Introduction

Copper(II) hydroxychloride minerals are typical oxidation products of other copper minerals under arid conditions. This paper describes the first mixed-valency copper hydroxychloride mineral bounahasite, Cu⁺Cu²⁺₂(OH)₃Cl_2. Only two other minerals with both univalent and divalent copper cations are known – a rare secondary mineral paramelaconite Cu⁺₂Cu²⁺₂O₃ (O'Keeffe and Bovin, Reference O'Keeffe and Bovin1987) and a rare fumarolic mineral allochalcoselite Cu⁺Cu²⁺₅PbO₂(SeO₃)₂Cl₅ (Vergasova et al., Reference Vergasova, Krivovichev, Britvin, Filatov, Burns and Ananyev2005; Krivovichev et al., Reference Krivovichev, Filatov, Burns and Vergasova2006).

Bounahasite was named after its type locality – Bou Nahas Mine, Morocco. Both the new mineral and the name (symbol Bnhs) have been approved by the Commission on New Minerals, Nomenclature and Classification of the International Mineralogical Association, proposal IMA2021-114 (Lykova et al., Reference Lykova, Rowe, Poirier, Friis and Helwig2022). The holotype has been deposited in the collection of the Canadian Museum of Nature, Ottawa, Canada. The catalogue number is CMNMC 89874. A part of the holotype used for structure determination has been kept at the Natural History Museum in Oslo under catalogue number KNR 44404.

Occurrence and general appearance

Bounahasite occurs at the Bou Nahas (Bou N'hass) Cu Mine, Oumjrane mining area, Anti-Atlas Mountains, Morocco. It is a supergene mineral found in the oxidation zone of hydrothermal polymetallic veins. The veins were formed along faults and fractures in Upper Ordovician marlstones, shales, sandstones and conglomerates during hydrothermal activity related to late Triassic volcanism. The main minerals of the polymetallic veins are pyrite, chalcopyrite, galena and baryte. The secondary supergene mineralisation developed later, probably between Jurassic and Neogene periods (Praszkier, Reference Praszkier2015).

The new mineral forms very small pseudo-hexagonal plates up to 3 × 30 × 40 μm in size. The dominant form is pinacoid {110} with minor rhombic prism and another pinacoid. The crystals are combined into loose clusters (Figs 1–2) on native copper together in association with paratacamite.

Fig. 1.

Green platy crystals of bounahasite on native copper. FOV 1 mm. Specimen CMNMC 89874. Photo: François Génier.

Fig. 2.

Bounahasite crystals. Scanning electron microscopy image, scale bar = 10 μm.

Physical and optical properties

Bounahasite is green with pale green powder colour and vitreous lustre (Fig. 1). The cleavage is parallel to {110}, perfect. The fracture is uneven, stepped. The Mohs hardness could not be determined as the crystals are very small. The mineral is non-fluorescent under ultraviolet light. The density calculated using the empirical formula and unit-cell volume refined from the single-crystal X-ray diffraction data is 3.90 g/cm³.

Bounahasite is optically biaxial, 2V (meas.) = 60(5)° (from a spindle-stage extinction curve). The refractive indices were not measured due to the lack of available high refractive index (>1.8) immersion fluids. The mean refractive index obtained from the Gladstone–Dale relationship (Mandarino, Reference Mandarino1981) is 1.961.

Experimental methods

Electron microprobe analyses of bounahasite were obtained using a JEOL 8230 SuperProbe electron microscope equipped with five wavelength dispersive spectrometers (University of Ottawa – Canadian Museum of Nature MicroAnalysis Laboratory, Canada) with an acceleration voltage of 10 kV, a beam current of 10 nA and a beam diameter of 5 μm. The following reference materials were used: cuprite (CuLα) and tugtupite (ClKα). The intensity data were corrected for Time Dependent Intensity (TDI) loss (or gain) using a self-calibrated correction for ClKα.

The Fourier-transform infrared spectrum of bounahasite was obtained at the Canadian Conservation Institute, Canada using a Bruker Hyperion 2000 microscope interfaced to a Tensor 27 spectrometer with a wide-band mercury cadmium telluride (MCT) detector. A crystal of bounahasite ~20 μm in size was mounted on a low-pressure diamond anvil microsample cell and analysed in transmission mode. The spectrum was collected between 400–4000 cm^–1 with the co-addition of 150 scans at a 4 cm^–1 resolution.

Powder X-ray diffraction data were collected at the Canadian Museum of Nature, Canada using a Bruker D8 Discover microdiffractometer equipped with a DECTRIS EIGER2 R 500K detector and IμS microfocus X-ray source (λCuKα₁ = 1.54060Å) with the Kα₂ contribution removed using the ‘Strip Kα2’ tool in Bruker Diffrac.EVA V4.3. The instrument was calibrated using a statistical calibration method (Rowe, Reference Rowe2009). A powder ball 200 μm in diameter, mounted on a fibre pin mount, was analysed with continuous Phi rotation and 10° rocking motion along the Psi axis of the Centric Eulerian Cradle stage.

Single-crystal X-ray studies were carried out at room temperature on a Rigaku XtaLAB Synergy-S diffractometer equipped with a HyPix 6000HE detector (λCuKα = 1.54184) operating at 50 kV and 1 mA, housed at the Natural History Museum, University of Oslo, Norway. The data were collected and processed using Rigaku's CrysAlis Pro software.

Description and discussion of the crystal structure

The crystal structure of bounahasite is unique. It is based on two alternating sheets – octahedral and tetrahedral – coplanar to (110) (Fig. 4a,b). The octahedral sheet consists of alternating edge-sharing slightly Jahn–Teller-distorted Cu(2)²⁺(OH)₆ octahedra with a <Cu–O> distance of 2.133 and two octahedra coordinated by oxygen and chlorine: Cu(1)²⁺(OH)₄Cl₂ and Cu(3)²⁺(OH)₄Cl₂. Both Cu(1)- and Cu(3)-centred octahedra are strongly distorted with short equatorial Cu–O bonds with <Cu–O> distances of 1.960 and 1.974 Å, respectively, and elongated axial Cu–Cl bonds (Fig. 5a; Table 5). The distortion is attributed to the pseudo Jahn–Teller effect observed in Cu²⁺-centred octahedra with mixed ligands (Hathaway, Reference Hathaway1984). Ignoring the long Cu–Cl bonds, the sheet can be described as consisting of alternating edge-sharing Cu²⁺(OH)₆ octahedra and two Cu²⁺(OH)₄ squares.

Fig. 4.

General view of the crystal structure of bounahasite: (a) polyhedral and (b) ball-and-stick models. The unit cell is outlined. Projection on (001).

Fig. 5.

(a) Octahedral sheet in the crystal structure of bounahasite and (b) a similar sheet in the crystal structure of botallackite (after Hawthorne, Reference Hawthorne1985).

A similar sheet formed by alternating edge-sharing Cu(OH)₄Cl₂ and Cu(OH)₅Cl octahedra was found in the structure of botallackite, Cu₂(OH)₃Cl (Fig. 5b; Hawthorne, Reference Hawthorne1985).

The tetrahedral sheet is based on Cu(4)⁺Cl₄ tetrahedra (Fig. 6). Two edge-sharing Cu⁺Cl₄ tetrahedra form Cu⁺₂Cl₆ dimers connected with each other via shared vertices (Fig. 7). The Cu4 site is split onto the Cu4a and Cu4b subsites (Fig. 8) with the occupancy factors 0.9596(17) and 0.0404(17) and <Cu–Cl> distances of 2.364 and 2.449 Å, respectively. The Cu4a–Cu4b distance is 1.24 Å. There are several peaks and holes in the electron density map between the Cu4a and Cu4b sites, which indicates further splitting with multiple low-occupancy Cu4 subsites located near the Cu4a site.

Fig. 6.

Tetrahedral sheet in the crystal structure of bounahasite.

Fig. 7.

Cu⁺₂Cl₆ dimer connected with other dimers via shared vertices in the crystal structure of bounahasite.

Fig. 8.

Splitting of the Cu4 site into two subsites in the crystal structure of bounahasite.

The two sheets are connected via Cl1 atoms. The weak bonding between the sheets explains the perfect cleavage in one direction and the platy habit of bounahasite.

Structural analysis was crucial in determining both the number and the nature of the anions in the formula, as well as the valence state of copper. The bond-valence sums (BVS) at the O1 [1.23 valence units (vu)], O2 [1.26 vu], and O3 [1.29 vu; Table 6] sites indicate that all three sites are occupied by hydroxyl groups. H atoms were tentatively localised in the structure (Fig. 4b, Table 7). The distances between H and O atoms were restrained during refinement using a soft restraint (0.85 Å using the DFIX command). Hydrogen bonding between O atoms of the octahedral sheet and Cl2 atoms of the tetrahedral sheet (O–H⋅⋅⋅Cl) connects the sheets. Each Cl2 atom is involved in three hydrogen bonds (Table 7). The low BVS at the Cl2 site [0.53 vu; Table 6] is due to the unaccounted hydrogen bonds contribution.

Table 7.

Hydrogen bonds in the structure of bounahasite.*

*D = donor; A = acceptor

The BVS at the Cu1, Cu2 and Cu3 sites [2.16, 1.96 and 2.10 vu, respectively; Table 6] confirm the bivalent state of copper at those sites. Although, as discussed above, the splitting of the Cu4 site into multiple subsites complicates bond-valence calculations for both Cu and Cl sites, the results are unambiguous. The BVS calculated using bond-valence parameters taken for Cu²⁺–Cl bonds (Brese and O'Keeffe, Reference Brese and O`Keeffe1991) is 1.44 vu, whereas the parameters were taken for Cu⁺–Cl bonds give 0.96 vu, indicating that Cu⁺ is the dominant valence state of copper at the Cu4 site.

The resulting structural formula of bounahasite is Cu⁺Cu²⁺₂Cl₂(OH)₃.

No minerals or synthetic compounds structurally related to bounahasite have been found in the literature or databases. All five copper hydroxychlorides that have been found in Nature so far (atacamite Cu₂Cl(OH)₃, belloite Cu(OH)Cl, botallackite Cu₂Cl(OH)₃, clinoatacamite Cu₂Cl(OH)₃ and paratacamite Cu₃(Cu,Zn)Cl₂(OH)₆ [IMA-CNMNC List of Mineral Names, Pasero, Reference Pasero2022] contain only bivalent copper, and their structures are based on Cu-centred polyhedra with mixed Cl^– and OH^– ligands (Wells, Reference Wells1949; Fleet, Reference Fleet1975; Hawthorne, Reference Hawthorne1985; Grice et al., Reference Grice, Szymanski and Jambor1996; Pollard et al., Reference Pollard, Thomas and Williams1989; Krivovichev et al., Reference Krivovichev, Hawthorne and Williams2017; Zheng et al., Reference Zheng, Yamauchi, Kitajima, Fujihala, Maki, Lee, Hagihala, Torii, Kamiyama and Kawae2018).

It is rare to find Cu–Cl polyhedra in minerals and occurrences are usually structural types unique to each mineral, for example vertex-sharing Cu⁺Cl₄ tetrahedra in nantokite CuCl, which is a representative of the sphalerite structural type (Wyckoff and Posnjak, Reference Wyckoff and Posnjak1922), distorted octahedra Cu²⁺Cl₆ in tolbachite CuCl₂ (Burns and Hawthorne, Reference Burns and Hawthorne1993) or discrete planar dimers Cu²⁺₂Cl₆ in sanguite KCuCl₃ (Pekov et al., Reference Pekov, Zubkova, Belakovskiy, Lykova, Yapaskurt, Vigasina, Sidorov and Pushcharovsky2015). In this study, the tetrahedral sheet of bounahasite is no exception, as no sheet of a similar topology has been described before in either minerals or synthetic compounds. This implies that there is no preferential stable configuration of Cu–Cl polyhedra. All three minerals mentioned above – nantokite, tolbachite and sanguite – are unstable in air and alter into secondary minerals. Bounahasite has shown no signs of alteration so far, possibly due to the octahedral sheet stabilising the structure. The splitting of the Cu4 site into multiple subsites may play a similar role by relaxing the bonds and thus satisfying the local charge balance within the tetrahedral sheet.