Introduction
The hematite-type structure occurs in a series of important compounds and was one of the first structures to be solved (Pauling and Hendricks, Reference Pauling and Hendricks1925). It is characterised by hexagonal close packing (hcp) of anions, with cations occupying ⅔ of octahedral cavities. Four minerals are isotypic with hematite: corundum and the rare mineral species eskolaite, karelianite and tistarite (Table 1). These minerals have space group R $\bar{3}$
c. The heterovalent substitution 2Me3+ = Me2+ + Ti4+ lowers the symmetry to R $\bar{3}$
, as observed in the ilmenite-group minerals (Table 1). The very rare mineral melanostibite is related to pyrophanite, an ilmenite-group mineral, through the coupled substitution 2Ti4+ = Fe3+ + Sb5+. This mineral was first reported by Igelström (Reference Igelström1893) from Sjögruvan, Örebro County, Sweden, under the name ‘melanostibian’ and later renamed melanostibite by Moore (Reference Moore1968a). Moore (Reference Moore1968a) demonstrated the relations between the ilmenite-group minerals and melanostibite, hypothesising that an ordered distribution of Fe3+ and Sb5+ may lower the symmetry to R3. However, the refinement of the crystal structure by Moore (Reference Moore1968b) suggested the possible R $\bar{3}$
space group, with a disordered distribution of Fe3+ and Sb5+. Since then, the crystal structure of melanostibite (as well as of its synthetic counterpart Mn2Fe3+Sb5+O6) was assumed as centrosymmetric and all the following investigations dealing with the study of its ferroelectric and ferromagnetic properties, showing potential technological applications, were based on Moore's structural model (e.g. Hudl et al., Reference Hudl, Mathieu, Nordblad, Ivanov, Bazuev and Lazor2013; Mathieu et al., Reference Mathieu, Ivanov, Solovyev, Bazuev, Anil Kumar, Lazor and Nordblad2013; Dos santos-García et al., Reference Dos santos-García, Solana-Madruga, Ritter, Andrada-Chacón, Sánchez-Benítez, Mompean, Garcia-Hernandez, Sáez-Puche and Schmidt2017; Liu et al., Reference Liu, Song, Li, Zhang, Mathieu, Ivanov, Skogby and Lazor2019).
Table 1. Hematite isotypic and homeotypic minerals.
[1] Ishizawa et al. (Reference Ishizawa, Miyata, Minato, Marumo and Iwai1980); [2] Logvinova et al. (Reference Logvinova, Wirth, Sobolev, Seryotkin, Yefimova, Floss and Taylor2008); [3] Blake et al. (Reference Blake, Hessevick, Zoltai and Finger1966); [4] Newnham and de Haan (Reference Newnham and de Haan1962); [5] Horiuchi et al. (Reference Horiuchi, Hirano, Ito and Matsui1982); [6] Mitchell and Liferovich (Reference Mitchell and Liferovich2004); [7] Liferovich and Mitchell (Reference Liferovich and Mitchell2006); [8] Bindi et al. (Reference Bindi, Chen and Xie2017); [9] Wechsler and Prewitt (Reference Wechsler and Prewitt1984); [10] this work. s.g. = space group.
Recently, a new occurrence of melanostibite was identified in the Scortico–Ravazzone Mn ore deposit, Apuan Alps, Tuscany, Italy. Single-crystal X-ray diffraction studies indicated the probably acentric nature of the Italian sample, suggesting the opportunity to undertake a re-examination of this species also using material from the Swedish type locality. Moreover, new electron microprobe and spectroscopic data were collected, improving the knowledge on this very rare but technologically interesting compound.
Experimental
Specimens studied
Two specimens of melanostibite were available for this study. The first one was collected by one of us (C.B.) in the dumps of the Scortico–Ravazzone Mn ore deposit, Apuan Alps, Tuscany, Italy, briefly exploited during the 1940s. Melanostibite occurs as euhedral pseudohexagonal tabular crystals, reddish-black in colour, up to 0.1 mm in size, associated with Mn-rich carbonates, rhodonite, baryte and sarkinite (Fig. 1). Other minerals occur in this assemblage and a study of the mineralogy of this small ore deposit is currently underway. The other specimen is from the type locality, Sjögruvan, Örebro County, Sweden and is housed in the Swedish Museum of Natural History under catalogue number GEO-NRM #18890293. Melanostibite occurs as thin mm-sized black platelets associated with hausmannite, dolomite and katoptrite in cross-cutting fissures in metamorphosed limestone.
Fig. 1. Melanostibite. (a) Tabular pseudohexagonal crystal, dark red in colour, with Mn carbonates and silicates. Scortico–Ravazzone, Fivizzano, Massa-Carrara, Tuscany, Italy. Private collection, photo C. Biagioni. (b) Back-scattered electron image of melanostibite from Sjögruvan, Örebro County, Sweden.
Chemical analysis
Quantitative chemical analyses were carried out using a Superprobe JEOL JXA 8200 electron microprobe (‘Eugen F. Stumpfl’ laboratory, Leoben University, Austria) using the following experimental conditions: wavelength dispersive spectroscopy mode, accelerating voltage = 20 kV, beam current = 10 nA and beam diameter = 1 μm. Counting times were 20 s on the peak and 10 s on the right and left backgrounds. Standards (element, emission line and diffracting crystals) were: magnetite (FeKα, LIFH), stibnite (SbLα, PETH) and rhodonite (MnKα, LIFH). The contents of other sought elements with Z > 8 (including Ti) were below detection limits. Matrix correction by the ZAF method was applied to the data. Results are given in Table 2.
Table 2. Chemical data for melanostibite and number of atoms per formula unit (apfu) based on O = 6 apfu.
n = number of spot analyses. e.s.d. = estimated standard deviation.
Mössbauer and micro-Raman spectroscopy
The 57Fe Mössbauer spectrum of melanostibite from Sjögruvan, for which sufficient homogeneous material was available, was collected at room temperature in transmission mode using a 57Co (in Rh matrix) point source, with a nominal activity of 0.40 GBq (Swedish Museum of Natural History, Stockholm, Sweden). Absorbers were prepared by gently grinding sample material (in the range 0.1–0.2 mg), which was placed in a ~2×2 mm square on a strip of tape and positioned closely in front of the point source. After calibrating the instrument against an α-Fe foil, the Mössbauer spectrum was acquired over the velocity range ±4 mm/s. The spectrum was fitted using the program MossA (Prescher et al., Reference Prescher, McCammon and Dubrovinsky2012). Hyperfine parameters are given in Table 3.
Table 3. Mössbauer hyperfine parameters for melanostibite from Sjögruvan.
Note: CS = centre shift; QS = quadrupole splitting; FWHM = full width at half maximum.
Micro-Raman spectra of melanostibite were collected on both samples using a Horiba Jobin-Yvon XploRA Plus apparatus (Dipartimento di Scienze della Terra, Università di Pisa), with a 50× long-working-distance objective lens and the 532 nm line of a solid-state laser. The spectrum of the Italian sample was collected on the unpolished sample shown in Fig. 1, whereas data on the Swedish melanostibite were collected on the polished sample used for electron microprobe data. The latter gave a better spectrum that is shown in Fig. 3. This spectrum was collected through three acquisitions with single counting times of 120 s. Back-scattered radiation was analysed with a 1200 cm–1 grating monochromator.
Single-crystal X-ray diffraction and structural refinements
Single-crystal X-ray intensity data were collected on both samples of melanostibite. Data for the Italian sample were collected using a Bruker Apex II diffractometer (50 kV and 30 mA) equipped with a Photon II CCD detector and graphite-monochromatised MoKα radiation (Dipartimento di Scienze della Terra, Università di Pisa, Italy). The detector-to-crystal distance was set at 50 mm. Data were collected using φ and ω scan modes in 0.5° slices, with an exposure time of 45 s per frame, and they were corrected for Lorentz, polarisation, absorption and background effects using the software package Apex3 (Bruker AXS Inc., 2016). The Swedish specimen was studied using a Bruker D8 Venture diffractometer (50 kV and 1.4 mA) equipped with a Photon III CCD detector and monochromatised MoKα radiation (Centro per l'Integrazione della Strumentazione scientifica dell'Università di Pisa, Università di Pisa, Italy). The detector-to-crystal distance was set at 38 mm. Data were collected using φ and ω scan modes in 0.5° slices, with an exposure time of 5 s per frame, and they were corrected for Lorentz, polarisation, absorption and background effects using the software package Apex4 (Bruker AXS Inc., 2022). The statistical tests on the distribution of |E| values gave |E 2 – 1| = 0.589 and 0.583 for the Italian and Swedish sample, respectively, thus suggesting the acentricity of melanostibite. Unit-cell parameters are a = 5.2351(3), c = 14.3645(8) Å and V = 340.93(4) Å3 for the sample from Scortico–Ravazzone, and a = 5.2314(2), c = 14.3518(8) Å and V = 340.15(3) Å3 for the specimen from Sjögruvan. In both cases, the space group is R3.
The crystal structure of melanostibite was solved through direct methods using Shelxs-97 and refined using Shelxl-2018 (Sheldrick, Reference Sheldrick2015). The following neutral scattering curves, taken from the International Tables for Crystallography (Wilson, Reference Wilson1992) were used: Sb vs. Fe at the M(1) and M(3) sites; Mn at M(2) and M(4) sites; and O at O(1) and O(2) sites. In the Italian sample, the M(1) and M(3) sites were found fully occupied by Fe and Sb, respectively and their occupancy was fixed to one. Table 4 gives details of data collection and refinement.
Table 4. Summary of crystal data and parameters describing data collection and refinement for melanostibite.
1 w = 1/[σ2(F o2)+(0.0159P)2]; 1/[σ2(F o2)+(0.0159P)2+0.6772P];
2Flack (Reference Flack1983)
Results and discussion
Chemical formula
Both samples of melanostibite have chemical compositions close to ideal. The empirical formula of the sample from Scortico–Ravazzone, recalculated on the basis of 6 O atoms per formula unit (apfu), is Mn1.98(Sb1.02Fe1.00)O6. The sample from Sjögruvan has chemical composition Mn1.96(Fe1.04Sb1.00)O6; possibly, very minor Fe2+ could occur, partially replacing Mn2+.
Mössbauer and micro-Raman spectroscopy
The Mössbauer spectrum of the sample from Sjögruvan shows only one quadrupole doublet (CS = 0.38 mm/s and QS = 0.64 mm/s) related to the occurrence of Fe3+ (Fig. 2). This is in agreement with the occurrence of Fe at a single site. The value of the centre shift suggests that Fe3+ occurs at a six-coordinated site.
Fig. 2. Mössbauer spectrum of melanostibite from Sjögruvan.
The micro-Raman spectra of melanostibite from Sjögruvan is shown in Fig. 3. The strongest bands occur between 550 and 700 cm–1, probably related to the symmetrical stretching of Fe–O and Sb–O bonds. Moreover, the band at 678 cm–1 can be assigned to Mn–O symmetric stretching modes, in agreement with Kharkwal et al. (Reference Kharkwal, Uma and Nagarajan2010). It is worth noting that in pyrophanite, as well as in other ilmenite-group minerals, only two bands occur in this spectral region (e.g. Ross and McMillan, Reference Ross and McMillan1984; Okada et al., Reference Okada, Narita, Nagai and Yamanaka2008; Kharkwal et al., Reference Kharkwal, Uma and Nagarajan2010), whereas three distinct bands can be identified in melanostibite. Dos santos-García et al. (Reference Dos santos-García, Solana-Madruga, Ritter, Andrada-Chacón, Sánchez-Benítez, Mompean, Garcia-Hernandez, Sáez-Puche and Schmidt2017) reported the Raman spectrum of synthetic Mn2FeSbO6, which looks very similar to that observed for its natural counterpart. However, in the Supporting Information of their work, these authors gave only two bands, at 594 and 663 cm–1, although a shoulder can be seen in their figure S7 that probably corresponds to the 678 cm–1 band observed in our study. Bands between 350 and 600 cm–1 can be attributed to bending vibrations of (Fe/Sb)-centred octahedra (e.g. Okada et al., Reference Okada, Narita, Nagai and Yamanaka2008; Dos santos-García et al., Reference Dos santos-García, Solana-Madruga, Ritter, Andrada-Chacón, Sánchez-Benítez, Mompean, Garcia-Hernandez, Sáez-Puche and Schmidt2017). Bands in the region below 350 cm–1 are probably related to lattice vibrations.
Fig. 3. Micro-Raman spectrum of melanostibite from Sjögruvan.
Crystal structure description
Fractional atomic coordinates and equivalent isotropic displacement parameters for melanostibite are given in Table 5, selected bond distances in Table 6 and bond-valence sums 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).
Table 5. Sites, Wyckoff positions, site occupancy factors (s.o.f.), fractional atom coordinates and equivalent isotropic displacement parameters (Å2) for melanostibite.
Table 6. Selected bond distances (Å) for melanostibite.
Table 7. Weighted bond-valence sums (in valence units) for melanostibite.*
* Note: right superscripts indicate the number of equivalent bonds involving cations. The following site populations were used: Scortico–Ravazzone M(1) = Fe3+, M(2) = Mn2+, M(3) = Sb5+ and M(4) = Mn2+; Sjögruvan M(1) = Fe3+0.97Sb5+0.03, M(2) = Mn2+, M(3) = Sb5+0.97Fe3+0.03 and M(4) = Mn2+. Bond valence units were calculated using the bond parameters of Gagné and Hawthorne (Reference Gagné and Hawthorne2015).
Melanostibite is homeotypic with ilmenite, and can be described as an hcp of O atoms with cations occupying ⅔ of the octahedral cavities. In the crystal structure there are four independent cation sites, namely M(1)–M(4), and two O sites: O(1) and O(2). Manganese is hosted at the M(2) and M(4) sites; average bond distances are 2.214 and 2.209 Å in the Italian sample, and 2.216 and 2.206 Å for the Swedish sample. Moore (Reference Moore1968b) reported an average bond distance of 2.209 Å for the Mn site of melanostibite, with values ranging from 2.110 to 2.309 Å. The observed values are in accord with the ideal <Mn2+–O> distance of 2.21 Å calculated using the ionic radii of VIMn2+ and IVO2– given by Shannon (Reference Shannon1976). In addition, bond-valence sums agree with the occurrence of Mn2+. Layers made by Mn-centred M(2) and M(4) octahedra alternate along c with ordered layers formed by Fe3+- and Sb5+-centred M(1) and M(3) octahedra (Fig. 4).
Fig. 4. Crystal structure of melanostibite: (a) as seen down a; and (b) details of the ordered M(1) + M(3) layer as seen down c.
Whereas the bonding environments of the M(2) and M(4) sites of melanostibite described in this work are very similar to the coordination of the Mn site of the crystal structure reported by Moore (Reference Moore1968b), interesting differences can be observed for the M(1) and M(3) sites. Indeed, in the R $\bar{3}$
structural model only one (Sb/Fe) site occurs, with average bond distance of 2.008 Å and single bonds ranging from 1.967 to 2.049 Å. Using the ionic radii given by Shannon (Reference Shannon1976), ideal <Fe3+–O> and <Sb5+–O> distances of 2.025 and 1.980 Å, respectively, can be calculated. The value observed by Moore (Reference Moore1968b) corresponds to a mixed (Fe3+0.5Sb5+0.5) site. In the R3 structure model, two symmetry-independent sites, namely M(1) and M(3) are present. The former has average bond distance ≈ 2.04 Å, whereas the latter shows an average distance of 1.99 Å. Such values, along with the refined site scattering, support an ordering of Fe3+ at the M(1) site and Sb5+ at the M(3) site, respectively. Bond-valence sums agree with such an ordering. Whereas the Italian sample shows pure Fe3+ and Sb5+ sites, the M(1) and M(3) sites of melanostibite from Sjögruvan seem to show a minor replacement of Fe3+ by Sb5+ at the M(1) site and vice versa at the M(3) position. In Table 5, the refined site occupancy factors are given; however, the substitution mechanism M (1)Fe3+ + M (3)Sb5+ = M (1)Sb5+ + M (3)Fe3+ is likely, owing to the necessity of maintaining the electrostatic balance. The site populations M (1)(Fe3+0.97Sb5+0.03) and M (3)(Sb5+0.97Fe3+0.03) are proposed for the calculation of bond-valence sums. The significance of these mixed site occupancies will be discussed below.
Oxygen atoms are four-fold coordinated; their bond-valence sums fully confirm the occurrence of O2– at these positions.
The structural formula of melanostibite can thus be written as M (2)(Mn1.00)M (4)(Mn1.00)M (1)(Fe1.00)M (3)(Sb1.00)O6 = Mn2Fe3+Sb5+O6 (Z = 3).
Ferric iron-Sb5+ disorder in melanostibite: a possible explanation
As discussed briefly in the Introduction, this study originated from the structural characterisation of a new finding of melanostibite from Italy, which suggested the acentric nature of this ilmenite-related mineral. When we studied the more abundant Swedish type material, a crystal of approximately 200 × 200 × 150 μm was examined through single-crystal X-ray diffraction. The collected data showed the occurrence of several individuals within the studied grain; however it was possible to collect data, refining the structure in the space group R $\bar{3}$
down to R 1 = 0.0321 for 102 unique reflections. Notwithstanding the |E 2 – 1| = 0.577, a reliable solution in the R3 space group was not obtained. A large number of systematic absence violations (1296, for a total of 1883 read reflections) suggested the opportunity to examine better crystals. Indeed, Moore (Reference Moore1968b) highlighted his difficulty in finding crystals suitable for single-crystal X-ray diffraction, because “most of the crystals were found to be not single but aggregates twinned by rotation on c {0001}” (Moore, Reference Moore1968b).
Using a smaller crystal (≈ 100 × 100 × 50 μm), better results were obtained. The crystal structure of melanostibite was refined in the space group R3 down to R 1 = 0.0092 for 512 unique reflections. No systematic absence violations were found. However, a partial disorder between Fe3+ and Sb5+ at the M(1) and M(3) sites was observed. The refined occupancies at these two sites were (Sb0.62Fe0.38) and (Fe0.64Sb0.36), respectively. This result was not in keeping with the Mössbauer data, that suggested a single Fe3+ site. However, the bond geometries of these two sites were very similar and could not be resolved through Mössbauer spectroscopy. M(1) and M(3) have average distances of 2.004 and 2.026 Å, with bond distances ranging between 1.96 and 2.05 Å at the M(1) site and 1.99 and 2.07 Å at the M(3) site. If structural data were correct, a possible hypothesis could be that melanostibite displays different degrees of Fe3+–Sb5+ ordering, maybe as a result of crystallisation temperature or kinetics factors. However, the sample from the Italian locality was collected in a Mn ore deposit that experienced greenschist metamorphism (up to 350–450°C and 0.4–0.8 GPa at the metamorphic peak – Molli et al., Reference Molli, Vitale-Brovarone, Beyssac and Cinquini2018 and references therein), and such values are probably not very different from the P–T conditions experienced by melanostibite from Sjögruvan. Holtstam and Mansfeld (Reference Holtstam and Mansfeld2001) suggested an upper temperature limit of 470°C for the Sjögruvan deposit, and in addition they suggested that the hydothermal fissures at the deposit were formed in the temperature range 100–350°C.
Finally, using a microfocus source, we were able to collect data on a very small crystal (30 × 30 × 15 μm) of melanostibite from Sweden, and the structure was found to be acentric, with a very limited amount of Fe3+–Sb5+ disorder between the M(1) and M(3) sites. As a relation between the size of the studied grains and the observed amount of Fe3+–Sb5+ disorder was observed, we suggest that melanostibite is actually an ordered R3 ilmenite homeotype; the Fe3+–Sb5+ mixed occupancy, as well as the apparent centrosymmetricity, probably result from the [0001] twinning and/or the possible occurrence of antiphase domains. Such kinds of defects are commonly reported in hematite- and ilmenite-type compounds (e.g. Tabata et al., Reference Tabata, Ishii and Okuda1981; Lawson et al., Reference Lawson, Nord, Dowty and Hargraves1981; Hojo et al., Reference Hojo, Fujita, Mizoguchi, Hirao, Tanaka, Tanaka and Ikuhara2009) and can also be the reason for the widespread twinning reported by Moore (Reference Moore1968b).
Conclusion
Melanostibite is a homeotypic derivative of pyrophanite, with Fe3+ and Sb5+ ordered in two symmetry-independent octahedrally-coordinated sites. In addition to contributing to a better knowledge of this very rare (but technologically interesting) species, this investigation also stresses the important role of the study of regional mineralogy. Indeed, the finding of a new occurrence of melanostibite from a small and forgotten locality in the Apuan Alps promoted a reinvestigation of this species using modern analytical techniques, resulting in the discovery of the acentric nature of this long-known but poorly-characterised mineral species.
Acknowledgements
CB acknowledges financial support from the Ministero dell'Istruzione, dell'Università e della Ricerca through the project PRIN 2017 “TEOREM – deciphering geological processes using Terrestrial and Extraterrestrial ORE Minerals”, prot. 2017AK8C32. CB and EB thank CISUP for the access to the single-crystal X-ray diffraction laboratory. The University Centrum for Applied Geosciences (UCAG) of the University of Leoben, Austria, is thanked for the access to the ‘Eugen F. Stumpfl’ electron microprobe Laboratory.
Supplementary material
To view supplementary material for this article, please visit https://doi.org/10.1180/mgm.2022.102
Competing interests
The authors declare none.
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