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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.

Pericytes have the potential to be developed as a cell therapy for the treatment of wounds; however, the efficacy of any cell therapy relies on the successful delivery of intact and functioning cells. Here, the effect of delivering pericytes on wound repair was assessed alongside the development of a surface-functionalized pericyte patch. Plasma polymerization (PP) was used to functionalize the surface of silicone patches with heptylamine (HA) or acrylic acid (AA) monomers. Human pericytes were subsequently delivered to murine excisional wounds by intradermal injection or using the pericyte-laden patches and the comparative effects on wound healing, inflammation and revascularization determined. The AA surface provided the superior transfer of the cells to de-epidermized dermis. Excisional murine wounds treated either with pericytes injected directly into the wound or with the pericyte-laden AA patches showed improved healing with decreased neutrophil infiltration and reduced numbers of macrophages in the wounds. Pericyte delivery also enhanced angiogenesis through a mechanism independent of VEGF signalling. Pericytes, when delivered to wounds, improved healing responses by dampening inflammation and promoting angiogenesis. Delivery of pericytes using PP-AA-functionalized patches was equally as effective as direct injection of pericytes into wounds. Pericyte-functionalized dressings may therefore be a clinically relevant approach for the treatment of wounds.