Plumboperloffite, PbMn2+2Fe3+2(PO4)3(OH)3, is a new mineral and member of the bjarebyite group from Wiperaminga Hill West Quarry, Boolcoomatta Reserve, Olary Province, South Australia, Australia. The mineral was found in a single cavity in triplite–barbosalite matrix associated with fluorapatite, phosphosiderite, natrodufrénite and fluorite. The mineral forms intergrowths of subparallel, thin tabular to bladed crystals. Individual crystals are up to 40 μm in length. Plumboperloffite is brownish orange in colour with a vitreous lustre. The mineral has brittle tenacity, an excellent cleavage on {100} and uneven fracture. The calculated density is 4.416 g/cm3. Plumboperloffite is biaxial (+), α = 1.87(1), β = 1.88(1) and γ = 1.89(1) as measured in white light. The measured 2V is 88(1)°. Dispersion is apparently strong, based on extinction colours and the orientation is Y = b. The pleochroism in shades of yellow brown is X < Z < Y. Electron microprobe analysis gave the empirical formula (based on 15 O apfu) (Pb0.92Ca0.04Ba0.01K0.01)Σ0.98(Mn2+1.84Fe2+0.13)Σ1.97(Fe3+1.97Al0.03)Σ2.00(P3.01O11.94)(OH)Σ3.06. Plumboperloffite is monoclinic, space group P21/m with a = 9.1765(18), b = 12.340(3), c = 5.0092(10) Å, β = 101.01(3)°, V = 556.8(2) Å3 and Z = 2. The crystal structure has been refined using X-ray single-crystal data to a final R1 = 0.0207 on the basis of 1417 reflections with Fo > 4σ(Fo). The mineral is isostructural with members of the bjarebyite-group minerals.

Bjarebyite-group minerals are secondary phosphates that occur primarily in granitic pegmatites, but have also been found in the oxidised zones of ore deposits. Bjarebyite was first described from the Palermo No.1 pegmatite, New Hampshire, USA by Moore et al. (1973) and its atomic structure was determined by Moore and Araki (1974). The bjarebyite group currently consists of seven International Mineralogical Association (IMA) approved minerals (Table 1). The minerals have the general formula XM12M22(PO4)3(OH)3 where X = Ba, Sr, Pb; M1 = Fe2+, Mn2+, Mg and M2 = Al or Fe3+. Until the discovery of strontioperloffite (Elliott, 2019), all group members contained Ba as the dominant cation at the X site. The new mineral species, plumboperloffite, characterised and described in this paper, is the first member of the group with Pb dominant at the X site. The name is for the relationship to perloffite with Pb dominating the X site. The mineral and mineral name (symbol Pplf) have been approved by the International Mineralogical Association, Commission on New Minerals, Nomenclature and Classification (IMA2020-007, Elliott and Kampf, 2020). The type specimen is deposited in the South Australian Museum, Adelaide, South Australia, (Registration number G34868).

Plumboperloffite was found on a specimen collected in 2018 from the dumps of the Wiperaminga Hill West Quarry, Boolcoomatta Reserve, Olary Province, South Australia, Australia (140°27'34''E, 31°57'42''S). Pegmatites at Wiperaminga Hill were exploited for feldspar, beryl and muscovite between 1957 and 1980 (Olliver and Steveson, 1982). Four pegmatites were worked in three workings on Wiperaminga Hill West and Wiperaminga Hill East. Recorded production is 31.7 tonnes of beryl and 2030 tonnes of feldspar. The pegmatites occur near the base of a prominent range of hills which comprise banded quartz–mica gneiss and schist of the Early to Middle Proterozoic age Willyama Complex. The metasediments have been granitised and in many places are intruded by granite and associated pegmatite and aplite bodies. The pegmatites are usually small lenticular bodies varying from 6 m to 30 m in length and from 1 m to 3 m in width (Hiern, 1966). The pegmatites are mineralogically zoned and comprise an outer border zone of fine- to medium-grained microcline, quartz, plagioclase and muscovite, an intermediate zone of coarse-grained muscovite, quartz, microcline, plagioclase, beryl and apatite (and triplite), and an inner quartz core or cores (Lottermoser and Lu, 1997). The Wiperaminga Hill pegmatites belong to the beryl–columbite–phosphate rare-element type in the classification of Černý (1991). Phosphate minerals, dufrénite and florencite, were first reported from Wiperaminga Hill by King (1954), and Hiern (1966) reported apatite, triplite, dickinsonite and barbosalite. During a visit to the locality in 2018 by one of the authors (PE), masses of orange to dark brown triplite–zwieselite were found on the dumps of the eastern quarry. Secondary phosphate minerals have formed in seams and cavities in the triplite–zwieselite by hydrothermal alteration and weathering, in an oxidising, low-temperature, low-pH environment (Lottermoser and Lu, 1997). Plumboperloffite occurs in a single cavity in a matrix comprising triplite, barbosalite and minor quartz. Associated minerals are fluorapatite, phosphosiderite, natrodufrénite and fluorite.

Plumboperloffite occurs as thin tabular to bladed crystals, with a brownish-orange colour. Individual crystals are up to 40 μm in length (Fig. 1). The streak is pale orange and the mineral has a vitreous lustre. The hardness is estimated to be 4 based on the hardness of other bjarebyite-group minerals. The fracture is uneven, the tenacity is brittle and the mineral has an excellent cleavage on {100}. Density was not determined owing to the small amount of material available. The calculated density is 4.416 g/cm3 from the empirical formula. Plumboperloffite is optically biaxial (+) with indices of refraction α = 1.87(1), β = 1.88(1) and γ = 1.89(1) measured in white light. The 2V measured directly by conoscopic observation is 88(1)°. The calculated 2V is 90.5°. Dispersion is apparently strong, based on extinction colours, but the sense could not be determined because of the indistinct conoscopic figure. The pleochroism in shades of yellow brown is X < Z < Y. The optical orientation is Y = b. The optical orientation could not be completely determined because crystals are subparallel intergrowths and the refractive indices are high. The compatibility index 1 – (KP/KC) is 0.03 (excellent) based upon the empirical formula, density calculated using the single-crystal cell and the measured indices of refraction (Mandarino, 1981).

Analyses of plumboperloffite (12 spots) were performed with a Cameca SXFive electron microprobe (wavelength-dispersive spectroscopy mode, 20 kV, 20 nA and 5 μm beam diameter). Data were processed using the φ(ρZ) correction procedure of Pouchou and Pichoir (1991). There was insufficient material for direct determination of H2O content so it was based on the crystal structure analysis. The results of the analyses are reported in Table 2. The empirical formula unit, based on 15 O atoms per formula unit (apfu) is (Pb0.92Ca0.04Ba0.01K0.01)Σ0.98(Mn2+1.84Fe2+0.13)Σ1.97(Fe3+1.97Al0.03)Σ2.00(P3.01O11.94)(OH)Σ3.06. The ideal formula is PbMn2+2Fe3+2(PO4)3(OH)3 which requires PbO 29.19, MnO 18.55, Fe2O3 20.87, P2O5 27.86, H2O 3.53, total 100.00 wt.%.

The infrared spectrum of plumboperloffite (Fig. 2) was recorded using a Nicolet 5700 FTIR spectrometer equipped with a Nicolet Continuum IR microscope and a diamond-anvil cell. Data were acquired from a powdered sample during 50 scans in the wavenumber range 4000 to 700 cm–1. The spectrum shows bands at 3471 cm–1 and 3209 cm–1 that correspond to O–H-stretching vibrations of OH groups forming weak hydrogen bonds (Libowitzky and Beran, 2004). The bands at 1157, 1067, 989 and 898 cm–1 are assigned to ν3 vibrations of the PO4 tetrahedra and the band at 827 cm–1 is assigned to the ν1 vibration of the PO4 tetrahedra. No absorption attributed to H–O–H bending vibrations was observed in the spectrum.

Powder X-ray diffraction

Powder X-ray diffraction data for plumboperloffite were obtained using a Rigaku R-AXIS Rapid II curved-imaging-plate microdiffractometer, with monochromatised MoKα radiation (50 kV and 40 mA). A Gandolfi-like motion on the φ and ω axes was used to randomise the sample. Observed d values and intensities were derived by profile fitting using JADE 2010 software (Materials Data, Inc.). Data (in Å for MoKα) are given in Table 3. Unit-cell parameters refined from the powder data using JADE 2010 with whole-pattern fitting are a = 9.17(2), b = 12.41(2), c = 5.02(2) Å, β = 100.84(5)° and V = 561(3) Å3.

Single-crystal X-ray diffraction

The single-crystal X-ray diffraction experiment was carried out on the micro-focus macromolecular MX2 beamline at the Australian Synchrotron, part of ANSTO (Aragao et al., 2018). A crystal was attached to a MiTeGen polymer loop and X-ray diffraction data were collected at 100 K using a Dectris EigerX 16M detector and monochromatic radiation with a wavelength of 0.710754 Å. The intensity data sets were processed using XDS (Kabsch, 2010) without scaling and with absorption correction and scaling performed using SADABS (Bruker, 2001). Crystal data and experimental details are reported in Table 4.

Structure refinement

The structure was solved in space group P21/m using SHELXT (Sheldrick, 2015a) as implemented in the WinGX suite (Farrugia, 2012). SHELXL-2018 (Sheldrick, 2015b) was used for the refinement of the structure. Following the solution of the structure, the atom coordinates were transformed to correspond to those in the structure of perloffite (Elliott and Willis, 2011). Difference-Fourier syntheses then located all H atom positions. The H sites were refined with soft restraints on the O–H distances of 0.85(3) Å for the O–H groups and 0.90(3) Å. The final cycle of the refinement converged to R1 = 0.0207. Final atom coordinates and anisotropic-displacement parameters are listed in Table 5, selected interatomic distances and framework angles are given in Table 6, and bond-valence values, calculated using the parameters of Gagné and Hawthorne (2015) are given in Table 7. The crystallographic information file has been deposited with the Principal Editor of Mineralogical Magazine and is available as Supplementary material (see below).

Structure description

Plumboperloffite is isostructural with minerals of the bjarebyite group. The structure contains one X site (occupied by Pb and minor Ca, Ba and K), one M1 site (occupied by Mn2+ and minor Fe2+), one M2 site, (occupied by Fe3+ and minor Al) and two P sites. The M1 and M2 sites were refined with full occupancy of Mn and Fe, respectively.

[M2O3(OH)3] octahedra share edges to form [M2O6(OH)4] dimers which corner-link to form (M22Φ9) chains along the b-direction (Fig. 3). Octahedra that share corners are also linked by P1O4 tetrahedra. The chains are decorated by P2O4 tetrahedra, which link between chains in the c-direction via the O5 and O6 anions. Chains are linked in the a-direction via [M1O5(OH)] octahedra, which share an edge with [M23+O3(OH)3] octahedra and corners with P1O4 and P2O4 tetrahedra (Fig. 4). The X site occupies channels parallel to [001] and also provides linkage between chains in the a-direction. The X site exhibits a lop-sided coordination (Fig. 5) with three very short bonds to O1 and O7, four medium length bonds to O2, O4 and OH8, and six very long bonds to O5, O6 and O7. This coordination is distinct from the more regular coordination of the X site in the structures of other bjarebyite-group minerals and is attributable to the accommodation of the stereoactive 6s2 electron lone pair on Pb2+. Coordination of the M1 and M2 sites is similar to the sites in the structures of other bjarebyite-group minerals. The M1O6 octahedron is strongly distorted with bond angles in the range 86.35 to 109.53°. The M1O6 octahedron is relatively undistorted with bond angles in the range 86.77 to 96.22°.

The hydrogen bonding scheme for plumboperloffite given in Table 6, is the same as reported in previous studies on bjarebyite-group minerals (e.g. Cooper and Hawthorne, 1994; Elliott, 2019). The H9 atom associated with OH9 hydrogen bonds to O3 with a donor–acceptor distance of H9⋅⋅⋅O3 = 1.89(3) Å and an OH9–H2⋅⋅⋅O3 angle of 168(8)°, an arrangement typical of strong hydrogen bonding (Libowitzky and Beran, 2004). The H8 atom provides a weak hydrogen bond to O6 with a donor–acceptor distance of H8⋅⋅⋅O6 = 2.73(2) Å and an OH8–H8⋅⋅⋅O6 angle of 124(6)°.

The supplementary material for this article can be found at

The authors declare none.

The authors thank Ben Wade of Adelaide Microscopy, The University of Adelaide for assistance with the microprobe analysis. The infrared spectrum was acquired with the assistance of the Forensic Science Centre, Adelaide. This research was undertaken in part using the MX2 beamline at the Australian Synchrotron, part of ANSTO, and made use of the Australian Cancer Research Foundation (ACRF) detector.

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