The sulfide-free metasomatic rocks with chalcophile metals from the Ne & zcaron;ilovo ore field, near Veles, Republic of North Macedonia belong to a rare kind of ore. The mineralogy and petrology of these rocks were studied in detail and can be considered as a standard description for ores of this type. A characteristic feature of Ne & zcaron;ilovo-type ores is a wide variety of accessory oxide minerals containing chalcophile elements (Zn, Pb, Sb, Cu and As). The new nolanite-supergroup mineral zincorinmanite-(Zn), ideally (Fe3+2Zn)SbZnO7(OH), was discovered in the Ne & zcaron;ilovo ore. The associated minerals are quartz, baryte, gahnite, Zn-bearing phlogopite, together with accessory hematite, almeidaite, a Pb-analogue of hydroxycalciorom & eacute;ite and an insufficiently studied Sb-rich h & ouml;gbomite-supergroup mineral. Zincorinmanite-(Zn) forms lamellar to tabular subhedral single-crystal grains up to 0.5 mm across and up to 40 mu m thick. The colour and streak are black and the lustre is submetallic. The new mineral is brittle, with the Mohs' hardness of 6. No cleavage is observed. The fracture is uneven. The calculated density is 5.446 gcm-3. In reflected light, zincorinmanite-(Zn) is light grey, no pleochroism is observed. The reflectance values (Rmin, %/Rmax, %/lambda, nm) are: 12.6/13.7/470, 12.1/13.2/546, 11.8/12.8/589 and 11.5/12.2/650. The Raman spectrum shows bands corresponding to the O-H and Sb-O stretching vibrations and (Fe3+,M2+)-O-H bending modes. The chemical composition is (electron microprobe data, with iron divided into Fe2O3 and FeO based on the charge balance and H2O calculated from the structural data, wt.%): MgO 1.42, MnO 0.44, FeO 2.04, ZnO 22.55, Al2O3 1.95, Fe2O3 35.59, TiO2 1.51, Sb2O5 33.05, H2O 1.18, total 99.73. The empirical formula is [(Fe3+2.12Al0.18)(Zn0.32Mg0.16Fe2+0.13Mn0.03)Ti0.06]Sigma 3.00(Sb0.97Ti0.03)Sigma 1.00Zn1.00O7[(OH)0.61O0.39]Sigma 1.00. The crystal structure was determined using single-crystal X-ray diffraction data and refined to R = 0.0191. Zincorinmanite-(Zn) is hexagonal, space group P63mc, a = 5.9720(1), c = 9.3578(1) & Aring; and V = 289.031(8) & Aring;3 (Z = 2). The new mineral is isostructural with other members of the nolanite group. The strongest lines of the powder X-ray diffraction pattern [d, & Aring; (I, %) - hkl] are: 5.176 (46) - 100; 3.473 (77) - 102; 2.989 (46) - 110; 2.674 (86) - 103; 2.520 (100) - 112; and 2.496 (42) - 201.

A multimethodic approach based on infrared, Raman, electron spin resonance and photoluminescence spectroscopy, absorption spectroscopy in near infrared, visible and ultraviolet regions, single-crystal X-ray diffraction as well as electron microprobe analyses was applied to the characterization of a new commensurately modulated cubic haüyne analogue with the modulation parameter of 0.2 and unit-cell parameter of 45.3629(3) Å (designated as haüyne-45Å) from the Malobystrinskoe lazurite deposit, in the Baikal Lake area, Siberia, Russia, as well as associated SO32−-bearing afghanite. Haüyne-45Å is the second member, after vladimirivanovite, of the sodalite group with a commensurately modulated structure. The average structure is based on the tetrahedral aluminosilicate sodalite-type framework with sodalite cages of different sizes. The simplified formula of haüyne-45Å is Na6Ca2−x(Si6Al6O24)(SO42−,HS−,S2●−,S4,S3●−,S52−)2−y. The structural modulations of the haüyne-45Å framework are presumably related to the regular alternation of SO42− anions with polysulfide S2●−, S3●−, S4, and S52− groups detected by the spectroscopic methods. Mechanisms of thermal conversions of S-bearing groups in haüyne-45Å under oxidizing and reducing conditions at temperatures up to 800 °C are studied, and their geochemical importance is discussed.

Rerefinement of the crystal structure of the mineral tashelgite with the idealized formula CaMgFe2+Al9O16(OH) (orthorhombic Pbam space group; a = 17.1823(1), b = 23.5718(4), c = 5.6973(5) Å) is performed using the earlier obtained diffraction data. Fine crystal structure details and distribution features of cation positions are retrieved from precision Mössbauer and optical spectroscopy data. It is shown that the main motif and the pattern of cation distribution over octahedral and tetrahedral positions are preserved, despite the symmetry increase. However, due to a smaller number of independent positions, the distribution in the Pbam model becomes less ordered than in the Pc model. The appearance of tashelgite, having a complex structure based on spinel modules, agrees well with the presence of associated minerals such as spinel-like magnetite and hercynite, as well as hibonite, also containing spinel modules in its structure. A comparative crystal chemical and modular analysis of natural and synthetic compounds containing spinel modules is performed.

New data on the crystal structure, chemical composition, and nature of extra-framework components of the orthorhombic sodalite-group mineral vladimirivanovite were obtained using chemical and single-crystal X-ray diffraction data as well as infrared and Raman spectroscopy. The crystal structure of vladimirivanovite is based on the sodalite-type aluminosilicate framework with ordered Al and Si atoms. Sodalite-like cages are mainly occupied by Na+ and Ca2+ cations and (SO4)2− anions. It was shown that vladimirivanovite is characterized by significant variations in the content of extra-framework polysulfide groups (S3•−, S4), as well as other neutral molecules (H2O and CO2), the presence of which in the structure is the main cause of structural modulations and the orientation disordering of sulfate anions. Three samples with different S3•−:S4 ratios were studied. All of them are orthorhombic (space group Pnaa) with the unit-cell parameters a ≈ 9.1, b ≈ 12.9, and c ≈ 38.6 Å; Z = 6. The general crystal-chemical formula of vladimirivanovite is (Na+6.0–6.4Ca2+1.5–1.7)(Al6Si6O24)(SO42−,S3•−,S4)1.7–1.9(CO2)0–0.1·nH2O (n = 1–3), where the S4 molecule occurs in different conformation states.

An Erratum to this paper has been published: https://doi.org/10.1134/S1028334X23070073

Two mineral species of the labuntsovite group from Khibiny (sample 1) and Lovozero (sample 2) alkaline massifs are analyzed by single crystal X-ray diffraction and Raman spectroscopy. They are intermediate members of the tsepinite-Na–“tsepinite-Ba”–tsepinite-K solid solution, which are characterized by a high degree of hydration and a low concentration of extra-frame cations. Parameters of monoclinic cells are: a = 14.5086(6) Å, b = 14.2174(6) Å, c = 7.8712(3) Å, β = 117.119(4)°, V = 1444.09(11) Å3 (sample 1) and a = 14.2582(4) Å, b = 13.7541(6) Å, c = 7.7770(2) Å, β = 116.893(4)°, V = 1360.20(9) Å3 (sample 2). Crystal chemical formulas (Z = 2) are: |A[Na0.84K0.6[(H2O)4]5.2]BK0.2CBa0.25D[Ca0.35Na0.15Fe0.025(H2O)]| M1(Ti1.2Nb0.8)M2(Ti1.1Nb0.9)(O,OH)4(Si4O12)2 for sample 1 and |A[Na1.6(H2O,H3O)0.4]BK2C(Ba0.51Sr0.21)D [Mn0.3Ca0.2(H2O)](H2O)4|M1(Ti1.94Nb0.06)M2(Ti1.88Nb0.12)(O,OH)4(Si4O12)2 for sample 2. The high degree of hydration of sample 1 is expressed in the presence of proton hydrate complexes and tetrahedral [H2O]4-associates. Labuntsovite group minerals (LGMs) are characterized by so-called block isomorphism due to different distributions of D cations. Our analysis of heteropolyhedral MT-frameworks in LGMs allows us to determine the topological features of cation networks.

Lobanovite from the Koashva mountain in the Kibiny massif (Kola Peninsula) has been studied by methods of X-ray-spectral microanalysis, monocrystal X-ray diffractometry and IR-spectroscopy. Parameters of the lobanovite monoclinic unit cell: a = 5.3329(1), b = 23.1500(5), c = 10.3844(2) Å, β = 99.640(2)°, V = 1263.92(4) Å3; space group C2/m; crystal structure was refined to R = 2.8% with use of 1918 reflections with I 3σ(I). Crystal-chemical formula is as following (Z = 2): A(K0.93Ba0.01□0.06)2 B(Na0.95Ca0.05) [M1Na M2 (Mn0.445Fe2+0.275Na0.115Fe3+0.1Ca0.065)2 M3(Fe2+0.525Mg0.375Fe3+0.1)2 M4(Mg0.57Fe2+0.33Fe3+0.1)2 (OH)4] [D(Ti0.885Fe3+0.09Nb0.025)O(Si4O12)(ОН)0.1]2. In general, the studied sample of lobanovite is close to previously described ones, but it characterized by supplementary splitting in several bands if IR-spectrum. In D-position, together with titanium, there were for the first time revealed admixtures of iron and niobium, and in the inter-packet spаce – the partial replacement of sodium and potassium cations by barium and calcium. These facts were not mentioned in earlier publications. The article displays also some chemical and IR-spectroscopic data about {-ray-amorphous karnasurtite-like silicate and a rare-earths phosphate associated with lobanovite.

На основе полученных ранее дифракционных данных выполнено повторное уточнение кристаллической структуры минерала ташелгита с идеализированной формулой CaMgFe2+Al9O16(OH) в рамках ромбической пространственной группы Pbam (параметры элементарной ячейки: a = 17.1823(1), b = 23.5718(4), c = 5.6973(5) Å). Тонкие детали кристаллической структуры и особенности распределения катионов по позициям выполнены на основе прецизионных данных мессбауэровской и оптической спектроскопии. Установлено, что, несмотря на повышение симметрии, основной мотив и характер распределения катионов по октаэдрическим и тетраэдрическим позициям сохраняется. Тем не менее, из-за меньшего числа независимых позиций в модели пр.гр. Pbam распределение становится менее упорядоченным по сравнению с моделью пр.гр. Pc. Возникновение минерала ташелгита, характеризующегося сложной структурой, основу которой составляют шпинелевые модули, хорошо согласуется с наличием ассоциирующих минералов, в частности, магнетита и герцинита (структурный тип шпинели), а также хибонита, структура которого также содержит шпинелевые модули. Проведен сравнительный кристаллохимический и модулярный анализ природных и синтетических соединений, содержащих шпинелевые модули.

An Erratum to this paper has been published: https://doi.org/10.1134/S1028334X23070073

Методами рентгеноструктурного анализа и КР-спектроскопии были изучены два образца минералов группы лабунцовита из Хибинского (образец 1) и Ловозерского (образец 2) щелочных массивов – промежуточных членов твердого раствора цепинит-Na–«цепинит-Ba»–цепинит-K, которые характеризуются высокой степенью гидратации и низким содержанием внекаркасных катионов. Параметры моноклинных ячеек: a = 14.5086(6), b = 14.2174(6), c = 7.8712(3) Å, β = 117.119(4)°, V = 1444.09(11) Å3 (образец 1) и a = 14.2582(4), b = 13.7541(6), c = 7.7770(2) Å, β = 116.893(4)°, V = 1360.20(9) Å3 (образец 2). Кристаллохимические формулы (Z = 2): |A[Na0.84K0.6[(H2O)4]5.2]BK0.2CBa0.25D[Ca0.35Na0.15Fe0.025(H2O)]|{M1(Ti1.2Nb0.8)M2(Ti1.1Nb0.9)(O,OH)4(Si4O12)2} для образца 1 и |A[Na1.6(H2O,H3O)0.4]BK2C(Ba0.51Sr0.21)D[Mn0.3Ca0.2(H2O)](H2O)4|{M1(Ti1.94Nb0.06)M2(Ti1.88Nb0.12)(O,OH)4(Si4O12)2} для образца 2. Высокая степень гидратации образца 1 выражается в присутствии гидратных комплексов протона, а также тетраэдрических [H2O]4-ассоциатов. Для минералов группы лабунцовита характерен так называемый «блочный изоморфизм» связанные с различным распределением D-катионов. Проведенный нами анализ гетерополиэдрических МТ-каркасов в МГЛ позволил установить топологические особенности катионных сеток.

A potentially new mineral—structural analog of magnesiohögbomite-2N3S (Mg,Ti)8Al20O38(O,OH)2, containing Zn, Fe, Sb, and Mn as species-defining components, has been studied using electron-probe and X-ray diffraction analysis. The diffraction experiment was performed on a crystal presenting an aggregate of högbomite and nezilovite with close unit-cell parameters. The trigonal-cell parameters for the studied mineral are a = 5.8805(3) Å, c = 23.077(8) Å, V = 691.50(3) Å3, sp. gr. P 3̅ m1. The structural model was refined using a limited number of unique reflections (1165 reflections with F > 4σ(F)) to R = 0.068. The simplified formula Zn8(Mn2+,Mn3+)2Mg2(Sb0.65Mn _0.35^2 + )(Fe _5^3 + Sb1.0)(Fe _4.5^3 + Sb1.5)Al3O37(О,OН)3 (Z = 1) corresponds to the empirical one. The found distribution of cations over structural model sites is confirmed by the local charge balance. The mineral structure is based on layers of edge-sharing Fe3+ and Al octahedra. These layers alternate with heteropolyhedral layers of Zn tetrahedra, which combine octahedra centered by (Sb,Mn), Mn, and Mg.

The new eudialyte-group mineral amableite-(Ce), ideally Na-15[(Ce1.5Na1.5)Mn-3]Mn2Zr3 square Si[Si24O69(OH)(3)](OH)(2)& sdot;H2O, was discovered in a peralkaline pegmatite at Saint-Amable Sill, Mont & eacute;r & eacute;gie, Qu & eacute;bec, Canada. The associated minerals are albite, microcline, aegirine, serandite, natrolite, yofortierite, and an unidentified titanosilicate forming minute grains. Amableite-(Ce) occurs as yellow equant or thick tabular crystals up to 2 mm across. The observed crystal forms are {0001}; the subordinate forms are {110}, {101}, and {100}. Amableite-(Ce) is brittle, with a Mohs hardness of 5. D(meas) = 2.89(1), D(calc) = 2.899 g & sdot;cm(-3). Amableite-(Ce) is optically anomalously biaxial (+) with alpha approximate to beta = 1.603(2) and gamma = 1.608(2). The chemical composition is (wt.%, electron microprobe, H2O measured by means of a modified Penfield method): Na2O 14.20, K2O 0.41, CaO 1.89, MnO 8.25, Fe2O3 2.40, La2O3 3.10, Ce2O3 4.19, Pr2O3 0.16, Nd2O3 0.59, SiO2 49.41, ZrO2 11.17, HfO2 0.24, TiO2 0.68, Nb-2 & Ocy;(5) 1.54, Cl 0.26, H2O 1.70, -O equivalent to Cl -0.06, total 100.13. The crystal structure was determined using single-crystal X-ray diffraction data and refined to R1 = 0.0423. Amableite-(Ce) is trigonal, space group R3, with a = 14.1340(3) & Aring;, c = 30.3780(11) & Aring; and V = 5255.6(3) & Aring;(3). The crystal-chemical formula is (Na12.93K0.27Ce0.06)(Sigma 13.26)[(Mn2.49Ce0.30Ca0.21)(Sigma 3.00)(Ce1.14Na1.04Ca0.82)(Sigma 3.00)](Mn1.05Fe0.90 square(1.05))(Sigma 3.00)(Zr2.85Ti0.12Hf0.03)(Sigma 3.00)(square 0.40Nb0.36Si0.24)(Sigma 1.00)(Si-0.88 square(0.12))(Sigma 1.00)[Si-24(O-70.44(OH)(1.56))(Sigma 72.00)][(OH)(2.20)(H2O)(1.27)]Sigma Cl-3.47(0.22) (Z = 3). Infrared and Raman spectra are given. The strongest lines of the powder X-ray diffraction pattern [d, & Aring; (I, %)(hkl)] are: 11.34 (51)(101), 7.06 (76)(110), 4.312 (63)(205), 3.783 (38)(033), 3.538 (43)(027, 220), 2.963 (84)(45), 2.837 (100)(404). The mineral is named after the discovery locality.

Xenoliths in kimberlites are the most perspective objects for studying the composition and structure of the lower levels of the continental crust. Present work is aimed at estimation of P-T fluid conditions of metamorphism for garnet-biotite-feldspar and orthopyroxene-garnet-biotite-feldspar rocks represented as xenoliths in kimberlites of the Yubileynaya and Sytykanskaya pipes, Yakutian kimberlite province. Seven studied samples show inverse dependences of relative contents of garnet and orthopyroxene, orthopyroxene and biotite, garnet and plagioclase, plagioclase and potassium feldspar. This indicates a consistent series of transformations of the assemblage garnet + plagioclase + orthopyroxene ± quartz to the assemblage garnet + biotite + potassium feldspar. In this process, the replacement of plagioclase by potassium feldspar was the leading reaction. Now it is represented by specific reaction textures in the rocks, negative correlations of the mineral contents, as well as in petrochemical characteristics of the rocks. Modeling of xenolith mineral assemblages using the pseudosection approach (PERPLE_X) revealed two groups of rocks corresponding to different depth levels of the Siberian cratonic crust. For rocks where orthopyroxene is absent or is present as single relics, pressure estimates are 9.5–10 kbar, and it is 6–7 kbar for orthopyroxene-bearing samples. The xenolith rocks have close metamorphic peak temperatures of 750–800°C. They experienced 200–250°C cooling and 3–4 kbar decompression, regardless of the level of the crust at which they were initially located. This points to the metamorphic evolution of the rocks during their exhumation, probably associated with collisional processes during the amalgamation of individual terrains of the Siberian craton. Xenoliths enriched in K-feldspar might have been products of metamorphic reactions with participation of aqueous-(carbonic)-salt fluids, which were sourced from basaltic magmas in the lower crust. The most metasomatized rocks were located closest to the place of accumulation of crystallizing magmas.

Betzite, ideally Na6Ca2(Al6Si6O24)Cl4, a new cancrinite-group mineral, was discovered in a metasomatically altered (pyrometamorphosed) calcic xenolith, hosted by alkaline basalt at the Bellerberg paleovolcano in the Eastern Eifel region, Rhineland-Palatinate, Germany. The associated minerals are anorthite, phlogopite, diopside, grossular, fluorite, calcite, a tobermorite-like mineral, and vanadoallanite-(Ce). Betzite occurs as colorless hexagonal prismatic crystals up to 2 mm long and up to 0.5 mm thick. The new mineral is brittle, with a Mohs' hardness of 5½. Distinct cleavage on {100} and parting on {0001} are observed. The Dmeas = 2.38(2) g/cm3 and Dcalc = 2.363 g/cm3. Betzite is optically uniaxial (+) with ω = 1.528(2) and ε = 1.545(3). The IR spectrum is given. The chemical composition of betzite is (wt.%; electron microprobe, H2O determined by the modified Penfield method): Na2O 11.88, K2O 4.82, CaO 10.74, MgO 0.21, Al2O3 27.32, Fe2O3 0.68, SiO2 32.84, SO3 1.89, Cl 10.48, H2O 1.10, −O≡Cl −2.37, total 99.59. The empirical formula is Na4.22K1.13Ca2.11Mg0.06(Si6.01Al5.90Fe3+0.09O24)Cl3.25(SO4)0.26(H1.34O0.64). The crystal structure was determined using single-crystal X-ray diffraction data. It is hexagonal, space group P63, a = 12.8166(9) Å, c = 5.3562(3) Å, V = 761.95(12) Å3 (at a temperature of 100 K) and Z = 3. Betzite is a dimorph of quadridavyne, with a disordered distribution of extra-framework components occupying channels. The strongest lines of the powder X-ray diffraction pattern [d, Å (I, %) (hkl)] are: 11.14 (31) (100), 4.833 (93) (101), 3.715 (95) (300), 3.313 (100) (211), 2.787 (37) (400), 2.681 (56) (002, 131), 2.474 (35) (112, 401), 2.146 (24) (330). The mineral is named in honor of the German amateur mineralogist Volker Betz (b. 1947).

Synthesis of zirconosilicates from a stoichiometric mixture of Na2CO3, CaO, Fe2O3, ZrOCl2, and SiO2 with the Na : Ca : Fe : Zr : Si ratio belonging to the compositional area of eudialyte-geoup minerals (EGM), was carried out under high-alkaline conditions (in the presence of 1 M aqueous solutions of NaCl and 46% NaOH) at a temperature of 600 °C and a pressure of 2 kbar, for 10 days. In some experiments, natural raslakite (a Ca-deficient EGM) was used as a seed added in amount of 2 wt % of the whole charge. According to electron microprobe analyses, powder X-ray diffraction data and IR spectroscopy, high-alkaline EGM, zirsinalite, parakeldyshite, and aegirine were identified in the products of the syntheses carried out using a charge with relatively high Si : Zr, Fe : Zr and Na : Zr ratios. At relatively low values of these ratios, no EGM formed.

For the first time, a new noble-metal (Pt–Au–Pd) Vasilinovskoe ore occurrence discovered near the village of Kharp in the Yamalo-Nenets Autonomous Okrug is described. It is associated with amphibolized gabbroids and subordinate pyroxenites of the Kershor complex, dated mainly to the Late Ordovician. In these rocks, mineralization zones with an apparent thickness from 0.5 to 50 m (sulfides 3–5 vol.%, occasionally more) are developed. In areas with scattered or finely nested sulfide inclusions, feldspar-quartz, epidote and other veins are often present. According to assay data, in substantially sulfide 0.5–1 kg samples of these, in general, low–sulfide zones, the Pd content reaches 1.4 g/t, Au – 0.8 g/t, and Pt – 0.2 g/t. PGE minerals are represented by abundant secretions of micron–sized palladium tellurides – merenskite PdTe2, temagamite Pd3HgTe3, kotulskite PdTe, as well as other noble metal compounds – sadberite PdSb, arsenopalladinite Pd8(As,Sb)3 and others. In addition to these palladium minerals, the magnetite–chalcopyrite–pyrite association contains microinclusions of native silver, native bismuth and native tin. In the later polysulfide–feldspar–carbonate–quartz association, Au and Ag tellurides, native gold (including Hg-bearing), Se-containing argentite, greenockite are found. The formation of parageneses of precious metals is associated with late magmatic processes, as well as with redistribution by subsequent magmatogenic hydrothermal fluids, up to a temperature of ~250°C; pressure decreased from ~0.9–1.3 to ~0.4–0.5 kbar.

Spurrite from Negra Mine, Queretaro, Mexico is characterized by a complex chemical composition. Its empirical formula derived based on electron microprobe, wet chemical analyses and gas chromatography of annealing products is H 0.18 Ca 5.01 Na 0.05 [(SiO 4 ) 1.91 (SO 4 ) 0.08 )][(CO 3 ) 0.71 (BO 3 ) 0.28 ]O 11 . The mineral was studied by single-crystal X-ray diffraction (SCXRD) as well as infrared (IR), Raman and nuclear magnetic resonance (NMR) spectroscopy. According to spectroscopic data, boron has three-fold coordination and sulfur occurs in the mineral in the sulfate form. A significant portion of carbonate groups is substituted by BO 3 3– anions. Charge compensation is achieved due to the substitution of a part of SiO 4 4– anions by SO 4 2– groups, as well as to the admixture of sodium. SCXRD shows that sodium occurs in its own site with a low occupancy. The studied sample is isotypic with the synthetic NaCa 5 (SiO 4 ) 2 (BO 3 ) compound. The IR spectrum shows possible partial protonation of the SiO 4 tetrahedra whereas bands of H 2 O molecules and isolated OH – anions are not observed. Thermal behavior of B,S,Na-bearing spurrite from Negra Mine has been studied using powder high-temperature X-ray diffraction (HTXRD) together with boron poor and S-free spurrite from Fuka Area (Japan). The studied samples are stable up to ~ 1200 °C and ~ 1100 °C, respectively, whereas synthetic B,S-free spurrite decomposes at about 900 °C. The thermal expansion is significantly anisotropic and is observed mainly in the direction perpendicular to the ac plane which is coplanar with the layers of calcium polyhedra and anionic pseudo-layers formed by (C,B)O 3 triangles and (Si,S)O 4 tetrahedra. Isomorphism and a similarity of the thermal, baric and compositional (C-B substitution) deformations of spurrite-like structures are discussed.

A variety of the mineral nezilovite, containing antimony and an elevated amount of titanium, has been studied using microprobe and X-ray diffraction analysis. The diffraction experiment was performed on a crystal presenting an aggregate of nezilovite and högbomite with close unit-cell parameters. The parameters of the hexagonal cell of the nezilovite studied are a = 5.8855(2) Å, c = 23.092(1) Å, V = 692.73 (4) Å3,sp. gr. P63/mmc. The structural model is refined using a limited number of unique reflections 231F 4σ(F) to R = 0.08. The crystallochemical formula is (Z = 2) PbZn2(Ti0.9Al0.1)(Al0.6Sb )Mn Fe O18.5(O,OH)0.5. The distribution of cations of this composition over structure sites is established. A basis of the mineral structure is a set of spinel layers, consisting of edge-sharing Fe3+ octahedra. They alternate with two heteropolyhedral layers: Zn tetrahedra combine (Al,Sb) octahedra in one layer, and five-vertex Ti polyhedra combine dimers of Mn3+ octahedra in the other layer.

The crystal structure of a mineral of the cancrinite group with an aluminosilicate framework of the marinellite type and a dominant sulfite group SO_3^2 - in one of the extraframework sites in the liottite cavity is studied. The studied mineral is derived from a paleovolcano near Magliano (Lazio, Italy) and is one of the major rock-forming phases of the leucite–nepheline syenite. The divergence factor was R = 5.71 SO_3^2 - anion was confirmed by the Raman spectrum.

In the Polar Urals, there are a few small granitoid intrusions (Yarkeu, Yajyu, and Pogurei complexes), which are usually associated with the Urals collision. Their Carboniferous–Early Permian age is generally based on methodologically obsolete K/Ar dates and is assumed from the field geological relationships. We have studied the monzonitoids of the Yarkeu petrotypical pluton, one of the largest intrusions, and for the first time we obtained the Late Precambrian U–Pb LA-ICP-MS (zircon) and 40Ar/39Ar (amphibole) dates of 687 ± 3 Ma and 669 ± 8 Ma, respectively. The water-saturated fluid regime (the presence of magmatic amphibole with a high water content of 4.5–5.6 wt