Occurrence

The new mineral was discovered in material from Milan Kvačeḱs research collection originating from the now abandoned Bukov mine, located on the northeastern edge of the village of Bukov, 35 km southeast of Nové Město na Moravě, Vysočina Region, Czech Republic. The GPS coordinates of the type occurrence are 49°27'27.333“N, 16°13'43.224”E.

The Bukov mine is a part of the Rožná–Olší uranium ore district with a total mine production of 23,000 t U in the years 1957–2017 (Kříbek et al., Reference Kříbek, Žák, Dobeš, Leichmann, Pudilová, René, Scharm, Scharmová, Hájek, Holeczy, Hein and Lehmann2009, Reference Kříbek, Knésl, Dobeš, Veselovský, Pořádek, Škoda, Čopjaková, Leichmann and Košek2022). This uranium ore district is an example of shear-zone hosted, late Variscan and post-Variscan hydrothermal mineralisation (Kříbek et al., Reference Kříbek, Žák, Dobeš, Leichmann, Pudilová, René, Scharm, Scharmová, Hájek, Holeczy, Hein and Lehmann2009). Uranium mineralisation is bound to a system of NNW–SSE trending faults and zones of cataclasites, which are hosted in high-grade metamorphic rocks with a Moldanubian Zone of the Bohemian Massif. Mineralised cataclasites are 4–15 m thick and are traceable over a horizontal distance of 15 km. The mineralised zones strike 340–355° and dip WSW at angles of 45–70° (Kříbek et al., Reference Kříbek, Knésl, Dobeš, Veselovský, Pořádek, Škoda, Čopjaková, Leichmann and Košek2022). The host rocks mainly comprise gneisses and amphibolites, with small bodies of calc-silicate gneiss, marble, serpentinite and pyroxenite. The vein and disseminated mineralisation at Rožná comprises (1) pre-uranium quartz–sulfide and carbonate–sulfide mineralisation, (2) uranium, and (3) post-uranium carbonate–quartz–sulfide mineralisation (Kříbek et al., Reference Kříbek, Žák, Dobeš, Leichmann, Pudilová, René, Scharm, Scharmová, Hájek, Holeczy, Hein and Lehmann2009, Reference Kříbek, Knésl, Dobeš, Veselovský, Pořádek, Škoda, Čopjaková, Leichmann and Košek2022). Uranium mineralisation in some carbonate veins is accompanied by selenides, which are generally slightly younger than the main uranium mineralisation (Kříbek et al., Reference Kříbek, Žák, Dobeš, Leichmann, Pudilová, René, Scharm, Scharmová, Hájek, Holeczy, Hein and Lehmann2009). The most significant occurrences of selenides appear in calcite–uraninite veins in the upper levels (5^th to 9th) of the Bukov mine in the underlying rocks of the uranium-bearing shear zone R1. Selenide mineralisation occurs in two distinct types. The first is represented by massive aggregates of predominant berzelianite up to several tens of cm in size, usually in association with Cu sulfides (chalcopyrite, bornite and chalcocite). The second type represents disseminated selenide grains, more rarely tiny veinlets, formed by diverse selenides of often microscopic dimensions (Kvaček, Reference Kvaček1973, Reference Kvaček1979). The full list of minerals (more than 110 species including 20 selenides) recorded from this area is given on https://www.mindat.org/loc-27262.html.

Kvačekite was identified in samples of white calcite gangue in association with nickeltyrrellite–tyrrellite, berzelianite, hakite-(Zn), hakite-(Cd), eucairite, clausthalite and gold.

Experimental procedures

The small size of kvačekite grains and its intergrowths with other minerals prevented its extraction and isolation in an amount sufficient for the relevant crystallographic and structural investigations. Therefore, these measurements were performed on synthetic NiSbSe.

The synthetic NiSbSe phase was prepared using an evacuated silica glass tube method in the Laboratory of Experimental Mineralogy of the Czech Geological Survey in Prague. Nickel (99.999%), antimony (99.999%) and selenium (99.9999%) were used as starting materials for synthesis. The evacuated tube with its charge was sealed and annealed at 800°C. After cooling by a cold-water bath, the charge was ground into powder in acetone using an agate mortar and pestle, and thoroughly mixed to homogenise. The pulverised charge was sealed in an evacuated silica-glass tube again, and heated at 300°C for 3 months. The experimental product was then rapidly quenched in cold water. The size of obtained NiSbSe grains ranges from 2 to 20 μm.

Physical and optical properties

Kvačekite occurs as anhedral grains up to 15 μm in size (Fig. 1), but usually only 2–5 μm across, in nickeltyrrellite, usually intergrown with hakite-(Zn) or clausthalite. Synthetic kvačekite is greyish white in colour with a grey streak and opaque in transmitted light; it has a metallic lustre. A cleavage was not observed; it is brittle with a conchoidal fracture. The calculated density for the empirical formula (Z = 4) is 7.607 g.cm^–3. Mohs hardness is assumed to be 5–6, in agreement with other members of the cobaltite group. In reflected light, kvačekite is white with a faint yellowish shade; bireflectance, pleochroism and anisotropy are absent. Internal reflections were not observed. Reflectance spectra for kvačekite and synthetic NiSbSe were measured in air with a TIDAS MSP400 spectrophotometer attached to a Leica microscope (100× objective) using a WTiC (Zeiss No. 370) standard, with a square sample measurement field of ca. 4 × 4 μm. The results for the 400–700 nm range are given in Table 1 and plotted in Fig. 2.

Figure 1.

Kvačekite from Bukov: (a) reflected light image of kvačekite (white) associated with nickeltyrrellite (yellowish brown) and berzelianite (greenish blue); (b) back-scattered electron image (BSE) of kvačekite (white), nickeltyrrellite (light grey) and berzelianite (dark grey, zonal due to SeS_–1 substitution). Holotype sample P1P 26/2023.

Table 1.

Reflectance values (%) for kvačekite and synthetic NiSbSe.^a

^a The reference wavelengths required by the Commission on Ore Mineralogy (COM) are given in bold.

Figure 2.

Reflectance curve for kvačekite from Bukov compared with data for synthetic NiSbSe.

Chemical composition

Chemical analyses of kvačekite from Bukov and synthetic NiSbSe were performed using a Cameca SX100 electron microprobe operating in wavelength-dispersive mode (25 kV, 20 nA and 0.7 μm beam size). The following standards and X-ray lines were used to minimise line overlaps: Ag (AgLα), Au (AuMα), Bi₂Se₃ (BiMβ), CdTe (CdLα), chalcopyrite (CuKα and SKα), Co (CoKα), GaAs (GaLα), Ge (GeLα), HgTe (HgMα), Mo (MoLα), Ni (NiKα), NiAs (AsLβ), PbS (PbMα), PbSe (SeLβ), PbTe (TeLα), pyrite (FeKα), Sb₂S₃ (SbLα), Sn (SnLα), Tl(Br,I) (TlLα) and ZnS (ZnKα). Peak counting times were 20 s for all elements, and 10 s for each background. Arsenic, Ag, Au, Bi, Cd, Fe, Ga, Ge, Hg, Mo, Pb, Sn, Te, Tl and Zn were all found to be below the detection limits (0.02–0.15 wt.%). Raw intensities were converted to the concentrations of elements using the automatic ‘PAP’ (Pouchou and Pichoir, Reference Pouchou, Pichoir and Armstrong1985) matrix-correction procedure.

Analytical data for kvačekite from Bukov (17 analyses) and synthetic NiSbSe (6 analyses) are given in Table 2. On the basis of 3 atoms per formula unit (apfu), the empirical chemical formula of kvačekite is (Ni_0.95Cu_0.04Co_0.03)_Σ1.02Sb_1.00(Se_0.97S_0.01)_Σ0.98 and Ni_1.00Sb_1.02Se_0.98 for synthetic NiSbSe. The ideal formula is NiSbSe, which requires Ni 22.63, Sb 46.93 and Se 30.44, a total of 100.00 wt.%.

Table 2.

EPMA chemical data (wt.%) for kvačekite from Bukov and synthetic NiSbSe.

(σ) – estimated standard deviation; n = number of spot analyses.

Raman spectroscopy

The Raman spectra of kvačekite from Bukov and synthetic NiSbSe were collected in the range 40–4000 cm^–1 using a DXR dispersive Raman Spectrometer (Thermo Scientific) mounted on a confocal Olympus microscope. The Raman signal was excited by an unpolarised green 532 nm solid state, diode pumped laser and detected by a CCD detector. The experimental parameters were: 100× objective, 10 s exposure time, 100 exposures, 50 μm slit spectrograph aperture and 1.5 mW laser power level. The eventual thermal damage of the measured points was excluded by visual inspection of the excited surface after measurement, by observation of possible decay of spectral features in the start of excitation and checking for thermal downshift of Raman lines. The instrument was set up by a software-controlled calibration procedure using multiple neon emission lines (wavelength calibration), multiple polystyrene Raman bands (laser frequency calibration) and standardised white-light sources (intensity calibration). Spectral manipulations were performed using the Omnic 9 software (Thermo Scientific). The Raman bands of kvačekite appear only in the area 250–40 cm^–1, the observed main bands at 199, 179 and 146 cm^–1, with weak to moderate intensity bands at 127, 102, 87, 68, 57 and 45 cm^–1 corresponding very well with Raman bands of synthetic NiSbSe (Fig. 3). Strong bands in the area 250–120 cm^–1 and medium intensity bands in the range 120–70 cm^–1 can be assigned to stretching and bending vibrations of Sb(Ni)–Se bonds. Weak Raman bands below 70 cm^–1 should be connected with external modes – translations and librations (Škácha et al., Reference Škácha, Buixaderas, Plášil, Sejkora, Goliáš and Vlček2014; Sejkora et al., Reference Sejkora, Buixaderas, Škácha and Plášil2018).

Figure 3.

Raman spectra of kvačekite from Bukov and synthetic NiSbSe.

X-ray diffraction data

The small size of natural kvačekite prevented its extraction and direct investigation by means of X-ray diffraction. Therefore, powder X-ray diffraction data were collected on the synthetic phase NiSbSe at room temperature using a Bruker D8 Advance diffractometer equipped with a solid-state LynxEye detector and secondary monochromator producing CuKα radiation, housed at the Department of Mineralogy and Petrology, National Museum, Prague, Czech Republic. The instrument was operating at 40 kV and 40 mA. In order to minimise the background, the powder was placed on the surface of a flat silicon wafer. The powder pattern was collected in the Bragg–Brentano geometry in the range 3–75°2θ, step size 0.01° and counting time of 20 s per step. The positions and intensities of diffractions were found and refined using the Pearson VII profile-shape function of the ZDS program package (Ondruš, Reference Ondruš1993). The obtained experimental data correspond well with the powder X-ray diffraction pattern (Table 3) calculated using the software PowderCell2.3 (Kraus and Nolze, Reference Kraus and Nolze1996) on the basis of our structural model of NiSbSe. The unit-cell parameters for cubic space group P2₁3 (# 198) were refined by the least-squares program of Burnham (Reference Burnham1962) as follows: a = 6.09013(13) Å, V = 225.881(15) ų and Z = 4. The refined unit-cell parameters agree very well with data a = 6.0868(6) Å (Foecker and Jeitschko, Reference Foecker and Jeitschko2001) and a = 6.090(3) Å (Hulliger, Reference Hulliger1963) given for synthetic NiSbSe.

Table 3.

Experimental powder X-ray diffraction data for the synthetic analogue of kvačekite (NiSbSe).

Intensity and d _hkl (in Å) were calculated using the software PowderCell2.3 (Kraus and Nolze, Reference Kraus and Nolze1996) on the basis of our refined structural model. Only reflections with I _calc > 0.5 are listed. The six strongest reflections are given in bold.

Crystal structure

The source data for Rietveld refinement of the synthetic phase NiSbSe were collected at room temperature using a Bruker D8 Advance diffractometer equipped with LynxEye XE detector and CuKα radiation (Czech Geological Survey, Prague). The instrument was operated at 40 kV and 30 mA. In order to minimise the background, the powder was placed on the surface of a flat silicon wafer. The powder pattern was collected in the Bragg–Brentano geometry in the range 10–140°2θ, step 0.015° and counting time of 1.4 s per step. The details of data collection and basic crystallographic facts are given in Table 4.

Table 4.

Powder diffraction data collection and Rietveld analysis of a synthetic analogue of kvačekite, NiSbSe.

Rietveld refinement was carried out using the Topas 5 program and involved refinement of unit-cell parameter, atomic coordinates, isotropic size and strain parameters. Isotropic displacement parameters were fixed during the refinement (B _iso = 0.2 Ų). The structure model proposed by Hulliger (Reference Hulliger1963) and subsequently by Foecker and Jeitschko (Reference Foecker and Jeitschko2001) for synthetic NiSbSe was confirmed, the refined coordinates did not deviate more than 0.002 from their starting positions. The refined unit-cell parameter a = 6.0902(2) Å agrees very well with the data a = 6.0868(6) Å (Foecker and Jeitschko, Reference Foecker and Jeitschko2001) and a = 6.090(3) Å (Hulliger, Reference Hulliger1963) given for synthetic NiSbSe. The refinement converged to R _wp = 0.056, R _B = 0.067 and the final Rietveld plot is shown in Fig. 4. The atomic positions are summarised in Table 5. The crystallographic information file has been deposited with the Principal Editor of Mineralogical Magazine and is available as Supplementary material (see below).

Figure 4.

Rietveld plot of synthetic analogue of kvačekite, NiSbSe. The refinement reveals 6 and 3 wt.% of Sb₂Se₃ and NiSb, respectively, as impurities.

Table 5.

Atomic fractional coordinates and isotropic displacement parameters in synthetic NiSbSe.

^a Isotropic displacement parameters were fixed during the refinement.

Synthetic NiSbSe crystallises in the cubic space group P2₁3 and has the ullmannite type structure. It can be considered as a ternary ordered variant of the pyrite-type structure MX₂ (Pa $\bar{3}$), where Sb and Se atoms replace S atoms and are ordered at two independent crystallographic positions X and Y. Consequently, the symmetry is lowered from Pa $\bar{3}$ (pyrite type) to P2₁3 (ullmannite type). Derivation of the kvačekite crystal structure from the pyrite-type and corresponding group–subgroup relation is shown in Fig. 5. The disordered (i.e. pyrite-type) structure model with the Sb/Se mixed site has been also tested in the Rietveld refinement. As indicated in Fig. 6, this structured model yields significantly worse profile agreement factors and cannot fit all observed reflections in the powder diffraction pattern of synthetic NiSbSe. Therefore, the disordered pyrite-type structure can be excluded.

Figure 5.

The group-subgroup relation (Pa $\bar{3}$ → P2₁3) for the pyrite-type and kvačekite crystal structure showing the splitting of the Wyckoff positions during the reduction of the symmetry (loss of the inversion centre in Pa $\bar{3}$ space group).

Figure 6.

Details of the Rietveld refinement of the synthetic analogue of kvačekite NiSbSe using the (a) pyrite and (b) ullmannite structure models. Only the ullmannite structure model is able to fit all of the observed reflection. The unfitted reflection is indicated by an arrow.

Another ordering of anion atoms occurs in the cobaltite-type structure (CoAsS), which shows orthorhombic symmetry (Pca2₁). No indication of peak splitting indicating orthorhombic symmetry have been observed for the synthetic analogue of kvačekite.

The crystal structure of kvačekite is formed by corner-sharing [NiSb₃Se₃] octahedra (Fig. 7). There are three Ni octahedra sharing every anion. The Sb and Se atoms form covalent pairs (i.e. dumbells), with bonding distance of 2.665 Å. A similar bonding distance of 2.636 Å in Sb–Se covalent pairs was observed in milotaite, PdSbSe (Paar et al., Reference Paar, Topa, Makovicky and Culetto2005). This is slightly longer than observed Ni–Se and Ni–Sb distances of 2.469(3) and 2.579(3) Å, respectively. Considering Ni–Se distances, slightly longer NiSe separations of 2.503 Å were observed in synthetic NiSe (Unoki et al., Reference Unoki, Yoshiasa, Kitahara, Nishiayama, Tokuda, Sugiyama and Nakatsuka2021), an analogue of sederholmite, which adopts a nickeline-type structure. Ullmannite shows a Ni–Sb distance of 2.563 Å (Foecker and Jeitschko, Reference Foecker and Jeitschko2001) which can be compared with the Ni–Sb separations in the kvačekite structure (2.579(3) Å). In addition to ullmannite, the most closely related mineral species is milotaite, PdSbSe (Paar et al., Reference Paar, Topa, Makovicky and Culetto2005).

Figure 7.

Crystal structure of synthetic analogue of kvačekite, NiSbSe, showing the corner-sharing [NiSb₃Se₃] octahedrons (in blue). Note the Sb–Se anion pairs. Drawn using Diamond (Crystal Impact, Reference Putz, Brandenburg and Kreuzherrenstr2014).

Electron back-scattered diffraction

The structural correlation between the synthetic NiSbSe and the natural kvačekite was confirmed by electron back-scattered diffraction (EBSD). For that purpose, we used a TESCAN Mira 3GMU scanning electron microscope combined with EBSD system Symmetry (Oxford Instruments). The natural sample surface was re-polished with colloidal silica (OP-U) for 20 min to remove an amorphised layer formed due to standard diamond polishing. The EBSD patterns were collected and processed using the proprietary software AZtec 6.0 (Oxford Instruments). The Kikuchi patterns obtained from the natural material (35 measurements on different spots on five grains of natural kvačekite) were found to match the patterns generated from our refined structural model for synthetic NiSbSe (Fig. 8). The Kikuchi bands (11, containing 48 reflectors) were detected using the optimised accuracy indexing mode, using band edges, with a Hough resolution of 65. The values of the mean angular deviation (MAD; goodness-of-fit in the solution) between the calculated and measured Kikuchi bands range between 0.11° and 0.36°. These values hence reveal a very good match; mean angular deviations <1° are considered as indicators of an acceptable fit.

Figure 8.

Examples of EBSD images of natural kvačekite; in the right pane, the Kikuchi bands are indexed.

Berzelianite

Berzelianite belongs among the most abundant selenides within the samples studied. It occurs as anhedral grains up to 1 cm in size in calcite gangue in association with other selenides. In reflected light it is greenish blue and isotropic.

The chemical composition of berzelianite (Table 6) is relatively uniform and is close to the ideal formula Cu_2–xSe (with x ≈ 0.18). In addition to the main cation (Cu), minor contents of Ag (up to 0.004 apfu), Co (up to 0.031 apfu) and Ni (up to 0.020 apfu) were found, Co and Ni may be an effect of sub-microscopic inclusions of nickeltyrrellite. In the anion part, the range of SSe_–1 substitution is limited to 0.26 apfu S. The mean composition of berzelianite (calculated from 69 point analyses on the basis of 1 Se+S apfu) is (Cu_1.81Co_0.01)_Σ1.82(Se_0.89S_0.11)_Σ1.00.

Table 6.

EPMA chemical data (wt.%) for berzelianite, clausthalite and eucairite.

Nickeltyrrellite–tyrrellite solid solution

Minerals of the nickeltyrrellite–tyrrellite solid solution are abundant in the association studied. They form euhedral grains (metacrysts) up to 300 μm in size (Fig. 9a) and groups of crystals up to 2 mm in length (Fig. 9b), both enclosed in berzelianite. More rarely, they occur as anhedral aggregates up to 800 μm in size in calcite gangue without other selenides (Fig. 9c). In reflected light they are yellowish brown and isotropic.

Figure 9.

Reflected light images of selenides in association with kvačekite from Bukov: (a) euhedral nickeltyrrellite–tyrrellite grains (yellowish brown) in berzelianite (greenish blue); (b) groups of nickeltyrrellite–tyrrellite grains (yellowish brown) with tiny clausthalite (white) in berzelianite (greenish blue); (c) anhedral nickeltyrrellite–tyrrellite aggregates in calcite; (d) clausthalite grains (white) in nickeltyrrellite–tyrrellite (yellowish brown) and berzelianite (greenish blue) with tiny hakite-(Zn) (brownish); (e) eucairite grains (brown) with tiny gold veinlets (yellow) in clausthalite (white), berzelianite (greenish blue) and nickeltyrrellite–tyrrellite (yellowish brown); (f) hakite-(Zn) grain (brownish) in berzelianite (greenish blue) with tiny nickeltyrrellite–tyrrellite inclusions (yellowish brown).

The chemical composition of the minerals studied corresponds to the formulae Cu(Ni,Co)₂Se₄–Cu(Co,Ni)₂Se₄ (Förster et al., Reference Förster, Ma, Grundmann, Bindi and Stanley2019). The determined representation of CoNi_–1 substitution (Fig. 10) indicates the presence nickeltyrrellite with Ni contents in the wide range of 1.08–2.43 apfu and on the other hand tyrrellite, where Co contents (1.04–1.29 apfu) only slightly prevail over Ni (0.83–1.29 apfu). A wide extent of CoNi_–1 substitution was observed even within individual grains, e.g. from 0.96 to 2.43 apfu Ni in a single grain of 40 μm size. For both minerals, the majority of measured Cu contents (0.55–1.06 apfu) is too low to completely fill the Cu position. It is likely that other cations (Co and/or Ni) have entered this position; a similar situation was described for part of nickeltyrrellite grains from El Dragón by Förster et al. (Reference Förster, Ma, Grundmann, Bindi and Stanley2019). The range of SSe_–1 substitution in nickeltyrrellite (0.01–0.25 apfu S) is close to that of tyrrellite (0.02–0.34 apfu). Representative compositions of minerals of the nickeltyrrellite–tyrrellite solid solutions and the corresponding empirical formulae are given in Table 7.

Figure 10.

Chemical composition of members of the tyrrellite–nickeltyrrellite series from Bukov in part of the ternary Cu–Co–Ni (at. units) plot. Dashed line corresponds to ideal Cu(Ni,Co)₂Se₄ composition.

Table 7.

Representative EPMA chemical data (wt.%) and atomic proportions for nickeltyrrellite and tyrrellite.

Clausthalite

Clausthalite is a rarer phase, it forms anhedral grains up to 300 μm in size in nickeltyrrellite–tyrrellite and partly replaces earlier berzelianite (Fig. 9d). In reflected light, it is isotropic and has a white colour.

Clausthalite contains, in addition to Pb and Se (Table 6), minor contents of Cu (up to 0.05 apfu) and Co, Ni (both up to 0.02 apfu) and is S-free. Its empirical formula (mean of 23 point analyses on the basis of 2 apfu) is (Pb_0.97Cu_0.02Ni_0.01Co_0.01)_Σ1.01Se_0.99.

Eucairite

Rare eucairite occurs as anhedral grains up to 100 μm in size and partly replaces earlier berzelianite (Fig. 9e), usually in association with clausthalite and nickeltyrrellite–tyrrellite.

Tiny veinlets of gold (with up to 17 wt.% Ag and 5 wt.% Hg) in eucairite grains were observed only occasionally. In reflected light, eucairite is brown and strongly anisotropic in blue green – blue grey rotation tints.

Its chemical composition (Table 6) is close to the ideal formula CuAgSe; only minor contents of Ni, Co (both up to 0.016 apfu) and Cd (up to 0.004 apfu) were determined. The mean composition of eucairite (calculated from 17 point analyses on the basis of 3 apfu) is Ag_1.00Cu_1.02Co_0.01Ni_0.01Se_0.96.

Hakite-(Zn) and hakite-(Cd)

Hakite forms anhedral grains up to 100 μm in size in berzelianite (Fig. 9f) and nickeltyrrellite–tyrrellite, locally in intergrowths with kvačekite and clausthalite. Hakite replaces earlier berzelianite and clausthalite and can contain relics of these minerals and of nickeltyrrellite. In reflected light it is brownish and isotropic.

According to the nomenclature scheme of minerals of the tetrahedrite group (Biagioni et al., Reference Biagioni, George, Cook, Makovicky, Moëlo, Pasero, Sejkora, Stanley, Welch and Bosi2020) the studied minerals correspond to hakite-(Zn) and two point analyses to hakite-(Cd), both with regular minor Hg contents (Fig. 11). Both minerals were recently defined as new minerals on samples from the Příbram uranium ore district (Czech Republic) by Sejkora et al. (Reference Sejkora, Biagioni, Škácha, Musetti and Dolníček2024). The trigonal position of both studied members from Bukov is predominantly occupied by Cu, with minor amounts of Ag (up to 0.60 apfu). Zinc, and in the case of two point analyses Cd, are dominant Me ²⁺ elements; there are two trends in minor contents of Hg (Fig. 11) – approximately 0.13 apfu and in the range 0.19–0.39 apfu. The calculated Cu²⁺ contents reach up to 0.60 apfu. Locally minor contents of Ni and Co were observed, reaching up to 0.19 and 0.16 apfu, respectively. The studied hakites are pure Sb members and the range of SSe_–1 substitution is limited to 1.70 apfu S. Representative chemical analyses of hakite-series minerals and the corresponding empirical formulae are given in Table 8.

Figure 11.

Chemical composition of members of the hakite series in the ternary Zn–Hg–Cd (at. units) plot; non-dominant elements Ni (up to 0.19 apfu), Co (up to 0.16 apfu) and calculated Cu²⁺ (up to 0.60 apfu) are omitted.

Table 8.

Representative EPMA chemical data (wt.%) and atomic proportions for hakite-(Zn) and hakite-(Cd).