Occurrence and sample

Holubite was found in 24 different samples (300 analytical points) from the Staročeské pásmo Lode (Old Bohemian Lode in English) of the Kutná Hora Ag–Pb–Zn ore district. The ore district (located 60 km east of Prague, Central Bohemia, Czech Republic, 49.9521753N, 15.2634625E) contains a hydrothermal vein type mineralisation of Variscan age (≈ 270 m.y.). The geological situation, mineralogy and geochemistry of the ore district have been detailed by Holub et al. (Reference Holub, Hoffman, Mikuš and Trdlička1982) and Malec and Pauliš (Reference Malec and Pauliš1997). It was one of the main European producers of silver in the 14^th to 16^th Century, with >100 mines on 12 major lodes (Fig. 1). Each lode (ore zone, also called pásmo in Czech or zug in German) represents a hydrothermally altered zone of several hundred metres to ~ 3 km in length and dozens of metres wide, with the depth ranging between several hundred metres to 1 km, each consisting of several, usually parallel veins (Holub et al., Reference Holub, Hoffman, Mikuš and Trdlička1982). Geologically and mineralogically, two mineral assemblages are present in this ore district, one ‘silver-rich’ in the southern part of the ore district and one ‘pyrite-rich’ in the northern part (Malec and Pauliš, Reference Malec and Pauliš1997). The Staročeské pásmo Lode belongs to the northern pyrite-rich lodes and is the biggest lode of the Kutná Hora ore district. The newly discovered Bi–Ag sulfosalt mineralisation was described in Pažout (Reference Pažout2017) and Pažout et al. (Reference Pažout, Sejkora and Šrein2017).

Figure 1. Map of Kutná Hora ore district with major lodes (zones) (Malec and Pauliš, Reference Malec and Pauliš1997). Each lode (zone) consists of several veins.

All the samples of holubite studied come from the Staročeské pásmo Lode (Old Bohemian Lode) of the Kutná Hora ore district, though Bi was also determined by the first author of this article in sulfosalts from other northern lodes (Hloušecké pásmo Lode and Turkaňské pásmo Lode). The samples were collected in the material from medieval mine dumps, therefore no information is available on their in situ position in individual vein structures. Only a small part of the samples studied comes from some recent mining and geological survey activity in the 1960's.

The Staročeské pásmo Lode was mined from the discovery and opening of the ore district in the second half of the 13^th Century until the end of large-scale mining at the end of 16^th Century. It is estimated that some 350 to 500 t of silver were extracted from this lode, far more than from any other lode of the ore district including the Ag-rich lodes in the South (Malec and Pauliš, Reference Malec and Pauliš1997). The second peak of mining activity in the Kutná Hora ore district was enabled thanks to the discovery of a new rich deposit, the Benátecká Vein of the Staročeské pásmo Lode, in the second half of the 16^th Century. The vein was not discovered by previous miners because it does not crop out. This Ag-rich base-sulfide vein with Fe–Cu–Sn–Zn–As–(Ag–Pb–Bi–Sb) formed mainly of massive pyrite, pyrrhotite, marcasite, chalcopyrite, arsenopyrite, sphalerite and stannite, up to two metres thick, produced an estimated 100 t of silver in <40 years (Holub, Reference Holub2009). This vein was the subject of small-scale mining carried out within the Geological Survey in the 1960's and the newly found material from this mining made it possible to study the mineralogical composition of the massive Ag-rich pyrite ores (not present on the medieval dumps), next to Ag–Bi mineralisation in quartz gangue without massive sulfides, which can occasionally be found on mediaeval mine dumps.

The holotype hand sample (ST 61) is formed of white coarse-grained quartz with silvery grey metallic lenses and grains of Ag,Bi-bearing galena and Ag–Bi sulfosalts (including holubite, terrywallaceite, eskimoite and treasurite) up to 3 mm across with no base sulfides. A back-scattered electron (BSE) image of the holotype sample extracted for the structure determination is in Fig. 2. The mineral occurs most frequently as replacement rims and grain aggregates of earlier Ag–Pb–Bi minerals, growing together in aggregates up to 200 × 50 μm. It commonly occurs in a close association with Ag,Bi-bearing galena and terrywallaceite (Fig. 3). We assume the mineral is a replacement product of earlier galena and lillianite homologues, richer in Bi, in line with a general succession trend observed in the Ag–Pb–Bi–Sb mineralisation in the Kutná Hora ore district being from Bi-rich to Sb-rich minerals (Pažout et. al., Reference Pažout, Sejkora and Šrein2017).

Figure 2. BSE image of holotype sample (ST 61) with Ag,Bi-bearing galena (white) and replacement rims and homogenous grains of holubite (grey). The red box indicates the area sampled for single-crystal X-ray diffraction.

Figure 3. A frequent mode of occurrence of holubite: Ag,Bi-bearing galena (G) replaced by lamellae of terrywallaceite (T, medium grey) and replacement rims of holubite (H, dark grey). The succession is galena – terrywallaceite – holubite. BSE image of sample ST 108; the field of view is 700 μm.

Physical and optical properties

Holubite is opaque, steel-grey in colour and has a metallic lustre and grey streak. The calculated density = 5.899 g.cm^–3 on the basis of the empirical formula and 5.905 g.cm^–3 on the basis of the ideal formula, both with single-crystal unit-cell parameters. In reflected light holubite is greyish white and bireflectance and pleochroism are weak with grey tints. Anisotropy is weak to medium, with grey to bluish-grey rotation tints. Fluorescence was not observed, neither were internal reflections. Reflectance values of holubite (WTiC Zeiss 370), measured in air (spectrophotometer MSP400 Tidas at Leica microscope, objective 50×), are in Table 1 (COM standard wavelengths are given in bold) and Fig. 4. A comparison of reflectance curves for holubite, staročeskéite and ramdohrite is in Fig. 5.

Table 1. Reflectance values of holubite (COM standard wavelengths are given in bold).

Figure 4. Reflectance curve for holubite from Kutná Hora.

Figure 5. Reflectance curve for holubite from Kutná Hora. For comparison, the curves for staročeskéite from Kutná Hora (Pažout and Sejkora, Reference Pažout and Sejkora2018) and ramdohrite from Chocaya, Bolivia (Picot and Johan, Reference Picot and Johan1982) are shown.

Chemical composition

Chemical analyses of the holotype sample were performed using a JEOL JXA-8600 electron probe microanalyser (EPMA) of University of Salzburg in wavelength dispersive spectroscopy (WDS) mode (25 kV and 35 nA) and beam diameter of 5 μm. The following standards and X-ray lines were used: CuFeS₂ (CuKα and FeKα); Ag (AgLα); PbS (PbLα); Bi₂S₃ (BiLα and SKα); Sb₂S₃ (SbLα); CdTe (CdLβ and TeLα); Bi₂Te₂S (BiLα and TeLα); and Bi₂Se₃ (SeKα). Raw data were corrected with an online ZAF-4 procedure. A second set of polished sections with staročeskéite was measured on a CAMECA SX100 electron probe microanalyser at the National Museum, Prague in 2015. The analytical conditions were as follows: WDS mode, accelerating voltage of 25 kV, beam current of 20 nA, electron-beam diameter of 2 μm and standards: chalcopyrite (SKα); Bi₂Se₃ (BiMβ); PbS (PbMα); Ag (AgLα); halite (ClKα); Sb₂S₃ (SbLα); CdTe (CdLα); HgTe (HgMα); pyrite (FeKα); Cu (Cu_Kα); ZnS (ZnKα); NiAs (AsLα) and PbSe (SeLβ). Measured data were corrected using PAP software (Pouchou and Pichoir, Reference Pouchou, Pichoir and Armstrong1985). Analytical data for the holotype sample are given in Table 2. Its empirical formula (calculated on the basis of 44 atoms per formula unit) is:

Table 2. Chemical data for holubite (six spot analyses)

(Ag_3.03Cu_0.03)_Σ3.06(Pb_6.19Fe_0.02Cd_0.01)_Σ6.22(Sb_7.71Bi_2.90)_Σ10.61S_24.12, corresponding to N _chem = 4.24, Bi/(Bi + Sb) = 0.27 and the (Ag⁺ + (Bi³⁺,Sb³⁺) ↔ 2 Pb²⁺) substitution percentage L = 71.6%. The simplified formula is (Ag,Cu)₃(Pb,Fe,Cd)₆(Sb₈Bi₃)_Σ11S₂₄ and the ideal formula is Ag₃Pb₆(Sb₈Bi₃)_Σ11S₂₄, corresponding to (in wt.%) Ag 8.22, Pb 31.58, Sb 24.74, Bi 15.92 and S 19.54, total 100 wt.%. Holubite can be differentiated unequivocally from chemical results from similar members of the lillianite homologous series on the basis of the substitution percentage L (calculated from the results of chemical analysis) and the Bi/(Bi+Sb) ratio.

Crystallography and crystal structure

A tiny fragment of holubite with dimensions of 0.035 × 0.030 × 0.030 mm was extracted from a polished section of the holotype sample and separated under the optical stereomicroscope. The intensity data were collected at ambient temperature using an Oxford Diffraction Gemini single-crystal diffractometer equipped with a SuperNova CCD detector and using monochromated MoKα radiation from conventional sealed X-ray tube (55 kV and 30 mA), using a fiberoptics Mo-Enhance collimator. The total of 7038 reflections were measured. After averaging, 4388 reflections were independent and 812 classified as observed [I _obs > 3σ(I)]. Data were corrected for background, Lorentz and polarisation effects, and a multi-scan correction for absorption was applied, resulting in R _int of the merged data equal to 0.1479. The twinning tool incorporated in Jana2020 (Petříček et al., Reference Petříček, Dušek and Palatinus2020) revealed the crystal is twinned on (001) in this unit-cell orientation and the volume fractions of each twin is 0.683(7) and 0.317(7), respectively. The final refinement of occupancies returned values close to those obtained from the microprobe study. The refinement for 122 parameters converged to the final R = 0.0853, wR = 0.1475 for 812 observed reflections with GOF = 1.31.

In the process of indexing, a monoclinic cell was found; images from data collection showed a primitive unit cell with the presence of reflections doubling the size of the shortest ‘sulfosalt’ parameter (c in this setting), typical of fizélyite, ramdohrite and oscarkempffite. The unit-cell parameters determined from single-crystal data by a least-squares algorithm using the CrysAlis Pro package (Rigaku, Reference Rigaku2019) are as follows: a = 19.374(4), b = 13.201(3), c = 8.651(2), β = 90.112(18)°, V = 2212.5(9) ų, space group P2₁/n and Z = 2. The powder X-ray diffraction data could not be collected due to paucity of material; the calculated powder diffraction data are given in Table 3.

Table 3. Calculated powder X-ray diffraction data for holubite. Intensity (I, %) and d _hkl (Å) were calculated using the software Diamond 4 (Putz and Brandenburg, Reference Putz and Brandenburg2017) on the basis of our single-crystal structure refinement. Only reflections with I _calc > 3 are listed. The eight strongest reflections are given in bold.

The structure of holubite was solved independently from earlier structure determinations of structurally related compounds by the charge-flipping algorithm (Palatinus and Chapuis, Reference Palatinus and Chapuis2007) implemented in Jana2020 (Petříček et al., Reference Petříček, Dušek and Palatinus2020). Systematic absences and intensity statistics indicated centrosymmetric space group P2₁/n, in line with previous structure determinations of oscarkempffite (Dan Topa, pers. comm.) and ramdohrite (Makovicky et al., Reference Makovicky, Mumme and Gable2013). All atomic positions were found, which were subsequently refined by full-matrix least-squares based on F² using Jana2020 (Petříček et al., Reference Petříček, Dušek and Palatinus2020). The distance and bond-valence calculations indicated that the trigonal prismatic sites Pb2 and Pb3 are occupied solely by Pb, similarly to other known structures of lillianite homologues with N = 4 and L ≤ 100%. Interatomic distances showed that one of the Sb sites (M4) is in a fact a bismuth site which was confirmed by the difference-Fourier and refinement results in Jana2020 and charge density calculations in the program ECoN21 (Ilinca, Reference Ilinca2022). It also showed that the M5 site is a mixed position with ~1:1 ratio of Bi and Ag and that the Sb6 position is a mixed site with 0.86 Sb and 0.14 Pb. Metal atoms were refined with anisotropic atomic displacement parameters (ADPs) with the exception of Sb atoms, which were refined with isotropic ADPs. Due to weak diffraction data (only 812 observed reflections out of the total of 4388 unique reflections), which could not be improved even with an exposition of 400 s per frame and a crystal fragment so small that a shape correction for absorption was not executable, Sb and some S atoms returned negative ADP values at various stages of refinement. However, in the final structural model Sb atoms and all sulfur atoms were successfully refined with individual isotropic ADPs. Details of data collection, crystallographic data and refinement are given in Table 4. Atom coordinates, occupancies and isotropic displacement parameters are in Table 5, ADPs of metal atoms that were refined anisotropically are in Table 6 and interatomic distances are listed in Table 7. The crystallographic information files have been deposited with the Principal Editor of Mineralogical Magazine and are available as Supplementary material (see below). Results of charge-distribution calculations of metal sites in the structure of holubite in the cation-centred description using ECoN21 (Ilinca, Reference Ilinca2022) is in Table 8. The final structural formula is Ag_2.98Pb_6.28(Sb_7.72Bi_3.02)_Σ10.74S₂₄, which is in good agreement with microprobe-established composition (Ag_3.03Cu_0.03)_Σ3.06(Pb_6.19Fe_0.02Cd_0.01)_Σ6.22(Sb_7.70Bi_2.90)_Σ10.60S_24.10.

Table 4. Summary of data collection conditions and refinement parameters for holubite.

* This value is for sin(th)/lambda limit set to 0.5 (corresponding to d =1 Å).

Table 5. Fractional atomic coordinates, occupancies and equivalent isotropic displacement factors (Ų).

* Site occupation factors: M5: Bi_0.51(3)Ag_0.49(3); M6: Sb_0.86(4)Pb_0.14(4)

Table 6. Anisotropic atomic displacement parameters (in Ų).

Table 7. Selected interatomic distances (Å).

Table 8. Detailed results of charge-distribution calculations of metal sites in the structure of holubite in the cation-centred description using the program ECoN21 (Ilinca, Reference Ilinca2022).

Key: MAPD: 2.58%; CN – coordination number; ECoN – effective coordination number; EDEV – deviation of ECoN from CNR (number of ligands with bond weights exceeding 0.001); AV– average bond length; PVol – volume of coordination polyhedron; qX – oxidation number of cations; QX – charge received by cations; MAPDL – mean absolute percentage deviation of ligands QA (anion charge); MAPD – mean absolute percentage deviation of QX; BVS – bond valence sum.

On the basis of the current crystal structure study we conclude that holubite is closely related to ramdohrite, which is a Bi-free lillianite homologue of the andorite branch. Holubite displays two significant differences from ramdohrite, justifying a new mineral species: (1) the marginal octahedral antimony site Me6 in ramdohrite (Makovicky et al., Reference Makovicky, Mumme and Gable2013) is a bismuth site, Bi4, in holubite; (2) the marginal octahedral Me9 site (0.4 Sb + 0.6 Ag) in ramdohrite becomes a Bi–Ag site, M5, with 0.51 Bi + 0.49 Ag. In addition, there is one more difference compared to the ramdohrite refinement. The marginal octahedral antimony site Me1 in ramdohrite is an Sb–Pb site M6 with (0.86 Sb + 0.14 Pb) in holubite, where the excess Pb above 6 apfu is located. Although the issue of excess Pb above 6 apfu (e.g. for And₇₀ it is 0.4 Pb) was not addressed in the new refinement of ramdohrite (Makovicky et al. Reference Makovicky, Mumme and Gable2013), it is likely that either their Me1 or Me6 site (or both) contain some Pb. A similar situation is in the structure of andorite IV (Nespolo at al., Reference Nespolo, Ozawa, Kawasaki and Sugiyama2012), where authors did not address the issue of excess Pb above 4 apfu (e.g. for And_92.5 it is 0.6 Pb).

The structure of holubite, a natural Sb–Bi monoclinic ^4,4L homologue of the lillianite homologous series, contains 10 cation (metal) sites and 12 anion (sulfur) sites. The metal sites consist of two Pb sites (Pb2 and Pb3) in trigonal prismatic coordination and eight independent octahedral sites. Four of the octahedral sites are marginal octahedra flanking the bicapped trigonal prisms of Pb2 and Pb3 from each side along a and four are central octahedra inside the ⁴L slabs. Both types of octahedra (marginal and central) can be viewed as formed by two rows along c, each row consisting of two alternating metal sites. The structure of holubite projected down [001] is shown in Fig. 6.

Figure 6. The crystal structure of holubite, a natural Bi–Sb ^4,4L homologue of the lillianite homologous series: Pb2 and Pb3 – lead atoms in bicapped trigonal prismatic coordination (CN 8), all other metal atoms are in octahedral coordination (CN 6). Marginal octahedra are: Ag10, M5 (Bi–Ag mixed site), Bi4 and M6 (Sb6–Pb6 mixed site). Central octahedral are: Pb1, Sb9, Sb8 and Sb7, S – sulfur atoms. View down c axis. Holubite is closely related to ramdohrite (Makovicky et al., Reference Makovicky, Mumme and Gable2013) and oscarkempffite (Topa, personal communication). Drawn using Diamond 4 (Putz and Brandenburg, Reference Putz and Brandenburg2017).

Regarding the marginal octahedra, in one row the Ag site Ag10 alternates with the Ag–Bi mixed site M5 (0.51Bi + 0.49Ag), in the other row one Pb–Sb mixed site M6 (0.86 Sb – 0.14 Pb) alternates with the pure Bi site Bi4. This is a significant difference compared to ramdohrite (Makovicky et al., Reference Makovicky, Mumme and Gable2013). In ramdohrite along a (in their setting), in one row the Ag site Me4 alternates with the Ag–Sb mixed site Me9 (0.4 Sb + 0.6 Ag), while in the other pure Sb site Me1 alternates with the Sb site Me6. On the other hand, this situation in holubite is somewhat similar (owing to the presence of the Sb–Pb site) to the one in the structure of Ag-excess fizélyite (Yang et al., Reference Yang, Downs, Burt and Costin2009), where one row of octahedra is formed by two alternating Sb positions Sb1 and Sb3. The situation in the second row is more complex here as there is alternation between a partially occupied pair Ag1 (0.75Ag) and Ag1’ (0.19Ag) with a M2 and M2’ mixed pair. M2’ is formed by partially occupied Ag (0.33Ag), whereas M2 contains (0.556Pb + 0.095Sb). Furthermore, there is another partially occupied position Ag2 (0.21Ag) sandwiched between the two pairs, not detected in structures of other andorite-branch minerals. As to the central octahedra, the situation in holubite and ramdohrite is similar. In holubite, one row is formed by alternating Sb positions Sb7 and Sb8 (pure Sb sites Me2 and Me7 in ramdohrite), while in the other the Pb site Pb1 alternates with the pure Sb site Sb9 (the Pb site Me5 alternates with the Sb site Me10 in ramdohrite). All four Sb sites in holubite are typical pure Sb sites with three short and three long opposing distances. The coordination of Bi4 does not deviate from a pure Bi site in other sulfosalts and the same applies to the octahedral Pb site Pb1.

Relation to other species

Holubite is a new member of the lillianite homologous series, class 3.1.1. of the Sulfosalt systematics (Moëlo et al., Reference Moëlo, Makovicky, Mozgova, Jambor, Cook, Pring, Paar, Nickel, Graeser, Karup-Møller, Balić-Žunić, Mumme, Vurro, Topa, Bindi, Bente and Shimizu2008), Strunz class 02.JB.40a, Dana class 3.04.15. A comparison of selected data for holubite Ag₃Pb₆(Sb₈Bi₃)_Σ11S₂₄, ramdohrite Ag₃Pb₆Sb₁₁S₂₄ and staročeskéite Ag_0.70Pb_1.60(Bi_1.35Sb_1.35)_Σ2.70S₆ is given in Table 9. All three minerals display the same (or very similar) percentage of the lillianite substitution [Ag⁺ + (Bi³⁺,Sb³⁺) ↔ 2 Pb²⁺], L% ≈ 70 and only differ by Bi content substituting for Sb. Whereas ramdohrite is a pure Sb member with no bismuth, holubite has one quarter to one third of Sb replaced by Bi (Bi/(Bi+Sb) = 0.26–0.34) and staročeskéite has a half of the Sb content replaced by Bi (Bi/(Bi+Sb) ≈ 0.5).

Table 9. Comparative data for the relevant minerals.

* – calculated from the structure data

Structurally, holubite has a unit cell and symmetry similar to those of ramdohrite, fizélyite, Ag-rich fizélyite, uchucchacuaite, menchettiite, oscarkempffite (Makovicky and Topa, Reference Makovicky and Topa2014) and lazerckerite, with a ≈ 19, b ≈ 13, c ≈ 8.5, β ≈ 90°, V ≈ 2200, (regardless of axial setting) and space group P2₁/n or P2₁/c. Lazerckerite, Ag_3.75Pb_4.50(Sb_7.75Bi₄)S₂₄, is a new mineral of the andorite branch, of the lillianite homologous series with L% ≈ 90–95 and a Bi/(Bi+Sb) ratio of ~0.30 (IMA2022-113; Pažout et al. Reference Pažout, Plášil, Dušek, Sejkora and Ilinca2023b). Chemically, holubite can be compared with other related lillianite homologues on the basis of two parameters: (1) lillianite substitution percentage L%; and (2) bismuth (vs. antimony) content expressed as the Bi/(Bi+Sb) ratio. Regarding the L% – holubite has the same L% as ramdohrite and staročeskéite (all three have L% ≈ 70). However, ramdohrite has no bismuth, whereas holubite has Bi/(Bi+Sb) = 0.26–0.34 and staročeskéite has Bi/(Bi+Sb) = 0.45–0.55. Regarding the Bi/(Bi+Sb) ratio – three minerals display Bi/(Bi+Sb) of ~0.30: holubite, lazerckerite and oscarkempffite. However, holubite has L% ≈ 70, lazerckerite has L% ≈ 90–95 and oscarkempffite is even an oversubstituted member with L% ≈ 120–125. All these minerals possess the above monoclinic unit cell with the exception of staročeskéite, which has an orthorhombic unit cell with a ≈ 19, b ≈ 13, c ≈ 4.25 and V ≈ 1100 (regardless of axial setting). Thus holubite stands as a unique mineral both structurally and chemically, differing distinctly from ramdohrite, staročeskéite, lazerckerite and oscarkempffite and other known members of the lillianite homologous series. It is defined as a lillianite homologue with the following requirements: N = 4, L (Ag⁺ + Bi³⁺,Sb³⁺ ↔ 2Pb²⁺ substitution) ≈ 70% and about one quarter to one third at.% of antimony is replaced by bismuth (Bi/(Bi+Sb) ≈ 0.26–0.34).

Mixed members of the lillianite homologous series are either Bi–Sb members or Sb–As members (arsenquatrandorite and jasrouxite). Here we will deal with the former. The mixed Bi–Sb members of the lillianite homologous series is a fairly new and not so frequent group among either Bi-dominant (lillianite branch) or Sb-dominant (andorite branch) members of the series. To this date, it comprises four minerals: terrywallaceite, oscarkempffite, clino-oscarkempffite and staročeskéite, which is now being widened by the addition of holubite and lazerckerite (IMA2022-113). Oscarkempffite Pb₄Ag₁₀Sb₁₇Bi₉S₄₈ is characterised by L = 120–125% and a Bi/(Bi+Sb) range between 0.29 and 0.37 (Topa et al., Reference Topa, Makovicky, Stanley and Robetzs2016), clino-oscarkempffite Pb₆Ag₁₅Sb₂₁Bi₁₈S₇₂ has L = 122–123% and Bi/(Bi+Sb) = 0.46–0.48 (Makovicky et al., Reference Makovicky, Topa and Paar2017). Terrywallaceite has L = 80–110% and Bi/(Bi+Sb) = 0.45–0.75 (values obtained by EPMA, Pažout, Reference Pažout2017).

Notable occurrences of mixed Bi–Sb members with N = 4 (both Sb-rich members of the lillianite branch and Bi-rich members of the andorite branch) were previously described on the basis of the EPMA data from Alyaskitovoye deposit, Yakutia, Russia (Mozgova et al., Reference Mozgova, Nenasheva, Borodaev, Sivcov, Ryabeva and Gamayanin1987, Reference Mozgova, Nenasheva, Jefimov, Borodaev, Cepin and Sivcov1988), from Julcani, Peru (Moëlo et al., Reference Moëlo, Makovicky and Karup-Møller1989) and Oruro, Bolivia (Keutsch and Brodtkorb, Reference Keutsch and Brodtkorb2008). Recently, an extraordinary extent of the Bi–Sb substitution in minerals of the lillianite homologous series was described from the Kutná Hora ore district, Czech Republic (Pažout, Reference Pažout2017). Due to a lack of single-crystal data (resulting from the difficulty to find suitable homogenous grains) these Bi–Sb members were then characterised in Pažout (Reference Pažout2017) as Bi-rich fizélyite or Bi-rich ramdohrite (= holubite, IMA2022-112) and Bi-rich andorite IV (= lazerckerite, IMA2022-113).

Comparing the data from Kutná Hora with published data from elsewhere in the past, it is apparent that a mineral phase corresponding to holubite has not been described before. Mineral phases from Alyaskitovoye deposit (Mozgova et al., Reference Mozgova, Nenasheva, Borodaev, Sivcov, Ryabeva and Gamayanin1987, Reference Mozgova, Nenasheva, Jefimov, Borodaev, Cepin and Sivcov1988) show L% between 94 and 114 and Bi/(Bi+Sb) = 0.41–0.70, and thus correspond mainly to terrywallaceite, which is also supported by their diffraction data. Samples from Julcani (Moëlo et al., Reference Moëlo, Makovicky and Karup-Møller1989) with L% = 101–118 and Bi/(Bi+Sb) = 0.31–0.40 correspond to a phase that can be chemically characterised as Bi-rich andorite VI (analyses with L% ≈ 101 and Bi/(Bi+Sb) around 0.30), terrywallaceite (analyses with L% ≈ 100–115 and Bi/(Bi+Sb) > 0.40) or oscarkempffite (analyses with L% ≈ 118). The majority of analyses show L% between 105 and 115; precise identification of these minerals would be possible on the basis of structural characterisation by single-crystal diffraction. Samples from Oruro (Keutsch and Brodtkorb, Reference Keutsch and Brodtkorb2008) with L% = 94.4 and Bi/(Bi+Sb) = 0.23 correspond to lazerckerite (IMA2022-113).

The question arises how to evaluate samples from Kutná Hora with border values of Bi/(Bi+Sb), which for holubite with L% ≈ 70 is 0.19 and 0.45 (values encountered by EPMA by the first author of this article). The value of 0.19 still corresponds in all cases to holubite, whether the depletion of Bi occurs in M5 site (Ag increases, Bi decreases) or in the Bi4 site (which would become a Bi–Sb site with Bi ≥ Sb). Analytical points with the value of 0.45 are difficult to classify, because these fall in the substitution field of staročeskéite. Hypothetically, if all Ag in M5 is replaced by bismuth, Bi/(Bi+Sb) is equal to 0.36 then we may still deal with holubite. A further increase in Bi content would result most probably in one (or more) Sb sites to become an Sb–Bi mixed site with Sb ≥ Bi and the question arises whether such a phase would keep the a ≈ 19, b ≈ 13, c ≈ 8.5, β ≈ 90° and V ≈ 2200 cell of holubite or acquire the a ≈ 19, b ≈ 13, c ≈ 4.25 and V ≈ 1100 cell of staročeskéite (Pažout and Dušek, Reference Pažout and Dušek2010). This question can be answered only by single-crystal X-ray diffraction which could show unequivocally whether the halving of the 4.25 Å periodicity occurs or not.