampera & Herzig, 2002; Schwarz-Schampera, 2014; Werner et al., 2017) and usually shared between several mineral phases (e.g., Pavlova et al., 2015; Andersen et al., 2016; Frenzel et al., 2016; George et al., 2016; Werner et al., 2017). Eighteen In minerals are currently identified, among them, roquesite, petrukite, sakuraiite, indite, laforêtite, dzhalindite (Andersen et al., 2016). In many In-rich deposits, the In minerals are not abundant or even absent. The Kawazu Au–Ag–Cu–Mn–Te epithermal ore deposit in Japan is an exception. Roquesite and dzhalindite are its main ores (Shimizu et al., 2008). In other In-rich deposits, the element is instead substituted in a wide variety of minerals, including base-metal sulfides (Fe-rich sphalerite), copper sulfides (chalcopyrite, bornite), copper-tin sulfides (chalcostannate group, stannite), tin oxides (cassiterite) (e.g., Seifert & Sandmann, 2006; Cook et al., 2009, 2011a, b, c; Dill et al., 2013; Pavlova et al., 2015; Andersen et al., 2016; George et al., 2016; Frenzel et al., 2016; Valkama et al., 2016);at this time sphalerite represents about 95% of global In production. The major In-rich deposits are, by decreasing order of importance, sediment-hosted massive sulfides, volcanogenic massive sulfides (VMS), skarn, epithermal, and porphyry; sediment-hosted Pb–Zn and VMS represent more than 60% of In resources (Werner et al., 2017). Magmatic-hydrothermal mineralizations mostly associated with post-collisional magmatic pulses, including skarn-, greisen-, and vein-type mineralization, also represent promising exploration targets for In (SE Finland; Erzgebirge/Krušné Hory; Far East Russia; SW England; South China Tin Belt) (Seifert, 2008; Cook et al., 2011c; Pavlova et al., 2015; Seifert et al., 2015; Andersen et al., 2016; Valkama et al., 2016).
The Variscan Belt contains several ore deposits identified for their significant In resources (Werner et al., 2017), including VMS in Portugal such as Neves Corvo (Pinto et al., 2014) or Lagoa Salgada (Figueiredo et al., 2012), different ore-deposit types in the Erzgebirge, eastern Germany (skarn-type ores in the Pöhla district: Schuppan & Hiller, 2012; Bauer et al., 2017; Jeske & Seifert, 2017), polymetallic Sn(-Ag)-base metal vein- and greisen-type deposits in the old Freiberg, Marienberg, Annaberg, and Ehrenfriederdorf-Geyer mining districts (Seifert et al., 1992; Jung & Seifert, 1996; Seifert & Sandmann, 2006; Seifert, 2015) and Sn deposits in SW England (Andersen et al., 2016). According to these recent investigations, late-Variscan granite-related Sn mineralizations might also represent potential interesting In targets.
Three topics of interest are (1) substitutions of In and other minor and trace elements, such as, Fe, Ti, Nb, Ta and W in the cassiterite lattice, (2) the In distribution among cassiterite and associated minerals, and (3) the trace element content in cassiterite, and more specifically the In content, in terms of ore deposit type.
2. Metallogeny in the Variscan Belt, samples and deposits
The European Variscides, extending from the Iberian Peninsula to Sudetic Mountains, are the result of continental collision between Gondwana and Laurussia. This collision caused the development of a polyphased orogeny, lasting more than 100 Ma from the Early Devonian to the Early Permian, and comprising three major successive stages (e.g., Faure et al., 2009; Maierová et al., 2016) of metallogenesis (Marignac & Cuney, 1999). The first stage of the Variscan orogeny (Early Devonian-Early Carboniferous) corresponds to the closure of Rheic Ocean followed by continental subduction. It is during this stage that sediment-hosted Pb–Zn and VMS were deposited (e.g., Lescuyer et al., 1998; Marignac & Cuney, 1999). The second stage (Mississippian) corresponds to the Variscan continental collision. The third stage of the Variscan Belt (Pennsylvanian to Lower Permian) is a syn-to post-orogenic collapse, marked by normal faults, development of granulite metamorphism of the lower crust and emplacement of granites (cf. Williamson et al., 1996; Seifert, 2008; Simons et al., 2016). Most of the magmatic-hydrothermal rare-metal mineralizations and hydrothermal W, Sn, Sn–F(Li) sulfide mineralizations are associated with the emplacement of peraluminous granites and rare-metal granites of this stage (e.g., Marignac & Cuney, 1999; Bouchot et al., 2005).
Samples of cassiterite-bearing ores were selected from twelve Late Variscan and the only Ordovician granite-hosted Sn mineralizations/deposits in the Armorican Massif and Massif Central (France), in Galicia (NW-Spain), and in SW England (Table 1; Fig. 1). In the French Armorican Massif, Sn ± W ore deposits were exploited for Sn (Abbaretz, Saint Renan, La Villeder) and for Sn + W (Montbelleux, Chauris & Marcoux, 1994). The Sn deposits La Villeder and Abbaretz are related to the Variscan leucogranites of the South Armorican zone belonging to the ilmenite serie (Chauris & Marcoux, 1994). Mineralization occurs as quartz − cassiterite ± sulfide veins associated with tourmaline + muscovite + beryl + apatite + albite ± fluorine hydrothermal alteration. At the Sn deposit La Villeder, metre-thick ore veins are hosted by the Lizio leucogranite at its periphery in contact with an Ediacarian metapelitic schist. The density of the ore veins increases toward the contact of the granite with schist. At the Abbaretz Sn deposit, low-angle quartz-veins are associated with the cupola of the Nozay leucogranite in contact with the schist of low metamorphic grade. The Saint Renan Sn deposit is located in the Leon block (Faure et al., 2008), a specific geodynamic domain, where late Hercynian intrusives are polyphased (two-mica potassic granite, locally injected by a leucogranite of probable Permian age). Mineralization occurs as wolframite–quartz veins with minor cassiterite and well-developed metagranite-greisen ore bodies in the northern part of the Saint Renan Massif (Chauris & Marcoux, 1994). Hydrothermal alteration is essentially represented by tourmalinization and muscovitization. Scheelite (but no cassiterite or wolframite) has been found in the porphyritic granite of the central part and in the fine-grained granite of the southern part. The Montbelleux district is different from the other Sn–W mineralizations by its Ordovician age (Chauris & Marcoux, 1994). Mineralization occurs as quartz–cassiterite–wolframite stockwork in a sodic granite and quartz–wolframite veins in schist near the granite contact (Chauris et al., 1989). The stockwork ore type also contains minor stannite, molybdenite, chalcopyrite, arsenopyrite and sphalerite.
The studied Sn deposits of the French Massif Central are a Cu–Sn–Fe ore deposit (Charrier), W(-Sn) ore deposits (Vaulry, Chataigneraie district) and rare-metal ore deposits disseminated within the rare-metal granites (as defined by Černý et al., 2005) of Beauvoir and Montebras. Charrier is a complex ore deposit (Picot & Pierrot, 1963), which is composed of: (1) Cu orebodies hosted by Devonian metasediments and metavolcanics in contact with microgranite; the massive sulfide ores consist of chalcopyrite, and bornite with inclusions of roquesite, sphalerite, wittichenite, tennantite–tetrahedrite; and (2) magnetite–cassiterite–lepidomelane orebodies hosted by metabasalts near the contact with the La Burnolle granite; molybdenite, scheelite, bismuthinite, native bismuth and pyrite are also present.
At Vaulry (northwestern Massif Central), the W–(Sn–Cu) mineralization is hosted by the 310 Ma Li–F-rich Blond rare-metal leucogranite close to its contact with Paleozoic schists (Boulandon, 1989). The Vaulry deposit is characterized by subvertical ore veins, which show three major stages (Vallance et al., 2001): (I) a stage of barren quartz; (II) infill of small fractures by younger quartz, cassiterite and wolframite, and (III) late microcracks infilled with loellingite, chalcopyrite, and pyrite. Stannite, stannoidite, arsenopyrite, bornite with inclusions of roquesite, mawsonite, scheelite, luzonite and molybdenite were also described (Cantinolle et al., 1985; Boulandon, 1989).
The W ± Sn ore deposits of the Chataigneraie district have limited economic potential for W (30 000 t of known WO3 production distributed across eight deposits; Béziat & Bornuat, 1995), but are not economic for their Sn content. The Sn mineralization is hosted by metamorphic schists in the vicinity of large monzogranites and leucogranitic stocks related to W mineralization at 305 Ma (Lerouge & Bouchot, 2005; Lerouge et al., 2000, 2007). It occurs as late magmatic cassiterite in leucogranite stocks (Entraygues leucogranite) and as hydrothermal cassiterite associated with tourmaline, sulfides and rutile, disseminated in biotite–muscovite–chlorite quartz-rich schist (Le Prunet, Entraygues schist). Typically, sulfides essentially consist of chalcopyrite, sphalerite, arsenopyrite and minor pyrite. The magmatic rare-metal (Sn, Ta, Nb, Be, Li) deposits of Beauvoir and Montebras in northwestern Massif Central are economic (Cuney et al., 1992; Raimbault et al., 1995). The Sn mineralization consists of dominantly disseminated post-magmatic cassiterite associated with a magmatic-hydrothermal paragenesis: lepidolite, topaz, columbo-tantalite, and amblygonite formed at around 570 ± 50 °C (Fouillac & Rossi, 1991). It is hosted by high-phosphorus, peraluminous small albite–lepidolite granitic stocks emplaced between 317 ± 6 Ma for the Beauvoir granite and 314 ± 4 Ma for the Montebras granite (U/Pb columbite-tantalite, Melleton et al., 2015).
The Sn-bearing deposits in central Galicia, NW Spain, are of several types, disseminated within LCT pegmatites or in quartz veins associated with granite intrusions in a district where intrusion-related gold deposits also occur (e. g., Gloaguen et al., 2014). Tin-W ore deposits (Mina Vella mine – Marcofán, Mina Soriana mine – Magros) are located on the eastern side of the late-Variscan Beariz granite (Gloaguen, 2006; Sizaret et al., 2009). Mineralization occurs in N060°E-trending large normal-faulting quartz veins emplaced both in granite and surrounding micaschist. Large hydrothermal alteration zones occur in micaschist as massive tourmalinite haloes closely related to intrusive bodies and quartz veins. Both cassiterite and wolframite occur in the first mineral assemblage that comprises the infill of quartz veins. Marcofán is essentially hosted by granite, whereas Magros consists of veins hosted by schist.
The Saint Agnes Sn–W ore deposit is hosted by a small peraluminous granitic stock associated with the post-Variscan Cornubian Batholith outcropping in SW England (Andersen et al., 2016; Simons et al., 2016). The mineralization consists of quartz–tourmaline–cassiterite–wolframite–chalcopyrite–stannite–sphalerite–löllingite–arsenopyrite veins associated with greisen developed in the apical part of the granitic stock. The greisen alteration minerals include topaz, beryl, apatite and fluorite (Andersen et al., 2016). Textural relationships provide evidence of a high-temperature cassiterite–wolframite ± arsenopyrite–quartz–tourmaline stage followed by arsenopyrite–chalcopyrite with minor stannite stage (Andersen et al., 2016). Roquesite was described in different ore deposits of the Cornwall district (Andersen et al., 2016).
3. Analytical techniques
Images in cathodoluminescence have been acquired on a MIRA 3 XMU (TESCAN, Brno, Czech Republic) equipped with a panchromatic cathodoluminescence detector (350–650 nm) (TESCAN BSE/CL detector) under a low vacuum mode (P = 20 Pa nitrogen).
Analyses of cassiterite and sulfides were performed at the BRGM using a Cameca SX50 EPMA with an accelerating voltage of 20 kV. The spot size was ∼1 μm. The system was calibrated with a variety of synthetic oxides and pure elements. Matrix corrections were made with the phi-rho-Z computing program PAP (Pouchou & Pichoir, 1984).
Tin and trace elements in cassiterite were analysed with a beam current of 150 nA. Ti–Kα, Sn–Lα, In–Lα/β, Nb–Lα were measured on PET, Fe–Kα on LiF and Ta–Mα/β, W–Lα on TAP. Counting times on peak and background were 10 s for Ti and Fe, and 40 s for other elements. Standards of calibration were natural minerals (cassiterite for Sn, roquesite for In), synthetic oxides (MnTiO3 for Ti, Fe2O3 for Fe), and pure elements (Nb, Ta and W). Detection of In and Ta in cassiterite is complicated because of interference between the Sn X-ray emission lines and those of In and Ta during EPMA-WDS analyses. The major Lα line of In (Fig. S1a and b in Supplementary Material, linked to this article and freely available online at the GSW website of the journal: http://eujmin.geoscienceworld.org) and the major Mα line of Ta (Fig. S1d) interfere with the positions of the Lη and the Lα2nd order lines of Sn, respectively. The contributions of the Sn X-rays to In-Lα and Ta-Mα were approximated by analysis of In-free and Ta-free cassiterite and of Sn metal at around 1400 ppm for In and 3000 ppm for Ta. The contribution of the Sn X-ray to the In-Lα is a value similar to that estimated by Benzaazoua et al. (2003). To avoid interference with Sn X-rays, In and Ta were measured on the second major In-Lβ and Ta-Mβ even though their intensities are lower than the intensities of the In-Lα and Ta-Mα (Fig. S1c and d). The In-Lβ/In-Lα intensity ratio is 0.45. The detection limits of the elements are (in ppm): 218 (Ti), 369 (Fe), 238 (Sn), 77 (Sc), 184 (Ta), 144 (Mn), 253 (In), 208 (W) and 313 (Nb).
Elemental mapping of Sn (Sn-Lα), Ta (Ta-Lα), Nb (Nb-Lα), Fe (Fe-Kα), Ti (Ti-Kα), and In (In-Lβ) in cassiterite were performed on a CAMECA SXFive-FE electron microprobe equipped with a Schottky Field-Emission Gun (FEG) (CAMECA, Gennevilliers – France), using an acceleration voltage of 20 kV and beam current of 200 nA.
Sulfides were analyzed for major and trace elements (S, Cu, Fe, Sn, As, Cd, Zn, In), using a beam current of 20 nA and counting time of 40 s for each element. Standards of calibration were natural minerals (pyrite for Fe, galena for S, sphalerite for Zn, cassiterite for Sn, roquesite for In), synthetic oxides (MnTiO3 for Ti, Fe2O3 for Fe), pure elements (Cu) and AsGa (As). The Cd-Lα, In-Lα, S-Kα and Sn-Lα lines were measured on PET, Cu-Kα, Fe-Kα, Zn-Kα on LiF, and W-Lα, As-Lα on TAP. The detection limits of the elements were (in ppm): 281 (Cu), 178 (Fe), 494 (Sn), 438 (As), 294 (Cd), 293 (Zn), and 306 (In).
4. Ore-mineral composition
Cassiterite from Saint Agnes is quite pure and only contains traces of Fe and W; it will not be discussed further. Iron is absent or present in small amounts in cassiterite from Beauvoir and Montebras, Magros and Marcofán. Iron is present in significant concentrations in cassiterite from other mineralizations. Considerable concentrations of Nb are present in cassiterite from Abbaretz (1082 ppm), Montbelleux (3901 ppm), Beauvoir (1764 ppm) and Vaulry (590 ppm), and in two samples from Marcofán (#1: 620 ppm; #13: 880 ppm). Tantalum and Ti are both significant trace elements in cassiterite from all the mineralizations, with Ti contents ranging between 326 ppm (Beauvoir) and 4494 ppm (Entraygues) and Ta contents ranging between 393 (Le Prunet) and 5809 ppm (Montbelleux).
4.2. Chemical composition of sulfides
A limited number of EPMA analyses were performed on sulfides that are associated with cassiterite in the thin sections from five Sn ore deposits (Table 3). Chalcopyrite, pyrite and sphalerite in the cassiterite–sulfide dissemination of Entraygues show In contents up to 940 ppm, 930 ppm and 520 ppm respectively. Sphalerite is also characterized by a homogeneous Cd content ∼5200 ppm. Chalcopyrite and bornite in the Sn-polymetallic deposit of Charrier show average In contents of ∼800 ppm and ∼430 ppm, respectively. Chalcopyrite, stannite (Cu2FeSnS4) and pyrite from the Marcofán Sn deposit have significant In contents (up to 1220 ppm, 620 ppm and 1540 ppm, respectively), whereas sphalerite shows very low In and high Cd (1.5 wt%) contents. Chalcopyrite (up to 450 ppm), arsenopyrite (up to 640 ppm) and pyrite (up to 740 ppm) from the Magros Sn deposit have lower In contents than sulfides from Marcofán. Chalcopyrite and stannite from the Saint Agnes Sn deposit are characterized by high average In contents of 1560 ppm and 2590 ppm, respectively.
5.1. Incorporation of trace elements in the cassiterite lattice
To conclude, two ideal coupled substitutions (1) Fe2+ + 2 (Nb, Ta)5+ ↔ 3 (Sn, Ti)4+, and (2) Fe3+ + (Nb, Ta)5+ ↔ 2 (Sn, Ti)4+ are at least possible for incorporation of Nb and Ta in the cassiterite studied. That has several implications: (1) incorporation will remain low in Fe-poor cassiterite, (2) incorporation will be limited by the formation of tantalite minerals, and (2) incorporation will highly depend on the Fe valence, and consequently on the redox condition in the system.
In regard to In incorporation in cassiterite, homogeneous spot values and mapping of Montbelleux cassiterite indicate that In is in the cassiterite lattice. Assuming that In is present as In3+ in the crust (Smith et al., 1978), and that the electroneutrality of the crystal needs to be maintained, In incorporation may follow the coupled substitution 1: (Fe, In)3+ + (Nb, Ta)5+ ↔ 2 (Sn, Ti)4+. Incorporation of In3+ in cassiterite via coupled substitution (2) could be possible by modifying the exchange vector as follows: Fe2+ + (Nb, Ta)5+ ↔ In3+ + (Ti, Sn)4+.
5.2. Distribution of In in mineral parageneses
Among the studied deposits, the In mineral roquesite is present at the Sn deposits Charrier, Vaulry and Saint Agnes. In these three deposits, cassiterite shows very low In contents. At the Charrier deposit, the order of In distribution in Zn-poor Cu–Sn ore is discrete roquesite, followed by sphalerite (0.8 wt%), chalcopyrite (800 ppm) and bornite (430 ppm). At Saint Agnes, the In distribution in the studied sample is discrete roquesite followed by stannite (2190 ppm) and chalcopyrite (1565 ppm), in good agreement with Andersen et al. (2016).
Cassiterite contains In in only three of the thirteen ore deposits studied: Montbelleux (519 ± 204 ppm), Abbaretz (up to 420 ppm) and Marcofán (up to 580 ppm). Indium contents measured in those cassiterites are consistent with literature data (Briskey, 2005; Pavlova et al., 2015). No sulfides were observed in samples from Montbelleux and Abbaretz. In the Marcofán ore deposit, cassiterite contains In in sulfide-bearing samples (#1: up to 400 ppm, #13: up to 578 ppm); this has already been described by Pavlova et al. (2015). The In distribution in Zn-poor Sn–Cu ore of the Marcofán Sn deposit is chalcopyrite (150–730 ppm), followed by cassiterite (150–270 ppm) and stannite (140 ppm).
In other ore samples containing sulfides (Magros and cassiterite–sulfide dissemination of Entraygues), no In mineral is observed and few analyses of cassiterite have detectable In contents, whereas associated sulfides and rutile (when it is analysed) contain In.
The comparative In contents of the different phases from each ore deposit confirm that chalcopyrite, bornite, stannite, pyrite, arsenopyrite, rutile can also contain In. In the studied Sn ore deposits, ores are Zn-poor and Cu-rich, and they are of interest because of the high average In contents in Cu-sulfides: chalcopyrite (up to 2780 ppm); stannite (up to 2670 ppm); bornite (up to 670 ppm).
5.3. Trace element contents in cassiterite and ore deposit type
Mineralizations of the Sn deposits Montebras and Beauvoir consist of magmatic cassiterite disseminated in rare-metal (Sn, Ta, Nb, Be, Li) granites (Černý et al., 2005). Mineralizations of the other Sn deposits of this study are dominantly hydrothermal vein-type (except the mineralizations of Le Prunet and Entraygues schists, which are disseminated in schists) and spatially associated with late Variscan peraluminous granites. These granites result from partial melting of the crust and fractional crystallisation (Cornwall: Simons et al., 2016; French Armorican Massif: Bernard-Griffiths et al., 1985; Chauris & Marcoux, 1994; Tartèse & Boulvais, 2010; Galicia: Gloaguen, 2006; French MassifCentral:Williamson et al., 1996). Partial melting was initiated by increased crustal temperature and by F–Li–P fluids derived from granulite metamorphism of the lower crust in relation with processes of underplating of mantle magmas (cf. Williamson et al., 1996; Seifert, 2008; Simons et al., 2016).
Even though Sn hydrothermal mineralizations are spatially associated with granites, they are not systematically genetically linked to them (Marignac & Cuney, 1999; Vallance et al., 2001). Case studies of mineralizations provided evidence of a genetic link between mineralizations and peraluminous granites in La Chataigneraie district French Massif Central (Lerouge et al., 2007), in the Beariz district, Galicia (Gloaguen et al., 2014), in Saint Agnes, SW England (Andersen et al., 2016), and in the South Armorican Massif (Chauris & Marcoux, 1994).
In the Sn deposits studied here, two types of cassiterite may be distinguished according to their trace element (Fe, Ti, Nb, Ta) contents. The first population of cassiterite, which is Fe–Ti-rich and Nb–Ta-poor, mostly corresponds to hydrothermal mineralizations hosted by pelitic schists (Entraygues schists, Le Prunet), metabasalts (Charrier) or granite not genetically linked to mineralizations (Vaulry, Vallance et al., 2001). The second population, which is Nb–Ta-rich, corresponds to magmatic mineralizations disseminated in rare-metal granites (Beauvoir and Montebras) and to hydrothermal vein-type mineralisations genetically associated with peraluminous granites and hosted by both granite and pelitic schists (Marcofán and Magros in the Beariz district, Galicia; Abbaretz and LaVilleder, South Armorican Massif; Ordovician Montbelleux). Reported in a binary Fe vs. Nb+Ta diagram, analyses of hydrothermal Fe–Ti-rich and Nb−Ta-poor cassiterites plot in the field of hydrothermal cassiterite of Tindle & Breaks (1998) (Fig. 4f). Analyses of magmatic-hydrothermal Nb−Ta-rich cassiterites associated with rare-metal granites (Beauvoir, Montebras) plot in the field of rare-element granites and pegmatites of Tindle & Breaks (1998). On the contrary, analyses of hydrothermal Nb−Ta-rich cassiterites from Montbelleux, Marcofán, Magros, Abbaretz and La Villeder plot in the field of rare-element granites and pegmatites, rather than in the hydrothermal field. Thus the field of rare-element granites and pegmatites defined by Tindle & Breaks (1998) is not so restrictive and would rather correspond to cassiterites that show the coupled substitutions (1) Fe2+ + 2 (Nb, Ta)5+ ↔ 3 (Sn, Ti)4+ and (2) Fe3+ + (Nb, Ta)5++↔ 2 (Sn, Ti)4+.
It is also noteworthy that the Nb−Ta contents of hydrothermal cassiterites are lower in the Sn deposit La Villeder (granite/schist-hosted) than in the Sn deposit Abbaretz (schist-hosted), although the Sn mineralizations are considered to be associated with the same types of granite. In the La Chataigneraie district, hydrothermal Fe−Ti-rich and Nb−Ta-poor cassiterites disseminated in schists (Le Prunet, Entraygues) and Nb−Ta-rich magmatic cassiterite in the Entraygues leucogranite derived both from magmatic fluids (Lerouge et al., 2007). These chemical variations of cassiterite from the different granite-related hydrothermal Sn mineralisations probably reflect the complex processes of Sn-ore deposition, including chemical heterogeneities of the peraluminous magmas (due to, e.g., different degrees of partial melting, fractional crystallisation, different sediment sources), but also interactions of magma-derived fluids with various host-rocks (various compositions, P–T conditions) and mixing of magma-derived fluids with external fluids (meteoric, metamorphic) (Lehmann, 1990; Linnen & Cuney, 2005).
On this basis, the Fe vs. Nb+Ta diagram of Tindle & Breaks (1998) could be interesting to efficiently target hydrothermal Nb−Ta-rich cassiterites, which have a favourable chemistry for In incorporation in the cassiterite lattice.
The purpose of this work was to evaluate the distribution of In within Sn-polymetallic mineralizations in the western Variscan Belt, to discuss criteria favouring the presence of In within cassiterite, and to determine how In may be substituted. The EPMA analyses of cassiterite from the twelve Variscan Sn-polymetallic ore deposits and from the Ordovician Sn–W ore deposit of Montbelleux provide evidence of low substitution of Sn by Ti, Fe, Nb, Ta and In, highly dependent on ore type, magmatic processes, host rock, fluid/rock interaction processes, and fluid mixing. The highest Ti and Fe substitutions in cassiterite are observed in ores hosted by metapelitic schists. The highest Nb and Ta substitutions in cassiterite are observed in magmatic ores associated with rare-metal granites and in hydrothermal vein-type mineralizations genetically linked with peraluminous granites (Montbelleux, Marcofán and Abbaretz). The significant In content in hydrothermal cassiterites from Montbelleux, Marcofán and Abbaretz correlates with the highest levels of Nb, Ta and Fe substitution, allowing two coupled substitutions to be proposed: (1) 2 (Sn4+, Ti4+) ↔ (Fe3+, In3+) + (Nb5+, Ta5+) and (2) Fe2+ +(Nb, Ta)5+ ↔ In3+ + (Ti, Sn)4+, depending on the Fe valence. These substitutions may be limited by the co-formation of tantalite or other Ta-bearing minerals. Further micro-X-ray fluorescence spectrometry coupled with micro-X-ray diffraction and near-edge X-ray absorption fine structure (XANES) measurements at the Fe K-edge could be of major interest to further constrain substitution mechanisms and Fe valency, and the consequence of these substitutions on the cassiterite lattice. In all deposit types, sulfides are the dominant In carriers, notably stannite (up to 3000 ppm In), chalcopyrite (up to 2800 ppm In), pyrite (up to 1490 ppm In), sphalerite (up to 700 ppm In) and arsenopyrite (up to 740 ppm In). Interestingly, other oxides host In, notably rutile (up to 1100 ppm In).
Zdeněk Johan was a high-level scientist in Mineralogy and Metallogeny, then Research Manager at BRGM for many years (1969–2000).Heworked on geological processes associated to the formation of ore deposits, and specially on the metallogenesis of granite-related Sn and W. He published several papers on indium in sphalerite. The first author has had the privilege and the honour to work with him and his wife Věra. She will not forget their kindness and their passion to transmit and share their knowledge to others. This paper is dedicated to them.
This research has been financially supported by the BRGM Research. We would like to thank Michel Outrequin from Cameca (Genevilliers, France) for the FEG mapping. We are grateful to Dr Karen M. Tkaczyk (McMillan translation) for editing the English text. The Editor in Chief, Professor Reto Gieré, the Guest Associate Editor, Professor Vojtěch Ettler, Professor Thomas Seifert and two anonymous referees are thanked for their constructive comments, which contributed to improvement of the manuscript.