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Tomiolloite (IMA2021-019) is a new aluminum tellurite sulfite-sulfate mineral discovered at the Bambolla mine, Moctezuma, Sonora, Mexico, a well-known tellurium (Te) mineral locality. Tomiolloite forms roughly spherical clusters of crystals comprised of very thin, needle-like crystals (1 μm diameter, ~40 μm length) around a core of small, stubbier, broken crystals. Tomiolloite is generally found growing on tellurite or quartz. The strongest powder X‑ray diffraction lines are [dobsÅ (Iobs) (hkl)]: 11.667 (89) (100), 8.240 (38) (101), 4.107 (29) (202,211,121), 3.223 (100) (203,302,130), and 2.905 (37) (213,123,222,400). The empirical formula of tomiolloite, as determined by electron microprobe analysis, is (Al10.64Te61.01+Fe30.31+Zn0.04)Σ12(Te45.00+Pb0.02)Σ5.02(S40.49+S60.49+Si0.02)Σ1.00O21.53[(OH)20.86Cl0.11]Σ20.97, which is simplified to the ideal formula Al12(Te4+O3)5[(SO3)0.5(SO4)0.5](OH)24. Significant Te6+substitution for Al3+is observed in tomiolloite, verified by X‑ray photoelectron spectroscopy and crystal-structure analysis. The structure of tomiolloite was determined using synchrotron single-crystal X‑ray diffraction, showing that tomiolloite is hexagonal and crystallizes in the space-group P63/m, with the unit-cell parameters a= 13.3360(19) Å, c= 11.604(2) Å, V= 1787.3(6) Å3, and Z = 2. Tomiolloite has a unique microporous framework structure, which bears a slight similarity to that of zemannite, but it has a much larger cavity diameter (8.85 Å). The framework is built from edge-sharing Mφ6octahedra (M= Al3+and Te6+), Te4+O3trigonal pyramids, and Te4+O4disphenoids. Mφ6octahedra edge-share to form crankshaft-shaped chains along c, with Te4+Onpolyhedra filling notches in the crankshafts and providing linkages between adjacent chains. The framework has an overall positive charge, which is balanced by the presence of both sulfite (SO32−) trigonal pyramids and sulfate (SO42−) tetrahedra in the channels.

For four decades fairbankite was reported to have the formula Pb2+(Te4+O3), but repeated attempts to isolate fairbankite crystals for structural determination found only the visually similar cerussite and, more rarely, anglesite. The crystal-structure determination of fairbankite using single-crystal X‑ray diffraction, supported by electron microprobe analysis and X‑ray powder diffraction on the type specimen, has shown that fairbankite contains essential S, along with Pb, Te, and O. The chemical formula of fairbankite has been revised to Pb122+Te4+O311SO4.$\mathrm{Pb}_{12}^{2+}\left(\mathrm{Te}^{4+} \mathrm{O}_{3}\right)_{11}\left(\mathrm{SO}_{4}\right).$This change has been accepted by the IMA–CNMNC, Proposal 19-I. The crystal structure of fairbankite [space group P1 (no. 1); revised cell: a= 7.0205(3) Å, b= 10.6828(6) Å, c= 14.4916(8) Å, a = 75.161(5)°, b = 81.571(4)°, g = 83.744(4)°, V= 1036.35(9) Å3, and Z= 1] is the first atomic arrangement known to contain a Te34+O96−$\mathrm{Te}_{3}^{4+} \mathrm{O}_{9}^{6-}$non-cyclic, finite building unit. Fairbankite has an average structure, formed from a 3D framework of Pb2+Onpolyhedra, Te4+Onpolyhedra, and SO4tetrahedra in a 12:11:1 ratio. The stereoactive lone pairs of the Pb2+and Te4+cations are oriented into void space within the structure. Fairbankite contains two mixed sites statistically occupied by Te4+and S6+in approximately 4:1 and 1:4 ratios. These two sites possess Te4+in trigonal-pyramidal environment and S6+in tetrahedral environment (with an additional O site to create tetrahedral SO4shape for the S-dominant site). Six of the 10 fully occupied Te4+sites have Te4+in trigonal-pyramidal environment, while four have Te4+at the center of highly distorted Te4+O4disphenoids. The disphenoids allow for the creation of two dimeric Te24+O64−$\mathrm{Te}_{2}^{4+} \mathrm{O}_{6}^{4-}$units in addition to the Te34+O96−$\mathrm{Te}_{3}^{4+} \mathrm{O}_{9}^{6-}$trimeric unit, which contains two disphenoids. All linkage between disphenoids and trigonal pyramids is via corner-linking. Secondary connectivity is via long Te–O and Pb–O bonds.

The classification and nomenclature of mineral species is regulated by the Commission on New Minerals, Nomenclature and Classification of the International Mineralogical Association (IMA-CNMNC). This mineral species classification is necessary for Earth Sciences, as minerals constitute most planetary and interstellar materials. Hazen (2019)has proposed a classification of minerals and other Earth and planetary materials according to “natural clustering.” Although this classification is complementary to the IMA-CNMNC mineral classification and is described as such, there are some unjustified criticisms and factual errors in the comparison of the two schemes. It is the intent of the present comment to (1) clarify the use of classification schemes for Earth and planetary materials, and (2) counter erroneous criticisms or statements about the current IMA-CNMNC system of approving proposals for new mineral species and classifications.

New zemannite-type phases, from Na 1.25 Fe 0.75 3 + Zn 1.25 ( Te O 3 ) 3 · 3 H 2 O to Na 0.55 Fe 1.44 3 + Zn 0.56 ( Te O 3 ) 3 · 3 H 2 O have been synthesised hydrothermally under basic conditions from a mixture of tellurium dioxide, zinc oxide, and either iron (III) oxide or iron (III) nitrate nonahydrate. Analysis by electron microprobe and inductively coupled plasma atomic emission spectrometry showed considerable variation in the Fe(III) and Zn contents of the framework. Single crystals of the compound produced from the iron (III) oxide syntheses were analysed, showing lower unit-cell parameters than natural zemannite, with a = 9.2620(9) and c = 7.6148(7) Å. The structure differs from type zemannite by the presence of Na and a water molecule which bridges the channel and framework by bonding via the oxygen atom. The unit-cell parameters of the compounds produced from iron (III) nitrate nonahydrate syntheses were refined from powder data and shown to increase with increasing pH. The results of this study show the potential for solid solution to exist in natural zemannite-type minerals and gives a stable boundary for the formation of pure zemannite-type compounds at basic pH levels, between pH 11.5 and pH 14.

The crystal structure of zemannite has been re-examined in order to address several features worthy of discussion. Analyses were performed on the type specimen and on material representative of Moctezuma. Type zemannite was found to refine in the space group P63 with a = 9.3877(5), c = 7.6272(4) Å and V = 582.12(7) Å3, whilst the unit-cell parameters in the same space group for the material representative of Moctezuma were a = 9.3921(13), c = 7.6230(15) Å and V = 582.3(2) Å3. The structural refinements undertaken were able to confirm for the first time the presence of a hydrogen bonding network in zemannite. An examination of the refinement of type zemannite in P63/m was also undertaken, showing that refining in the higher-symmetry space group does not show the ordering of framework octahedral metal cations. Zemannite-type minerals should therefore be refined in a non-centrosymmetric space group if possible, allowing the occupancies of the framework metal cations to refine. The chemical composition of zemannite was analysed by EMPA and by ICP-AES, showing conclusively that zemannite contains negligible Na, though the presence of Na should always be checked when analysing zemannite-type minerals. We also recommend that the formula of zemannite is revised to Mg0.5ZnFe3+(Te4+O3)3·(3 + n)H2O, where 0 = n = 1.5 from the current definition of Mg0.5ZnFe3+(Te4+O3)3·4.5H2O to better reflect the variable degree of hydration, since the type specimen is almost fully dehydrated and only contains three H2O molecules per formula unit.

Environmental context Cobalt is a technologically critical element due to its uses in the green energy transition, but its cycling is poorly constrained in surface environments. We determined the form of cobalt in naturally enriched soils and found that it is commonly associated with manganese as mixed oxide nanoparticles. These findings demonstrate that the behaviour of critical elements such as cobalt in the environment is in part governed at the nanoscale. Rationale Cobalt (Co) faces increasing demand for use in batteries and alloys, but its environmental behaviour in terrestrial surface environments is poorly constrained. This study analyses cobalt regolith mineralogy and nanoparticulate phase transitions to address this knowledge gap. Methodology We studied Co-enriched environments across six localities and four distinct deposit types in arid and semi-arid Australian regolith environments to analyse its environmental behaviour. We used a combination of single particle inductively coupled plasma–mass spectrometry (SP ICP-MS) and synchrotron X-ray techniques (fluorescence microscopy, X-ray flouresence microscopy and X-ray absorption spectroscopy). Results We discovered the presence of Co oxide-based nanoparticles in soils surrounding cobalt-rich rocks at all of our studied locations, to our knowledge the first detection of terrestrial Co oxide-based nanoparticles. The extractable concentration of Co in the nanoparticles varied from 0.7ng of nanoparticulate Co per gram of soil (ngCog–1 ), up to 1390ng Cog–1 , the latter soil containing 1 × 109 extractable Co-based nanoparticles per gram of soil. Discussion Nanoparticulate cobalt was typically closely associated with manganese (Mn) in the form of natural Co–Mn oxide phases, with only two of the studied locations not showing a close Co–Mn association. We discuss the environmental drivers that may facilitate formation of Co–Mn oxide nanoparticles. Our study suggests that Co may be more mobile in surface environments than previously thought, with Co–Mn oxide nanoparticles found around all four analysed types of Co-rich outcrops.

We report the characterisation of two new tetrahedrite-group minerals, rozhdestvenskayaite, Ag10Zn2Sb4S13, and argentotetrahedrite, Ag6Cu4(Fe2+,Zn)2Sb4S13, and discuss the structural chemistry of the Ag-rich tetrahedrite group in order to identify correlations between structure and composition. Argentotetrahedrite is the Sb-analogue of argentotennantite. Rozhdestvenskayaite is named for Irina Rodzhdestvenskaya in recognition of her important contributions to mineralogy, and to the crystal chemistry of the tetrahedrite group in particular. Rozhdestvenskayaite is cubic I 4 ¯ 3 m with unit-cell parameter a = 10.9845(7) Å and V = 1325.37(15) Å3, and has a Mohs’ hardness of 3.0. Argentotetrahedrite is cubic I 4 ¯ 3 m with unit-cell parameter a = 10.6116(1) Å and V = 1194.92(2) Å3, and has a Mohs’ hardness of 3.9. The five strongest peaks in the X-ray powder diffraction patterns ([(hkl), dobs (Å), I/Imax (%)]) are: rozhdestvenskayaite [(222), 3.161, 100], [(004), 2.738, 35], [(044), 1.936, 24], [(226), 1.651, 19], [(134,015), 2.147, 18]; argentotetrahedrite [(222), 3.063, 100], [(044), 1.876, 35], [(004), 2.652, 28], [(226), 1.599, 25], [(134,015), 2.081, 19]. The large unit-cell volume of rozhdestvenskayaite is due to the high Ag content (70%) of the BS4 tetrahedron. A major issue for understanding the crystal chemistry of the tetrahedrite group relates to the occupancy of the Z site in which sulfur is coordinated octahedrally to monovalent metals (Cu or Ag). It is shown that this site can be completely empty, as in freibergite, and that this vacancy leads to a marked reduction in the volume of the Z(A6) octahedron from 16 Å3 in tetrahedrite with a fully occupied site to 11 Å3 in freibergite with a vacant Z site. In freibergite, the Ag–Ag distance of the Ag6 octahedron is 2.84 Å and is almost the same as that of silver metal (2.85 Å), strongly suggesting the presence of metallic bonding in this octahedral group. In contrast, the corresponding Ag–Ag distances of argentotetrahedrite and rozhdestvenskayaite are 3.23 Å and 3.24 Å, respectively, indicative of no metallic bonding. An important consequence of the metallically bonded Ag6 group of freibergite is that it has an aggregate formal charge of +4 (not +6), leading to a charge-balanced ideal formula (Ag6)4+(Cu+)4(Zn,Fe2+)2Sb4S12.

We describe here the case of twinning by reticular (pseudo)merohedry in case of natural zippeite crystal from Cap Garonne, France. The twin is by two-fold rotation in [100] and it is a first document of this type of twinning in zippeite-related minerals and compounds. Zippeite crystals from Cap Garonne mine, France, were studied by single-crystal X-ray diffraction [a=8.7243(4), b=13.9337(7), c=8.8741(4) Å, β=104.243(5) and V=1045.59(9) Å3, Z=2, in C2/m]; refinement taking into account of the twinning resulted in R=2.81% for 1596 reflections with [I>3σ(I)] and refined twin fraction 0.7773(9):0.2227(9).

Wampenite, C18H16, is a new organic mineral from the fossil wood (conifer) locality at Wampen, Fichtelgebirge, Bavaria, Germany. It is monoclinic, space group P21/a, with a= 6.7331(19), b= 8.689(3), c= 23.709(7) Å, ß = 90.118(6)°, V= 1387.0(7) Å3 and Z= 4. Its structure was determined by single-crystal X-ray diffraction, which revealed that the molecular structure comprises an aromatic phenanthrene moiety with an axial methyl group at one end and a disordered propen-2-yl (methylvinyl) terminal group at the other. High resolution mass spectrometry (HRMS) confirmed the molecular formula C18H16and the IR spectrum is consistent with the molecular structure found.

We report the new mineral hydroxykenoelsmoreite, which has been approved by the IMA as IMA2016-056. The mineral occurs at the Masaka gold mine, Burundi, as rosettes up to 150µm across of platy crystals up to 20µm wide but <2µm thick, associated with goethite and galena. Crystals are canary yellow, transparent with a vitreous lustre, and have a pale yellow streak. Hydroxykenoelsmoreite is uniaxial (–) and non-pleochroic. The refractive indices were too high to measure, but the Gladstone-Dale compatibility index predicts nave= 2.065. Crystals are brittle with an irregular fracture, but have perfect cleavage on {0 0 1}. The Mohs hardness is ~3 by analogy with hydrokenoelsmoreite. The mineral is a member of the elsmoreite group of the pyrochlore supergroup, but deviates from the ideal cubic symmetry due mainly to ordering of Fe3+onto one of two W sites. Its structure is trigonal, space group R3, with unit-cell parameters a= 7.313(2), c= 17.863(7) Å, V= 827(1) Å3and Z= 6. The empirical formula (based on 7 (O + OH) per formula unit (pfu)) is: ([] 1.668Pb0.315Ca0.009Na 0.005K0.003Ba0.001)S2(W6+1.487Fe3+0.357Al0.156)S2(O4.119(OH)1.881)S6(OH). Raman spectroscopy and bond–valence sums showed that molecular H2O was absent or nearly so. The calculated density is 5.806 g cm-3.

Hydroxyferroroméite, ideally (Fe2+ 1.5[]0.5)Sb5+ 2O6(OH), is a new secondary mineral from the Correc d'en Llinassos, Oms, Pyrénées-Orientales Department, France. Hydroxyferroroméite occurs as yellow to yellow-brown powdery boxwork replacements up to about 50µm across after tetrahedrite in a siderite–quartz matrix. No distinct crystals have been observed. The empirical formula (based on 7 (O + OH) per formula unit, pfu) is (Fe2+ 1.07Cu2+ 0.50Zn0.03Sr0.03Ca 0.01[]0.36)S2 (Sb5+ 1.88Si0.09Al0.02As0.01)S2 O6 ((OH)0.86 O0.14). X-ray photoelectron spectroscopy was used to determine the valence states of Sb, Fe and Cu. Hydroxyferroroméite crystallises in the space group Fd3 m with the pyrochlore structure and hence is a new Fe2+ -dominant member of the roméite group of the pyrochlore supergroup. It has the unit-cell parameters: a = 10.25(3) Å, V = 1077(6) Å3 and Z = 8. A model, based on bond-valence theory, for incorporation of the small Fe2+ cation into a displaced variant of the A site of the pyrochlore structure is proposed.

Zincostrunzite (IMA2016-023), ZnFe3+; 2(PO4)2(OH)2· 6.5H2 O, is a new secondary phosphate mineral from the Sitio do Castelo tungsten mine in Portugal and the Hagendorf-Süd pegmatite in Germany. At Sitio do Castelo, zincostrunzite was derived from the alteration of triplite – zwieselite. At Hagendorf-Süd, it was found in a nodule of former triphylite that had been replaced by phosphophyllite and minor apatite. At Sitio do Castelo, zincostrunzite occurs as prisms up to 2 mm long. At Hagendorf-Süd, the mineral makes up portions of needles that are up to about 5 mm long. Crystals are elongated on [0 0 1] with the prism forms {0 1 0} and {1 1 0} and poorly formed terminations, probably {0 0 1}. Twinning is ubiquitous by 180° rotation on [0 1 0] with the composition plane {1 2 0}. Zincostrunzite crystals from Sitio do Castelo are light brownish yellow; those from Hagendorf-Süd are silvery white. The lustre is vitreous to silky and the streak is white. Crystals are brittle with irregular, splintery fracture and at least one perfect cleavage parallel to [0 0 1]; probably either {1 1 0} or {1 0 0}. The Mohs' hardness is about 2½. The measured density (Sitio do Castelo) is 2.66(1) g cm-3. At room temperature, the mineral is slowly soluble in dilute HCl and rapidly soluble in concentrated HCl. Optically, crystals are biaxial (-), with a = 1.620(2), ß = 1.672(2), ? = 1.720(2) (white light); 2 V meas. = 89.5(5)°; 2V calc. = 85.1°; orientation is Z ^c = 3°; X ˜ a*; pleochroism is X nearly colourless, Y light brownish yellow, Z darker brownish yellow (X < Y < Z). Electron-microprobe analyses gave the empirical formulas (Zn0.74 Mn2+ 0.23)S0.97 Fe3+ 1.99(PO4)2(OH)2·6.5H2 O (Sitio do Castelo) and (Zn0.93 Mn2+ 0.08)S1.01 (Fe3+ 1.84Mn2+ 0.19)S2.03 (PO4)2 (OH)2 ?6.5H2 O (Hagendorf-Süd). Zincostrunzite is triclinic, P -1, with a = 10.1736(6), b = 9.7999(5), c = 7.3296(2) Å, a = 91.325(4) °, ß = 97.895(6) °, ? = 116.948(4) °, V = 642.22(6) Å3 and Z = 2. The eight strongest lines in the X-ray powder diffraction pattern are [d obs/Å (I) (h k l)]: 8.87 (100) (100, 010, 1 1 0), 5.32 (95) (1 1 1, 011), 4.457 (30) (200), 4.287 (41) (020, 2 2 0), 3.310 (29) (120, 2 1 1), 3.220 (75) (multiple), 1.9116 (25) (multiple) and 1.6222 (32) (multiple). The crystal structure was refined to R 1 = 0.0715 for 3243 observed reflections [F o >4a F] for a crystal from Sitio do Castelo. The mineral is isostructural with other members of the strunzite group, except for an additional split H2 O site near the (½,0,0) centre of symmetry, which accounts for the additional 0.5 H2 O in the ideal formula. The extra H2 O site may be present in some crystals of other strunzite-group minerals, as its presence cannot be determined without a structure refinement.

Culture surfaces that substantially reduce the degree of cell manipulation in the delivery of cell sheets to patients are described. These surfaces support the attachment, culture, and delivery of multipotent adult progenitor cells (MAPC). It was essential that the processes of attachment/detachment to the surface did not affect cell phenotype nor the function of the cultured cells. Both acid-based and amine-based surface coatings were generated from acrylic acid, propanoic acid, diaminopropane, and heptylamine precursors, respectively. While both functional groups supported cell attachment/detachment, amine coated surfaces gave optimal performance. X-ray photoelectron spectroscopy (XPS) showed that at a primary amine to carbon surface ratio of between 0.01 and 0.02, greater than 90% of attached cells were effectively transferred to a model wound bed. A dependence on primary amine concentration has not previously been reported. After 48 h of culture on the optimized amine surface, PCR, functional, and viability assays showed that MAPC retained their stem cell phenotype, full metabolic activity, and biological function. Consequently, in a proof of concept experiment, it was shown that this amine surface when coated onto a surgical dressing provides an effective and simple technology for the delivery of MAPC to murine dorsal excisional wounds, with MAPC delivery verified histologically. By optimizing for cell delivery using a combination of in vitro and in vivo techniques, we developed an effective surface for the delivery of MAPC in a clinically relevant format.

Ferraioloite, MgMn2+ 4(Fe2+ 0.5Al3+ 0.5)4Zn4(PO4) 8(OH)4(H2O)20, is a new secondary phosphate mineral from the Foote Lithium Company mine, Kings Mountain district, Cleveland County, North Carolina, USA. The mineral was found in tiny vughs within a thin seam of very fine-grained, sugary pegmatite with vivianite, fairfieldite/messelite, phosphophyllite, scholzite/ parascholzite, rittmannite, mangangordonite, kingsmountite, kastningite and metaswitzerite. Ferraioloite crystals occur as very thin greenish grey to lemon yellow plates or blades up to about 0.2 mm in length, but no more than a few m m thick. Crystals are biaxial (À), with indices of refraction a = 1.575(calc), ß = 1.5825(5), ? = 1.5835(5), 2V (meas.) = 40(5). Dispersion is weak:r > v, the orientation is: X~ a, Y = b , Z ~ c and pleochroism: X, Z = colourless, Y = blue grey; Y> > X ~ Z. The empirical formula (based on 56 O atoms pfu) is Ca0.21 Mg0.50 Mn2+ 4.16Fe2+ 2.05Al3+ 2.01Zn 4.27P8.00H43.59O56. Ferraioloite is monoclinic, space group I2/ m, with the unit-cell parameters: a = 25.333(3) Å, b = 6.299(1) Å , c = 15.161(3) Å , b = 90.93(3) and V = 2419.0(2) Å3. Ferraioloite has a heteropolyhedral layer structure with layers parallel to (100) and with isolated Mg(H2 O)6 octahedra and water molecules packing between the layers. The heteropolyhedral slabs have the same topology as falsterite, with Mn2+ replacing Ca2+ and with Al3+ substituting for Fe3+.

Kayrobertsonite, MnAl2 (PO4)2 (OH)2·6H2 O, is a new secondary phosphate mineral from the Hagendorf Süd pegmatite, Hagendorf, Oberpfalz, Bavaria, Germany and the Foote Lithium Company mine, Kings Mountain district, Cleveland County, North Carolina, USA. Kayrobertsonite crystals occur as intergrown masses of snow-white, soft, finely fibrous needles, less than 5 µm in diameter and no more than 100 m m in length. Quantitative analysis of Foote mine kayrobertsonite gave the empirical formula: Mn0.97 Ca0.03 Fe0.02 Al1.87 (PO4)2 (OH)1.62 F0.03 (H2 O)0.38 6H2 O; and for Hagendorf Süd kayrobertsonite: Mn0.92 Ca0.06 Fe0.02 Al1.87 (PO4)2(OH)1.19 F0.42 (H2O)0.39 6H2 O. Foote mine kayrobertsonite crystals are biaxial (–), with indices of refraction a = 1.530(1), b = 1.554(1), g = 1.566(1), measured in white light; 2 V (meas.) is 70.3(5)°, while 2 V (calc.) is 69.6 . The mineral is nonpleochroic. The orientation of the crystals is Z ~ c (length slow). Kayrobertsonite is triclinic, space group P1, with the unit-cell parameters: a = 10.049(2), b = 10.205(2), c = 6.083(1) Å , a = 91.79(3), b = 99.70(3), g = 98.02(3)Å, V = 607.9(2) Å3 and Z = 2 (Foote mine). The polyhedral framework in kayrobertsonite has the same topology as that in nordgauite, but with replacement of F by OH at the bridging anion sites. The main crystal chemical change from nordgauite to kayrobertsonite is a doubling of the number of water molecules in the [001] channels.

Alfredopetrovite, Al2 (Se4+ O3)3 6H2 O, is a new secondary selenite mineral from the El Dragón mine, Antonio Quijarro Province, Potosí Department, Bolivia. The mineral occurs in vugs in a matrix of Co-rich krut'aite–penroseite, dolomite and goethite. Associated minerals are: ahlfeldite, allophane, calcite, chalcomenite, favreauite, felsobányaite, malachite and molybdomenite. Crystals occur in drusy/scaly coatings and compact balls, the latter to 0.5 mm in diameter. Individual crystals are up to about 0.1 mm across. The Mohs hardness of alfredopetrovite is 2½ it has no cleavage, curved fracture and a vitreous lustre. The calculated density based on the empirical formula is 2.504 g cm3. Alfredopetrovite is uniaxial (+), with ? = 1.554(2) and e = 1.566(2) (white light), and exhibits no pleochroism. Electron microprobe analyses gave the empirical formula Al1.94 Cu0.07 Ni0.03 Co0.01 Se2.95 O15 H12.16, based on 15 O apfu. Alfredopetrovite is hexagonal, space group P 6 2 c, with the unit-cell parameters: a = 8.818(3) Å , c = 10.721(2)Å , V = 722.0(5) Å 3and Z = 2. The eight strongest lines in the X-ray powder diffraction pattern are [d obs/Å (I) (hkl)]: 7.63(55)(100), 6.22(55)(101), 5.37(26)(002), 4.398(40)(110,102), 3.404(100)(112), 2.783(50)(211), 2.606(22)(203), and 1.6609(26)(410,322,314,116). The crystal structure was refined to R 1 = 0.0268 for 240 observed reflections [F o. > 4sF]. The structure is comprised of fairly regular AlO6 octahedra and Se4+ O3 triangular pyramids. Three Se4+ O3 pyramids link two adjacent AlO6 octahedra forming a [Al(H2O)3]2 (Se4+ O3)3 cluster structural unit. These structural units are bonded to one another only via hydrogen bonds yielding a structure with relatively large channels along [001]. The configuration of the cluster is similar to that of the distinctive unit in the NASICON structure, commonly referred to as a lantern unit.

Tellurium (Te) is a Critical Element that is toxic to microorganisms and humans alike, most notably in its soluble oxyanionic forms. To date, the biogeochemical behaviour of Te in Earth’s surface environment is largely unknown. Here, we report the discovery of elemental Te nanoparticles (Te NPs) in regolith samples using Single-Particle Inductively Coupled Plasma Mass Spectroscopy. Tellurium NPs were detected in both proximal and distal locations (bulk concentrations >4 ppm) relative to weathering Te ores. Synchrotron X-ray Fluorescence Mapping and X-ray Absorption Spectroscopy showed that bulk Te in the regolith is generally associated with Fe (oxyhydr)oxides and clay minerals, and mostly found in the oxidation states +IV and +VI. Although Te NPs account for less than 2 mol‰ of Te in our samples, their detection provides evidence for the active biogeochemical cycling of Te in surface environments. Te NPs are reactive and are likely to have formed in situ in distal samples, most likely via microbially-mediated reduction. Hence, the presence of Te NPs indicates the potential for release of toxic soluble forms of Te even in environments where most Te is “fixed” in forms such as Fe (oxyhydr)oxides that have low solubility and poor bioavailability.

The type specimen of partzite has been reinvestigated by powder X-ray diffraction and electron microprobe traverses. Re-examination of the type material shows that it is a mixture of several phases, intergrown on a submicrometre scale and hence not fully resolved by electron microprobe. Investigation of major-element spot analyses for correlations between elements indicates that the two dominant phases are a plumboroméite-like oxide phase and a chrysocolla-like amorphous Cu silicate. This analysis also suggested the presence of several minor phases that were too scarce to be detectable by X-ray diffraction, including acanthite, chlorargyrite, baryte, halite, and an Al-rich clay mineral. Lack of correlation between Si-corrected Cu content and Sb content implies that Cu is not a significant component of the roméite-group mineral. Partzite is therefore discredited as a valid mineral species. This proposal has been approved by the IMA CNMNC (proposal 16–B).

Apexite (IMA2015-002), NaMg(PO4)·9H2O, is a new mineral from the Apex mine, Lander County, Nevada, U.S.A., where it occurs as a low-temperature secondary mineral on massive quartz matrix in association with andersonite, calcite, čejkaite, gaylussite, and goethite. Apexite forms colorless needles up to 0.5 mm in length. The streak is white. Crystals are transparent and have vitreous to satiny luster. The Mohs hardness is about 2, the tenacity is brittle, the fracture is curved, and crystals exhibit one perfect cleavage on {100}. The measured density is 1.74(1) g/cm3and the calculated density is 1.741 g/cm3. Electron microprobe analyses provided: Na2O 9.26, MgO 14.42, P2O523.31, H2O 53.01 (structure), total 100.00 wt% (normalized). The empirical formula (based on 13 O apfu) is: Na0.91Mg1.09P1.00O13.00H17.91. Apexite is triclinic, P1̄, a = 6.9296(7), b = 11.9767(13), c = 14.9436(19) Å, α = 92.109(6), β = 102.884(7), γ = 105.171(7)°, V = 1160.9(2) Å3, and Z = 4. The eight strongest lines in the X‑ray powder diffraction pattern are [dobsin Å(I)(hkl)]: 14.63(35)(001); 5.11(61)(021,1̅1̅1,110,1̅20); 4.68(75)(02̅2,1̅1̅2,12̅1,01̅3); 4.301(96)(102,013,022,1̅13); 4.008(44) (1̅1̅3,12̅2); 2.876(46)(040); 2.762(100)(2̅1̅3,23̅1,03̅4,2̅04,015); and 2.507(30)(212,025,2̅2̅3). Apexite is a new struvite-type phase with a unique structure (R1= 4.44% for 1401 Fo> 4σF) consisting of four components: (1) a [Na2Mg4(H2O)14]10+heteropolyhedral cation cluster; (2) a trans edge-sharing chain of Na(H2O)6octahedra; (3) an isolated PO4group; and (4) an isolated H2O group. The structural components are linked to one another only via hydrogen bonds. Its structure is related to that of hazenite.

Favreauite, ideally PbBiCu6O4(SeO3)4(OH)·H2O, is a new secondary selenite mineral from the El Dragón mine, Antonio Quijarro Province, Potosí Department, Bolivia. The mineral occurs in vughs in a matrix of (Co, Cu)-rich penroseite, dolomite and goethite. Associated minerals are: ahlfeldite, allophane, calcite, chalcomenite, malachite, molybdomenite and an unnamed Al selenite. Favreauite forms tiny green square tabular crystals, flattened on {001}, up to 0.1 mm on edge and 0.01 mm thick, occurring in subparallel and divergent groups. The Mohs hardness of favreauite is estimated as ~3; it has perfect cleavage on {001}, an irregular fracture and a vitreous lustre. The calculated density based on the empirical formula is 4.851 g cm3. Favreauite is uniaxial (–), with mean refractive index estimated as 1.854 from the Gladstone–Dale relationship. It is pleochroic in shades of green, O < E. Electron microprobe analyses gave the empirical formula Pb0.95Ca0.17Bi0.90Cu5.81Se4.10O16(OH)·1H2O, based on 18 O pfu. The Raman spectrum shows strong SeO3 bands at 847 cm1 (?1), 764 and 795 cm1 (?3), 493 and 542 cm1 (?2), and 320 and 392 cm1 (?4). Favreauite is tetragonal, space group P4/n, with the unit-cell parameters: a = 9.860(4) Å, c = 9.700(5) Å, V = 943.0(9) Å3 and Z = 2. The eight strongest lines in the X-ray powder diffraction pattern are [d obs/Å (I) (hkl)]: 5.67(100)(111), 3.470(76)(220,202), 3.190(35)(003), 2.961(40)(311,113), 2.709(33)(302,203), 2.632(34)(231,312), 2.247(36)(331,133), and 1.6652(33)(305,513,531). The crystal structure was refined to R 1 = 0.0329 for 1354 observed reflections [F o < 4sF o] and 0.0356 for all 1432 unique reflections. Favreauite is a close structural relative of nabokoite, KCu7Te4+O4(SO4)5Cl, and atlasovite, KCu6Fe3+BiO4(SO4)5Cl. In all cases, oxygen-centred tetrahedra share edges to form corrugated [Cu6 MO4] layers (M = Bi or Te) which can be derived from the framework structure of murdochite, Pb4+Cu2+ 6O8-x (Cl,Br)2x by selective deletion of atoms. In favreauite, additional OH and H 2O between the layers are weakly bound to Cu, giving it Jahn-Teller distorted 4 + 2 coordination. The Cu–Bi–O layer is braced by SeO 3pyramids. The Bi3+ and interlayer Pb2+ form an approximately face-centred cubic array analogous to the Pb4+ sites in murdochite. Unlike Bi3+, Pb2+ is in a site with nonpolar 4 point symmetry, which suppresses the stereoactivity of its lone pair.

A sample of Sb-rich segnitite from the Black Pine mine, Montana, U.S.A., has been studied by microprobe analyses, single-crystal X-ray diffraction, and μ-EXAFS and XANES spectroscopy. Linear combination fitting of the spectroscopic data provided Sb5+:Sb3+= 85(2):15(2), where Sb5+is in octahedral coordination substituting for Fe3+and Sb3+is in tetrahedral coordination substituting for As5+. Based upon this Sb5+:Sb3+ratio, the microprobe analyses yielded the empirical formula Pb1.02H1.02(Fe3+2.36Sb5+0.41Cu2+0.27)Σ3.04(As5+1.78Sb3+0.07S6+0.02)Σ1.88O8(OH)6.00. The crystal structure refinement and bond valence analysis are consistent with these cation site assignments. The formation of Sb-rich segnitite opens new possibilities for Sb sinks within the supergene zone. Segnitite may, in fact, be an ideal host for the sequestering of several toxic elements for pH < 2. At higher pH values, As is more likely to be incorporated into schwertmannite and ferrihydrite.

The new mineral graţianite, MnBi2S4, is described from the Bǎiţa Bihor skarn deposit, Bihor County, Romania. Graţianite occurs as thin lamellae, intimately intergrown with cosalite and bismuthinite, or as flower-shaped blebs within chalcopyrite, where it is associated with cosalite and tetradymite. Graţianite displays weak to modest bireflectance in air and oil, respectively, and strong anisotropy. The mean empirical composition based on 20 electron probe microanalyses is: (Mn0.541Fe0.319Pb0.070Cu0.040Cd0.009Ag0.001)S0.980(Bi1.975Sb0.018)S1.993(S4.008Se0.012Te0.007)S4.027, corresponding to the ideal formula MnBi2S4. Graţianite crystallizes in the monoclinic system (space group C2/m). Single-crystal X-ray studies of material extracted by the focused ion beam-scanning electron microscopy (FIB-SEM) technique, and carried out on the MX2 macromolecular beamline of the Australian Synchrotron determined the following cell dimensions: a = 12.6774(25) Å, b = 3.9140(8) Å, c = 14.7581(30) Å, b = 115.31(3)°, V = 662.0(2) Å3, and Z = 4. The six strongest X-ray reflections and their relative intensities are: 3.448 Å (100), 2.731 Å (77), 2.855 Å (64), 3.637 Å (55), 3.644 Å (54), and 3.062 Å (51).

New data for parnauite from the type locality, Majuba Hill, Nevada, USA (MH; type specimen), and also from Cap Garonne, Var, France (CG), and the Clara Mine, Baden-Württemberg, Germany, are presented. The average chemical composition of MH material is (Cu8.82Al0.16Fe0.02)? 9.00(As1.78Al0.07Si0.08S0.07)? 2.00O8(SO4)(OH)10 · 7H2O and that of CG parnauite, (Cu8.42Al0.21Zn0.10)? 8.73(AsO4)2[(S0.97As0.10)? 1.07O4](OH9.23Cl0.77)? 10.00 · 7H2O. Both of these formulae confirm the 9:2:1 Cu:As:S ratio obtained from earlier descriptions of parnauite. Raman spectra for parnauite from both localities are very similar. Bands are assigned, but show no evidence of the presence of CO3, in contrast to previous studies, and no distinct Cu?Cl stretching mode. It appears that neither the minor CO3 and PO4 previously reported nor Cl are essential constituents of parnauite. Single-crystal XRD analysis indicates a primitive orthorhombic unit cell with dimensions 6 × 14 × 15 Å, similar to previous studies, but h = odd reflections were heavily streaked and diffuse, preventing full refinement. A 3 Å substructure was refined, with space group Pmn21, to R 1(F) = 0.0750 (MH). For a MH crystal, the subcell had a = 3.0113(4), b = 14.259(3), c = 14.932(2) Å, V = 641.13(16) Å3 and Z = 1. The structure is of a new type, and contains Cu in 6 distinct sites, forming two three-polyhedron wide ribbons of edge-sharing Cu-O polyhedra extended parallel to the a-axis. The two ribbons lie back-to-back and are bridged by two AsO4 tetrahedra. The collection of 6Cu + 2As cations plus ligands forms a rod-like moiety extended || a. These rods link through polyhedral corners to form complex, corrugated (010) layers. The interlayer space is occupied by H2O molecules. Thus, the disorder observed by XRD is of an unusual type, in which the shape of the unit mesh within layers is variable, rather than the stacking of the layers. Disorder arises because each AsO4 tetrahedron shares a face with a Cu(O, OH, H2O)5-6 polyhedron in the substructure, necessitating partial occupancy of both As and Cu sites. The S atoms were not located in the refinement, but four electron-density maxima in the interlayer region were interpreted as H2O molecules. Hence, the simplified structural formula derived from the substructure is (Cu10?2)(As2?2)O8(OH)148H2O, deviating from that obtained in chemical analyses. The discrepancy presumably arises due to strong delocalisation of the sulphur and the apical oxygen of the SO4 tetrahedron in the substructure. Short-range order of Cu?As and Cu?S || a can occur independently in the relevant structural rods, which accounts for the observed long-range disorder. Cell parameters and substructures obtained from CG and Clara material are similar to those from the MH crystal. Site splitting of OH positions in the CG refinement indicates that Cl is distributed over several sites in the 3 Å substructure, making the mineral a Clrich variety of parnauite rather than a distinct mineral species.

Single-crystal diffraction of jarosite, KFe33+(SO4)2(OH)6, has been undertaken at low temperatures that proxy for martian surface conditions. Room-temperature data are consistent with literature data [a = 7.2913(5), c = 17.1744(17), and V = 790.72(11) in R3¯m], while the first low-temperature data for the mineral is presented (at 253, 213, 173, and 133 K). Data collections between 297 and 133 K show strongly anisotropic thermal expansion, with the c axis much more expandable than the a axis. Much of the anisotropy is due to strong distortion of the KO12polyhedron, which increases by 8% between 297 and 133 K. The data sets can aid in the identification of jarosite by X-ray diffraction of martian soils using the Curiosity Rover’s CheMin instrument.

Eckhardite, (Ca,Pb)Cu2+Te6+O5(H2O), is a new tellurate mineral from Otto Mountain near Baker, California, U.S.A. It occurs in vugs in quartz in association with Br-rich chlorargyrite, gold, housleyite, khinite, markcooperite, and ottoite. It is interpreted as having formed from the partial oxidation of primary sulfides and tellurides during or following brecciation of quartz veins. Eckhardite is monoclinic, space group P21/n, with unit-cell dimensions a = 8.1606(8), b = 5.3076(6), c = 11.4412(15) Å, ß = 101.549(7)°, V = 485.52(10) Å3, and Z = 4. It forms as needles or blades up to about 150 × 15 × 5 mm in size, typically in radial or sub-radial aggregates, but also as isolated needles. The color is light bluish green and the streak is very pale bluish green. Crystals are transparent with vitreous to subadamantine luster. The Mohs hardness is estimated at between 2 and 3. Eckhardite is brittle with an irregular fracture and one likely (but not observed) cleavage on {101}. The calculated density based on the empirical formula is 4.644 g/cm3. The mineral is biaxial (-), with indices of refraction of a = 1. 770 (calc), ß = 1.860 (calc), and ? = 1.895(5). The measured 2V is 61.2(5)°, dispersion is r < v, perceptible and the optical orientation is Z = b; X ˜ [101]. The pleochroism is: Z (light blue green) < Y (very pale blue green) < X (colorless). The normalized electron microprobe analyses (average of 4) provided: PbO 4.79, CaO 15.90, MgO 0.06, CuO 22.74, Fe2O30.06, TeO351.01, H2O 5.45 (structure), total 100 wt%. The empirical formula (based on 6 O apfu) is: Ca0.962Pb0.073Cu2+0.971Mg0.005Fe3+0.002Te6+0.986O6H2.052. The Raman spectrum exhibits prominent features consistent with the mineral being a tellurate, as well as an OH stretching feature confirming a hydrous component. The eight strongest powder X-ray diffraction lines are [dobsin Å (hkl) I]: 5.94 (101) 100, 3.287 (112) 80, 2.645 (020,2¯13) 89, 2.485 (1¯14,301,014) 48, 2.245 (114,122) 46, 1.809 (223,4¯13,321,4¯04) 40, 1.522 (413,5¯12,421,133) 42, and 1.53 (2¯17,2¯33,4¯06) 43. The crystal structure of eckhardite (R1= 0.046 for 586 reflections with Fo> 4sF) consists of stair-step-like octahedral layers of Te6+O6and Cu2+O6octahedra parallel to {101}, which are linked in the [101¯] direction by bonds to interlayer Ca atoms. The structure can be described as a stacking of stepped HCP layers alternating with chains of CaO7polyhedra. The structures of bairdite, timroseite, and paratimroseite also contain stair-step-like HCP polyhedral layers.

Bairdite, Pb2Cu42+Te26+O10(OH)2(SO4)(H2O), is a new tellurate-sulfate from Otto Mountain near Baker, California, U.S.A. It occurs in vugs in quartz associated with khinite, cerussite, goethite, and hematite. It is interpreted as having formed from the partial oxidation of primary sulfides and tellurides during or following brecciation of quartz veins. Bairdite is monoclinic, space group P21/c, with unit-cell dimensions a = 14.3126(10), b = 5.2267(3), c = 9.4878(5) Å, b = 106.815(7)°, V = 679.41(7) Å3, and Z = 2. Bairdite occurs as diamond-shaped tabular crystals up to about 250 mm long and 5 mm thick, in subparallel and fan-shaped aggregates. The color is lime green, the streak is pale lime green, and the luster is adamantine. The Mohs hardness is estimated at between 2 and 3. Bairdite is brittle with an irregular fracture and one perfect cleavage on {100}. The calculated density based on the empirical formula is 6.062 g/cm3. Bairdite is biaxial (+), with calculated indices of refraction of a = 1.953, b = 1.966, and g = 2.039. The measured 2V is 47(2)°, dispersion is r < v, strong and the optical orientation is Y = b; Z ^ a = 34° in obtuse angle b. The pleochroism is strong: Z (pale green) <<< X (green) < Y (green). Electron microprobe analyses (average of 4) provided: PbO 34.22, CaO 0.06, CuO 23.80, TeO326.34, SO35.74, H2O 2.81 (structure), total 92.97 wt%. The empirical formula (based on 17 O atoms pfu) is: Pb2.05Ca0.01Cu2+3.99Te6+2.00S0.96O17.00H4.16. The eight strongest powder X-ray diffraction lines are [dobsin Å (hkl) I]: 4.77 (110,102) 50, 4.522 (002,011,111) 66, 3.48 (multiple) 62, 2.999 (311,411) 97, 2.701 (502,113,213) 79, 2.614 (013,020) 100, 1.727 (multiple) 65, and 1.509 (911,033,324) 83. The crystal structure of bairdite (R1= 0.072 for 1406 reflections with Fo> 4sF) contains edge-sharing chains of Te6+O6and Cu2+O6octahedra parallel to b that are joined by corner-sharing in the a direction, forming thick stair-step-like hexagonal close packed layers parallel to {100}. The polyhedral sheet has similarities to those in the structures of timroseite and paratimroseite. The thick interlayer region contains PbO10polyhedra and half-occupied SO4groups. Raman and infrared spectral data are presented

Fuettererite, Pb3Cu62+Te6+O6(OH)7Cl5, is a new tellurate from Otto Mountain near Baker, California, named for Otto Fuetterer who is largely responsible for the development of the mining claims on Otto Mountain. The new mineral is known from only two specimens, one from the NE2 vein and the other from the Bird Nest drift. Fuettererite occurs in vugs in quartz, on the first specimen associated with Br-rich chlorargyrite, iodargyrite, and telluroperite and on the second specimen associated with anglesite, anatacamite, atacamite, chalcopyrite, galena, goethite, hematite, muscovite, phosphohedyphane, timroseite, and wulfenite. It is interpreted as having formed from the partial oxidation of primary sulfides and tellurides during or following brecciation of quartz veins. Fuettererite is hexagonal, with space group R3¯, a = 8.4035(12), c = 44.681(4) Å, V = 2732.6(6) Å3, and Z = 6. Crystals are tabular to short prismatic, exhibit the forms {100}, {101}, and {001} and reach a maximum dimension of 50 µm. The color is bluish green, the streak is pale bluish-green, and the luster is adamantine. The Mohs hardness is estimated at between 2 and 3. The new mineral is brittle with irregular fracture and one perfect cleavage on {001}. The calculated density based on the empirical formula is 5.528 g/ cm3. Fuettererite is uniaxial (-), with calculated indices of refraction of ? = 2.04 and e = 1.97, and is dichroic bluish-green, E < O. Electron microprobe analysis provided: PbO 41.45, CuO 30.35, Al2O30.23, TeO312.80, Cl 12.08, H2O 3.55 (structure), O=Cl -2.73, total 97.73 wt%. The empirical formula (based on 18 O + Cl apfu) is: Pb2.88Cu2+5.92Al0.07Te6+1.13O6.59(OH)6.12Cl5.29. The ten strongest powder X-ray diffraction lines are [dobsin Å (hkl) I]: 6.106 (104) 44, 3.733 (0.0.12) 100, 2.749 (121¯) 53, 2.6686 (124¯) 49, 2.5289 (127¯) 41, 2.2772 (1.2.11) 38, 1.9637 (315, 1.2.1¯6¯) 87, 1.8999 (multiple) 48, 1.5976 (multiple) 40, and 1.5843 (410, 1.2.23, 143) 44. The crystal structure of fuettererite (R1= 0.031 for 971 reflections with Fo > 4sF) contains edge-sharing sheets of CuO5Cl and TeO6octahedra. These sheets are virtually identical to that in the structure of spangolite, but in fuettererite they are linked together to form a double sheet. The double octahedral sheets alternate with thick double layers of PbO2Cl6polyhedra. The CuO5Cl octahedra exhibit pronounced Jahn-Teller distortions and the PbO2Cl6polyhedron has a lopsided distribution of bond lengths attributable to the localization of the Pb2+6s2lone-pair electrons.

Agaite, Pb3Cu2+Te6+O5(OH)2(CO3), is a new tellurate from the Aga mine on Otto Mountain near Baker, California, U.S.A. The new mineral is known from only one specimen. It occurs on quartz in association with cerussite, Br-rich chlorargyrite, chrysocolla, goethite, khinite, markcooperite, muscovite, phosphohedyphane, timroseite, and wulfenite. It is interpreted as having formed from the partial oxidation of primary sulfides and tellurides during or following brecciation of quartz veins. Agaite is orthorhombic, space group Pca21, with unit-cell dimensions a = 10.6522(7), b = 9.1630(5), c = 9.6011(7) Å, V = 937.12(11) Å3, and Z = 4. Agaite crystals form as blades flattened on {010} and probably elongated on [001], and are up to about 20 µm thick and 200 µm in length. The color is blue, the streak is pale blue, and the luster is adamantine. The Mohs hardness is estimated at between 2 and 3. Agaite is brittle with an irregular fracture and one perfect cleavage on {010}. The calculated density based on the empirical formula is 6.987 g/cm3. Agaite is biaxial (-), with calculated indices of refraction of a = 2.015, ß = 2.065, and ? = 2.070°. The measured 2V is 34(5)° and the optical orientation is X = b, Y = c, and Z = a. It is pleochroic: X = pale blue, Y and Z = blue; X < Y = Z. Electron microprobe analyses (average of 4) provided: PbO 65.91, CuO 7.75, TeO317.41, CO24.33 (structure), H2O 1.78 (structure), total 97.18 wt%. The empirical formula (based on 10 O apfu) is: Pb3.00Cu2+0.99Te6+1.01O5(OH)2(CO3). The eight strongest powder X-ray diffraction lines are [dobsin Å (hkl) I]: 4.26 (012) 28, 4.165 (211) 14, 3.303 (022, 310, 221) 100, 2.7472 (131, 203, 312) 68, 2.571 (032, 401, 231) 14, 2.0814 (332, 422) 21, 2.0306 (511) 17, and 1.7468 (multiple) 40. The crystal structure of agaite (R1= 0.033 for 1913 reflections with Fo > 4sF) contains edge-sharing chains of Cu2+O5square pyramids and Te6+O6octahedra parallel to a that are joined by corner-sharing in the c direction, forming a polyhedral sheet parallel to {010}. The polyhedral sheet is very similar to those in the structures of timroseite and paratimroseite. The thick interlayer region contains 8- and 9-coordinated Pb2+, as well as CO3and OH groups. The Pb coordinations have lopsided distributions of bond lengths attributable to the localization of the Pb2+6s2lone-pair electrons.

Saltonseaite, K3NaMn2+Cl6, is a new mineral from the Salton Sea, Imperial County, California, U.S.A., which formed as the result of the evaporation of geothermal (hydrothermal) brines enriched in K, Na, Mn, and Cl. It occurs as lozenge-shaped and bladed crystals to about 10 cm that are composites of parallel-grown {012} rhombohedra. It is associated with large, well-formed crystals of sylvite and halite. Crystals are transparent and colorless, but appear light orange due to inclusions of akaganéite. The streak is white and the luster is vitreous to oily, the latter being due to deliquescence. The Mohs hardness is about 2½, the tenacity is brittle, the fracture is irregular, and crystals exhibit one very good cleavage on {110}. The mineral has an astringent taste and is markedly hygroscopic. The measured and calculated densities are 2.26(1) and 2.297 g/cm3, respectively. Saltonseaite is soluble in water at room temperature and crystallizes from solution above 52 °C. Optically, saltonseaite is uniaxial positive, with ? = 1.577(1) and e = 1.578(1) (white light) and is non-pleochroic. Energy-dispersive spectroscopic analyses (average of 5) provided: K 28.79, Na 5.35, Mn 13.48, Fe 0.24, Cl 52.19, total 100.05 wt%. The empirical formula (based on 6 Cl atoms) is: K3.00Na0.95Mn2+1.00Fe2+0.02Cl6. Saltonseaite is trigonal, R3¯c, with cell parameters a = 12.0966(5), c = 13.9555(10) Å, V = 1768.48(16) Å3, and Z = 6. The nine strongest lines in the X-ray powder diffraction pattern are [dobs in Å(I)(hkl)]: 5.83(61) (012); 3.498(25)(300); 2.851(68)(131); 2.689(32)(312); 2.625(62)(214); 2.542(100)(223); 1.983(32) (324); 1.749(20)(600), and 1.384(22)(multiple). The structure of saltonseaite (R1= 1.08% for 558 Fo> 4sF) contains face-sharing chains of alternating Mn2+Cl6octahedra and NaCl6polyhedra along c. The chains are joined via bonds to eight-coordinated K atoms. Saltonseaite is isostructural with rinneite, K3NaFe2+Cl6, and very similar in structure with chlormanganokalite, K4Mn2+Cl6. Existing chemical analyses for saltonseaite and rinneite fail to confirm a solid-solution series between them; experimental studies are needed.

Paseroite, ideally PbMn2+(Mn2+,Fe2+)2(V5+,Ti,Fe3+,)18O38, is a new mineral (IMA2011-069) from fossil wood in the upper part of the Molinello mine, Val Graveglia, Italy. Paseroite occurs in direct association with quartz, chalcocite, volborthite, metatyuyamunite and pyrophanite, and was also found as zones within V-rich senaite crystals with which it forms a solid-solution series. Paseroite forms as isolated submetallic, dark grey to black, elongated scalenohedral crystals between 50 and 100 m m in length, with the forms {001} and {102} present. The tenacity is brittle, the fracture conchoidal, and the streak is black. The Vickers hardness is 847 kg mm-2 (load 500g), which is equivalent to 6-6.5 on the Mohs scale. The calculated density is 4.315 g/cm3 (on the basis of the empirical formula). In plane-polarised incident light, paseroite is greyish in colour, weakly bireflectant and non-pleochroic. Internal reflections are absent. Between crossed polars, paseroite is anisotropic, without characteristic rotation tints. Reflectance percentages (Rmin and Rmax) are: 18.4 %, 18.2 % (471.1 nm); 17.9 %, 17.7 % (548.3 nm); 17.6 %, 17.3 % (586.6 nm); and 17.0 %, 16.8 % (652.3 nm), respectively. The empirical formula, calculated on the basis of 38 O atoms pfu is: (Pb0.61Sr0.39)S1.00 (V5+7.78Ti4+7.03Mn2+1.86Fe2+0.67Fe3+0.37Zn0.24Na0.19U0.02Mg0.022.82)S21.00O38. According to the structural results, the simplified formula is: PbMn2+(Mn2+,Fe2+)2(V5+,Ti,Fe3+,)18O38. Structurally, paseroite crystallises in the space group R3, with the unit-cell parameters a = 10.3894(5), c = 20.8709(8) Å, V = 1950.98(15) Å3 and Z = 3. The crystal structure was refined to R = 0.0234 for 632 reflections with Io > 2s(Io) and is isostructural with senaite and all other members of the crichtonite group. The eight strongest X-ray powder-diffraction lines [d in Å (I/I0) (hkl)] are: 3.417 (100) (024), 3.012 (21) (300), 2.896 (61) (216), 2.858 (36) (214), 2.765 (27) (303), 2.260 (85) (144), 2.149 (65) (415) and 1.809 (57) (418). The name is after Marco Pasero (b. 1958), Professor of Mineralogy at the University of Pisa.

The new mineral whelanite, Cu2Ca6[Si6O17(OH)](CO3)(OH)3(H2O)2, was approved by the Commission on New Minerals and Mineral Names (IMA) in 1977, but until now a description has not been published. The mineral is orthorhombic with space group Pn2n and cell parameters a = 5.6551(4), b = 3.683(3), c = 27.1372(7) Å, V = 565.3(5) Å3, and Z = 1. The mineral occurs with thaumasite, stringhamite, and kinoite in a copper-rich, diopside-garnet-magnetite skarn at the Bawana mine, Beaver County, Utah, and has also been confirmed to occur at other localities. At the Bawana mine, it is found as irregular clusters and radial aggregates of platy to lath-like crystals up to 1 mm in length, flattened on {001} and elongated on [100]. The color and streak are pale blue and the luster is vitreous. The laths are flexible, but not elastic. Cleavage is perfect on {001} and good on {010}, producing splintery fracture. The Mohs’ hardness is about 2½. The measured density is 2.74(3) g/cm3and the calculated density is 2.737 g/cm3based upon the empirical formula. The mineral is biaxial (-), α = 1.612(2), β = 1.622(calc), and γ = 1.626(2), and 2Vmeas= 64(1)°. The pleochroism is weak: X = Y (pale blue) < Z (light blue). The optical orientation is X = a, Y = c, Z = b. A combination of electron microprobe analyses and thermogravimetric analyses (for CO2and H2O) yielded: CaO 34.46, CuO 12.09, FeO 1.52, SiO237.96, CO25.93, H2O 8.86, total 100.82 wt%, providing the empirical formula (based on O = 26):

The new mineral reynoldsite, Pb2Mn4+2O5(CrO4), occurs at the Blue Bell claims, near Baker, San Bernardino County, California, U.S.A., and at the Red Lead mine, Dundas, Tasmania, Australia. At the Blue Bell claims, reynoldsite occurs in subparallel growths and divergent sprays of thin prisms with a square cross section. At the Red Lead mine, it occurs as thin rectangular blades. At both occurrences, crystals are small (≤0.2 mm), and ubiquitously and multiply twinned. At both deposits, reynoldsite formed as a secondary mineral derived from the weathering of primary minerals including oxides and sulfides in the presence of acidic groundwater. Reynoldsite is dark orange-brown to black in color and has a dark orange-brown streak. Its luster is subadamantine and its Mohs hardness is about 4½. The mineral is brittle with irregular to splintery fracture and a poorly developed {001} cleavage. The calculated density is 6.574 g/cm3(Red Lead mine). The very high indices of refraction and dark color permitted only partial determination of the transmitted light optical properties. Electron microprobe analyses of Blue Bell and Red Lead reynoldsite provided the empirical formulas (based on nine O atoms): Pb1.97Mn2.01O5(Cr1.01O4) and (Pb2.07Sr0.04)Σ2.11Mn2.15O5(Cr0.87O4), respectively. The strongest powder X-ray diffraction lines for Red Lead reynoldsite are [d(hkl)I]: 3.427(02̅1,110)52, 3.254(021,11̅2,12̅1)85, 3.052(1̅ 1̅2,111,02̅2,1̅03)100, 2.923(013,1̅22)40, 2.5015(004,2̅11,1̅30)47, 1.9818(01̅5,1̅05,202,23̅1)42, 1.7694(1̅15,13̅4,203,1̅42,1̅ 3̅3)36, and 1.6368(2̅2̅3,04̅3,221,124,22̅4)36. Reynoldsite is triclinic with space group P1 and unit-cell parameters: a = 5.0278(7), b = 7.5865(11), c = 10.2808(15) Å, α = 91.968(12), β = 99.405(12), γ = 109.159(10)°, V = 363.81(9) Å3, and Z = 2 (for a Red Lead mine crystal). The crystal structure of reynoldsite (R1= 10.2% for 902 reflections with Fo > 4σF for a Red Lead crystal) contains close-packed layers of edge-sharing Mn4+O6octahedra parallel to {001}. These layers are composed of edge-sharing double chains of octahedra extending along [100], which in turn are linked to one another by sharing edges in the [010] direction. The thick interlayer region contains Pb2+cations and CrO4tetrahedra. The 6s2lone-electron pair of the Pb2+is stereochemically active, resulting in a one-sided Pb-O coordination arrangement. The structure bears strong similarities to those of the phyllomanganates, such as chalcophanite and birnessite.

Chromschieffelinite, Pb10Te6O20(OH)14(CrO4)(H2O)5, is a new tellurate from Otto Mountain near Baker, California, named as the chromate analog of schieffelinite, Pb10Te6O20(OH)14(SO4)(H2O)5. The new mineral occurs in a single 1 mm vug in a quartz vein. Associated mineral species include: chalcopyrite, chrysocolla, galena, goethite, hematite, khinite, pyrite, and wulfenite. Chromschieffelinite is orthorhombic, space group C2221, a = 9.6646(3), b = 19.4962(8), c = 10.5101(7) Å, V = 1980.33(17) Å3, and Z = 2. Crystals are blocky to tabular on {010} with striations parallel to [001]. The forms observed are {010}, {210}, {120}, {150}, {180}, {212}, and {101}, and crystals reach 0.2 mm in maximum dimension. The color and streak are pale yellow and the luster is adamantine. The Mohs hardness is estimated at 2. The new mineral is brittle with irregular fracture and one perfect cleavage on {010}. The calculated density based on the ideal formula is 5.892 g/cm3. Chromschieffelinite is biaxial (-) with indices of refraction α = 1.930(5), β = 1.960(5), and γ = 1.975(5), measured in white light. The measured 2V is 68(2)°, the dispersion is strong, r < v, and the optical orientation is X = b, Y = c, Z = a. No pleochroism was observed. Electron microprobe analysis provided: PbO 59.42, TeO329.08, CrO31.86, H2O 6.63 (structure), total 96.99 wt%; the empirical formula (based on 6 Te) is Pb9.65Te6O19.96(OH)14.04(CrO4)0.67(H2O)6.32. The strongest powder X-ray diffraction lines are [dobsin Å (hkl) I]: 9.814 (020) 100, 3.575 (042,202) 41, 3.347 (222) 44, 3.262 (241,060,113) 53, 3.052 (311) 45, 2.9455 (152,133) 55, 2.0396 (115,353) 33, and 1.6500 (multiple) 33. The crystal structures of schieffelinite (R1= 0.0282) and chromschieffelinite (R1= 0.0277) contain isolated Te6+O6octahedra and Te26+O11corner-sharing dimers, which are linked into a three-dimensional framework via bonds to Pb2+atoms. The framework has large channels along c, which contain disordered SO4or CrO4groups and H2O. The lone-electron pair of each Pb2+is stereochemically active, resulting in one-sided Pb-O coordination arrangements. The short Pb-O bonds of the Pb2+coordinations are all to Te6+O6octahedra, resulting in strongly bonded layers parallel to {010}, which accounts for the perfect {010} cleavage.

A new occurrence of rankamaite is here described at the Urubu pegmatite, Itinga municipality, Minas Gerais, Brazil. The mineral forms cream-white botryoidal aggregates of acicular to fibrous crystals, intimately associated with simpsonite, thoreaulite, cassiterite, quartz, elbaite, albite, and muscovite. The average of six chemical analyses obtained by electron microprobe is (range in parentheses, wt%): Na2O 2.08 (1.95-2.13), K2O 2.61 (2.52-2.74), Al2O31.96 (1.89-2.00), Fe2O30.01 (0.00-0.03), TiO20.02 (0.00-0.06), Ta2O581.04 (79.12-85.18), Nb2O59.49 (8.58-9.86), total 97.21 (95.95-101.50). The chemical formula derived from this analysis is (Na1.55K1.28)Σ2.83(Ta8.45Nb1.64Al0.89Fe3+0.01Ti0.01)Σ11.00[O25.02(OH)5.98]Σ31.00. Rankamaite is an orthorhombic “tungsten bronze” (OTB), crystallizing in the space group Cmmm. Its unit-cell parameters refined from X‑ray diffraction powder data are: a = 17.224(3), b = 17.687(3), c = 3.9361(7) Å, V = 1199.1(3) Å3, Z = 2. Rietveld refinement of the powder data was undertaken using the structure of LaTa5O14as a starting model for the rankamaite structure. The structural formula obtained with the Rietveld analyses is: (Na2.21K1.26)Σ3.37(Ta9.12Nb1.30Al0.59)Σ11.00[O26.29(OH)4.71]Σ31.00. The tantalum atoms are coordinated by six and seven oxygen atoms in the form of distorted TaO6octahedra and TaO7pentagonal bipyramids, respectively. Every pentagonal bipyramid shares edges with four octahedra, thus forming Ta5O14units. The potassium atom is in an 11-fold coordination, whereas one sodium atom is in a 10-fold and the other is in a 12-fold coordination. Raman and infrared spectroscopy were used to investigate the room-temperature spectra of rankamaite.

Yttriaite-(Y), ideally Y2O3, is a new mineral (IMA2010-039) from the alluvial deposits of the Bol’shaya Pol’ya River, Subpolar Urals, Russia. The new mineral occurs as isolated crystals, typically cubo-octahedra <6 μm in size, embedded in massive native tungsten. Associated minerals include: copper, zircon, osmium, gold, and pyrite. The main forms observed are {100} and {111}. Due to the crystal size, physical properties could not be determined; however, the properties of synthetic Y2O3are well known. Synthetic Y2O3crystals are colorless to white with a white streak; crystals are transparent with an adamantine luster, while massive Y2O3is typically translucent with an earthy luster. Synthetic Y2O3has a Vickers hardness of 653.91, which corresponds to 5.5 on the Mohs scale. Synthetic Y2O3crystals have good cleavage on {111}. Yttriaite-(Y) is isotropic; the refractive index measured at 587 nm on synthetic Y2O3is n = 1.931. The empirical chemical formula (mean of 4 electron microprobe analyses) calculated on the basis of 3 O is: Y1.98Dy0.01Yb0.01O3. Yttriaite-(Y) is cubic, space group Ia3̅, with parameters a = 10.6018(7) Å, V = 1191.62(7) Å3, and Z = 16. The five strongest lines in the powder X-ray diffraction pattern (measured on synthetic Y2O3using synchrotron radiation) are [dobsin Å (I) (hkl)]: 3.0646 (100) (222), 1.8746 (55) (440), 1.5984 (38) (622), 2.6537 (26) (400), and 4.3356 (14) (211). The mineral name is based on the common name for the chemical compound, yttria.

Stichtite, ideally Mg6Cr2CO3(OH)16∙4H2O, from Stichtite Hill, Tasmania, Australia, and barbertonite, also ideally Mg6Cr2CO3(OH)16∙4H2O, from the Kaapsehoop asbestos mine, South Africa, have been studied by powder X-ray diffraction and their structures have been refined using the Rietveld method. Stichtite from Stichtite Hill crystallizes in the rhombohedral space group R3̄m, with unitcell parameters a = 3.09575(3) and c = 23.5069(6) Å, V = 195.099(6) Å3, with Z = 3/8. Barbertonite from the Kaapsehoop asbestos mine crystallizes in the hexagonal space group P63/mmc. The co-type specimens of barbertonite were found to be intergrown mixtures consisting of barbertonite and stichtite. Unit-cell parameters of barbertonite from the co-type specimens were a = 3.09689(6), c = 15.6193(8) Å, and V = 129.731(8) Å3and a = 3.09646(6), c = 15.627(1) Å V = 129.76(1) Å3, and Z = ¼. Rietveld refinements of both stichtite and barbertonite show that they are polytypes rather than polymorphs and do not represent distinct mineral species. Several possible nomenclature systems are discussed for the naming of hydrotalcite minerals and groups. Raman band assignments are also presented for stichtite from Stichtite Hill.

Telluroperite, Pb3Te4+O4Cl2, is a new tellurite from Otto Mountain near Baker, California. The new mineral occurs on fracture surfaces and in small vugs in brecciated quartz veins in direct association with acanthite, bromine-rich chlorargyrite, caledonite, cerussite, galena, goethite, and linarite. Various other secondary minerals occur in the veins, including six new tellurates, housleyite, markcooperite, paratimroseite, ottoite, thorneite, and timroseite. Telluroperite is orthorhombic, space group Bmmb, a = 5.5649(6), b = 5.5565(6), c = 12.4750(14) Å, V = 386.37(7) Å3, and Z = 2. The new mineral occurs as rounded square tablets and flakes up to 0.25 mm on edge and 0.02 mm thick. The form {001} is prominent and is probably bounded by {100}, {010}, and {110}. It is bluish-green and transparent, with a pale bluish-green streak and adamantine luster. The mineral is non-fluorescent. Mohs hardness is estimated to be between 2 and 3. The mineral is brittle, with a curved fracture and perfect {001} cleavage. The calculated density based on the empirical formula is 7.323 g/cm3. Telluroperite is biaxial (-), with very small 2V (~10°). The average index of refraction is 2.219 calculated by the Gladstone-Dale relationship. The optical orientation is X = c and the mineral exhibits moderate bluish-green pleochrosim; absorption: X < Y = Z. Electron microprobe analysis provided PbO 72.70, TeO219.26, Cl 9.44, O≡Cl -2.31, total 99.27 wt%. The empirical formula (based on O+Cl = 6) is Pb2.79Te4+1.03O3.72Cl2.28. The six strongest powder X-ray diffraction lines are [dobsin Å (hkl) I]: 3.750 (111) 58, 2.857 (113) 100, 2.781 (020, 200) 43, 2.075 (024, 204) 31, 1.966 (220) 30, and 1.620 (117, 313, 133) 52. The crystal structure (R1= 0.056) is based on the Sillén X1structure-type and consists of a three-dimensional structural topology with lead-oxide halide polyhedra linked to tellurium/lead oxide groups. The mineral is named for the relationship to perite and the dominance of Te (with Pb) in the Bi site of perite.

Timroseite, Pb2Cu52+(Te6+O6)2(OH)2, and paratimroseite, Pb2Cu42+(Te6+O6)2(H2O)2, are two new tellurates from Otto Mountain near Baker, California. Timroseite is named in honor of Timothy (Tim) P. Rose and paratimroseite is named for its relationship to timroseite. Both new minerals occur on fracture surfaces and in small vugs in brecciated quartz veins. Timroseite is directly associated with acanthite, cerussite, bromine-rich chlorargyrite, chrysocolla, gold, housleyite, iodargyrite, khinite-4O, markcooperite, ottoite, paratimroseite, thorneite, vauquelinite, and wulfenite. Paratimroseite is directly associated with calcite, cerussite, housleyite, khinite-4O, markcooperite, and timroseite. Timroseite is orthorhombic, space group P21nm, a = 5.2000(2), b = 9.6225(4), c = 11.5340(5) Å, V = 577.13(4) Å3, and Z = 2. Paratimroseite is orthorhombic, space group P212121, a = 5.1943(4), b = 9.6198(10), c = 11.6746(11) Å, V = 583.35(9) Å3, and Z = 2. Timroseite commonly occurs as olive to lime green, irregular, rounded masses and rarely in crystals as dark olive green, equant rhombs, and diamond-shaped plates in subparallel sheaf-like aggregates. It has a very pale yellowish green streak, dull to adamantine luster, a hardness of about 2½ (Mohs), brittle tenacity, irregular fracture, no cleavage, and a calculated density of 6.981 g/cm3. Paratimroseite occurs as vibrant “neon” green blades typically intergrown in irregular clusters and as lime green botryoids. It has a very pale green streak, dull to adamantine luster, a hardness of about 3 (Mohs), brittle tenacity, irregular fracture, good {001} cleavage, and a calculated density of 6.556 g/cm3. Timroseite is biaxial (+) with a large 2V, indices of refraction > 2, orientation X = b, Y = a, Z = c and pleochroism: X = greenish yellow, Y = yellowish green, Z = dark green (Z > Y > X). Paratimroseite is biaxial (-) with a large 2V, indices of refraction > 2, orientation X = c, Y = b, Z = a and pleochroism: X = light green, Y = green, Z = green (Y = Z >> X). Electron microprobe analysis of timroseite provided PbO 35.85, CuO 29.57, TeO327.75, Cl 0.04, H2O 1.38 (structure), O≡Cl -0.01, total 94.58 wt%; the empirical formula (based on O+Cl = 14) is Pb2.07Cu2+4.80Te6+2.04O12(OH)1.98Cl0.02. Electron microprobe analysis of paratimroseite provided PbO 36.11, CuO 26.27, TeO329.80, Cl 0.04, H2O 3.01 (structure), O≡Cl -0.01, total 95.22 wt%; the empirical formula (based on O+Cl = 14) is Pb1.94Cu2+3.96Te6+2.03O12(H2O)1.99Cl0.01. The strongest powder X-ray diffraction lines for timroseite are [dobsin Å (hkl) I]: 3.693 (022) 43, 3.578 (112) 44, 3.008 (023) 84, 2.950 (113) 88, 2.732 (130) 100, 1.785 (multiple) 33, 1.475 (332) 36; and for paratimroseite 4.771 (101) 76, 4.463 (021) 32, 3.544 (120) 44, 3.029 (023,122) 100, 2.973 (113) 48, 2.665 (131) 41, 2.469 (114) 40, 2.246 (221) 34. The crystal structures of timroseite (R1 = 0.029) and paratimroseite (R1= 0.039) are very closely related. The structures are based upon edge- and corner-sharing sheets of Te and Cu polyhedra parallel to (001) and the sheets in both structures are identical in topology and virtually identical in geometry. In timroseite, the sheets are joined to one another along c by sharing the apical O atoms of Cu octahedra, as well as by sharing edges and corners with an additional CuO5square pyramid located between the sheets. The sheets in paratimroseite are joined only via Pb-O and H bonds.

Markcooperite, Pb2(UO2)Te6+O6, is a new tellurate from Otto Mountain near Baker, California, named in honor of Mark A. Cooper of the University of Manitoba for his contributions to mineralogy. The new mineral occurs on fracture surfaces and in small vugs in brecciated quartz veins. Markcooperite is directly associated with bromian chlorargyrite, iodargyrite, khinite-4O, wulfenite, and four other new tellurates: housleyite, thorneite, ottoite, and timroseite. Various other secondary minerals occur in the veins, including two other new secondary tellurium minerals: paratimroseite and telluroperite. Markcooperite is monoclinic, space group P21/c, a = 5.722(2), b = 7.7478(2), c = 7.889(2) Å, β = 90.833(5)°, V = 349.7(2) Å3, and Z = 2. It occurs as pseudotetragonal prisms to 0.2 mm with the forms {100} and {011} and as botryoidal intergrowths to 0.3 mm in diameter; no twinning was observed. Markcooperite is orange and transparent, with a light orange streak and adamantine luster, and is non-fluorescent. Mohs hardness is estimated at 3. The mineral is brittle, with an irregular fracture and perfect {100} cleavage. The calculated density is 8.496 g/cm3based on the empirical formula. Markcooperite is biaxial (+), with indices of refraction α = 2.11, β = 2.12, γ = 2.29 calculated using the Gladstone-Dale relationship, measured α-β birefringence of 0.01 and measured 2V of 30(5)°. The optical orientation is X = c, Y = b, Z = a. The mineral is slightly pleochroic in shades of orange, with absorption: X > Y = Z. No dispersion was observed. Electron microprobe analysis provided PbO 50.07, TeO322.64, UO325.01, Cl 0.03, O≡Cl -0.01, total 97.74 wt%; the empirical formula (based on O+Cl = 8) is Pb2.05U0.80Te6+1.18O7.99Cl0.01. The strongest powder X-ray diffraction lines are [dobsin Å (hkl) I]: 3.235 (120, 102, 1̅02) 100, 2.873 (200) 40, 2.985 (1̅21, 112, 121) 37, 2.774 (022) 30, 3.501 (021, 012) 29, 2.220 (221, 2̅21, 212) 23, 1.990 (222, 2̅22) 21, and 1.715 (320) 22. The crystal structure (R1= 0.052) is based on sheets of corner-sharing uranyl square bipyramids and tellurate octahedra, with Pb atoms between the sheets. Markcooperite is the first compound to show Te6+substitution for U6+within the same crystallographic site. Markcooperite is structurally related to synthetic Pb(UO2)O2.

Ottoite, Pb2TeO5, is a new tellurate from Otto Mountain near Baker, California. Most of the mining on Otto Mountain occurred between 1940 and 1970 and is attributed to Otto Fuetterer, for whom the mountain is now named. The new mineral occurs on fracture surfaces and in small vugs in brecciated quartz veins, which intersect granitic rocks. Ottoite is directly associated with acanthite, bromine-rich chlorargyrite, gold, iodargyrite, khinite, wulfenite, and four other new tellurates: housleyite, markcooperite, thorneite, and timroseite. Various other secondary minerals occur in the veins, including two other new secondary tellurium minerals, paratimroseite and telluroperite. Ottoite and most other secondary minerals of the quartz veins are interpreted as having formed from the partial oxidation of primary sulfides and tellurides during or following brecciation of the veins. A later generation of quartz mineralization then recemented the breccias, effectively isolating and protecting the secondary mineralization from further alteration. Ottoite is monoclinic, space group I2/a, with the unit cell: a = 7.5353(6), b = 5.7142(5), c = 10.8981(12) Å, β = 91.330(6)°, V = 469.13(8) Å3, and Z = 4. The mineral occurs as complex spear-shaped crystals in subparallel to divergent intergrowths. It is yellow and transparent to translucent, with a pale yellow streak and adamantine luster. Mohs hardness is estimated at 3. The mineral is brittle, with an irregular fracture and two cleavages in the [100] zone at ~90°-possibly on {010} and {001}. The calculated density is 8.721 g/cm3. Ottoite is biaxial (-), with a large 2V, but indices of refraction are too high to be measured. The optic orientation could only partially be determined: Y ≈ a. No pleochroism was observed. Electron microprobe analyses provided the following averages: PbO 68.88 and TeO328.03, total 96.95 wt%; the empirical formula (based on O = 5) is Pb1.96Te6+1.01O5. The strongest powder X-ray diffraction lines are [dobsin Å (hkl) I]: 3.131 (2̅02) 64, 3.055 (013) 90, 3.015 (211) 100, 2.112 (2̅22) 29, 1.810 (006, 2̅15) 21, 1.773 (4̅11, 402) 43, 1.686 (033, 231) 20. The crystal structure (R1= 0.020) consists of straight chains of trans-corner-sharing Te6+O6octahedra parallel to a, which are joined by bonds to Pb atoms. The Pb atom exhibit markedly lopsided 11-coordination, typical of Pb2+with stereoactive 6s2lone-pair electrons. The powder X-ray diffraction pattern of ottoite is very similar to that reported for girdite. Examination of girdite type material suggests that its description was based upon data obtained from at least two and possibly three different phases, one of which may correspond to ottoite.

A study of the thermal decomposition sequence of a sample of natural arsenian plumbojarosite has been undertaken using in situ X-ray diffraction. The sample was heated to 900ºC using an Anton-Paar heating stage fitted to an INEL CPS120 diffractometer. The data were analysed using a whole-pattern, Rietveld based approach for the extraction of quantitative phase abundances. The instrument configuration used required the development and application of algorithms to correct for aberrations in the (i) peak intensities due to differing path lengths of incident and diffracted beams in the sample and (ii) peak positions due to sample displacement. Details of the structural models used were refined at selected steps in the pattern and then fixed for subsequent analysis. The data sequence consists of some 110 individual data sets which were analysed sequentially with the output of each run forming the input for analysis of the next data set. The results of the analysis show a complex breakdown and recrystallisation sequence including the formation of a major amount of amorphous material after initial breakdown of the plumbojarosite.

The TOPAS macro language can be a powerful tool for increasing the capabilities of X-ray powder diffraction analysis. New corrections and constraints can be implemented without altering the program's code, allowing for experimentation with new ideas and approaches. Examples are given, exposing the power and flexibility of the macro language to help solving problems with a few lines of code. The use of simulated annealing for structure solution of an organic material from data exhibiting preferential orientation is one example. Another one is about extraction of useful structural information in Rietveld refinement of natural hydrotalcite-group minerals, a problematic case that would normally be regarded as over-parameterized for the data available.

Kapundaite, ideally (Na,Ca)2Fe43+(PO4)4(OH)3∙5H2O, is a new mineral (IMA2009-047) from Toms phosphate quarry, Kapunda, South Australia, Australia. The new mineral occurs as cavernous aggregates of fibers up to several centimeters across, associated with leucophosphite, natrodufrenite, and meurigite-Na crystals and amorphous brown, black, and/or greenish coatings. Individual kapundaite crystals are very thin flattened fibers up to a few millimeters in length, but typically no more than a few micrometers in thickness. The main form observed is {100}; other forms in the [010] zone are present, but cannot be measured. Crystals of kapundaite are pale to golden yellow, transparent to translucent, have a yellow streak and silky luster, and are non-fluorescent. Mohs hardness is estimated to be about 3; no twinning or cleavage was observed. Kapundaite is biaxial (+), with indices of refraction α = 1.717(3), β = 1.737(3), and γ = 1.790(3). 2V could not be measured; 2Vcalcis 64.7°. The optical orientation is Z = b, Y ≈ c with weak pleochroism: X = nearly colorless, Y = light brown, Z = pale brown; absorption: Y > Z > X. No dispersion was observed. The empirical chemical formula (mean of seven electron microprobe analyses) calculated on the basis of 24 O is (Ca1.13Na0.95)Σ2.08(Fe3+3.83Mn0.03Al0.02Mg0.01)Σ3.89P3.92O16(OH)3·5H2.11O. Kapundaite is triclinic, space group P1, a = 6.317(5), b = 7.698(6), c = 9.768(7) Å, α = 105.53(1)°, β = 99.24(2)°, γ = 90.09(2)°, V = 451.2(6) Å3, and Z = 1. The five strongest lines in the powder X-ray diffraction pattern are [dobsin Å (I) (hkl)]: 9.338 (100) (001), 2.753 (64) (21̄1), 5.173 (52) (011), 2.417 (48) (2̄1̄3, 202, 01̄4), and 3.828 (45) (02̄1). The crystal structure was solved from single-crystal X-ray diffraction data using synchrotron radiation and refined to R1= 0.1382 on the basis of 816 unique reflections with Fo > 4σF. The structure of kapundaite is based on a unique corrugated octahedral-tetrahedral sheet, which is composed of two types of chains parallel to a. Kapundaite is structurally related to mélonjosephite. The mineral is named for the nearest town to the quarry.

Joëlbruggerite, ideally Pb3Zn3(Sb5+,Te6+)As2O13(OH,O), is a new arsenate mineral (IMA 2008-034) and the Sb5+analog of dugganite, from the Black Pine mine, 14.5 km northwest of Philipsburg, Granite County, Montana. It is usually found perched on mimetite; other species that may be present include malachite, azurite, pseudomalachite, chalcocite, beudantite-corkite, duftite, dugganite, and kuksite, in milky quartz veins. Joëlbruggerite occurs as barrel-shaped or prismatic crystals up to about 50 μm across in various shades of purple. The crystals have an adamantine luster and a white streak. Mohs hardness is about 3. The fracture is irregular, and the tenacity is brittle. Joëlbruggerite crystals are uniaxial (-), with a calculated refractive index of n = 1.993, and weakly pleochroic: X = Y = gray, Z = purple; absorption: Z > X = Y. Crystals show straight extinction and are length-fast. The empirical chemical formula (mean of 5 electron microprobe analyses) calculated on the basis of 14 [O + OH] anions is Pb3.112(Zn2.689Fe2+0.185)Σ2.874(Sb5+0.650Te6+0.451)Σ1.101(As1.551P0.203Si0.160)Σ1.914O13.335(OH)0.665. Joëlbruggerite is trigonal, space group P321, a = 8.4803(17), c = 5.2334(12) Å, V = 325.94(12) Å3, Z = 1. The five strongest lines in the powder X-ray diffraction pattern are [dobs in Å (I) (hkl)]: 3.298 (100) (111), 3.008 (89) (021), 1.905 (39) (122, 131), 2.456 (36) (012, 121, 030), and 1.609 (30) (112, 132, 231, 140). The crystal structure was solved from single-crystal X-ray diffraction data and refined to R1= 0.038 on the basis of 604 unique reflections with F > 4σ(F). It is composed of heteropolyhedral sheets of edge-sharing (Sb,Te)O6octahedra and PbO8disphenoids, oriented parallel to (001). The sheets are cross-linked by AsO4and ZnO4tetrahedra, which share corners to form an interlinked, two- and threeconnected two-dimensional net parallel to (001). The mineral is named for Joël Brugger (born 1967), Swiss-Australian mineralogist, for his contributions to mineralogy.