Zuktamrurite, FeP2, is a new mineral, a natural iron diphosphide found in the pyrometamorphic rocks of the Hatrurim Formation, in the southern part of the Negev Desert, Israel and on the Transjordan Plateau, Jordan. The mineral occurs as irregular grains up to 50 µm in size associated with murashkoite, FeP, and barringerite, (Fe,Ni)2P. In reflected light, zuktamrurite is white with a distinct bluish tint. It is non-pleochroic but exhibits distinct anisotropy in bluish colours. Reflectance values for the IMA COM recommended wavelengths are [Rmax/Rmin, % (λ, nm)]: 50.40/47.20 (470); 49.16/46.23 (546); 48.97/46.16 (589); 49.40/46.40 (650). It is brittle. Electron microprobe analysis of the holotype specimen gave the following chemical composition (wt%, average of 5 points): Fe 40.23; Ni 7.97; P 51.70; total 99.90. The empirical formula calculated on the basis of 3 apfu is (Fe0.86Ni0.16)1.02P1.98 corresponding to FeP2. Zuktamrurite is orthorhombic, space group Pnnm, unit cell parameters refined from the single-crystal data: a 4.9276(6), b 5.6460(7), c 2.8174(4) A, V 78.38(1) A3, Z = 2. Dx = 5.003 g cm−3. The crystal structure was solved and refined to R1 = 0.0121 on the basis of 109 unique reflections with I > 2σ(I). The strongest lines of the powder X-ray diffraction pattern [(d, A) (I, %) (hkl)]: 3.714 (54) (110); 2.820 (31) (020); 2.451 (100) (120, 101); 2.242 (55) (111); 1.760 (37) (211). The mineral is named for the Zuk-Tamrur cliff (Dead Sea) located nearby the type locality, the Halamish Wadi, southern Negev Desert, Israel. Zuktamrurite is the phosphide analogue of lollingite (loellingite), FeAs2. It is the most phosphorus-rich phosphide ever found in nature.

Zuktamrurite, FeP 2 , a new mineral, the phosphide analogue of löllingite, FeAs 2.

The mayenite group includes minerals with common formula Ca12Al14O32−x(OH)3x[W6−3x], where W = F, Cl, OH, H2O and x = 0–2. This distinction in the composition is associated with W site which may remain unoccupied or be occupied by negatively charged ions: OH−, F−, Cl−, as well as neutral molecules like H2O. However, there is no experimental approach to easily detect or differentiate mineral species within the mayenite group. Electron micro-beam facilities with energy- or wavelength-dispersive X-ray detectors, as most common tools in mineralogy, appear to be insufficient and do not provide a definite identification, especially, of hydroxylated or hydrated phases. Some solution provides typical Raman analysis ensuring identification of minerals and 3D Raman imaging as an innovative approach to distinguish various co-existing minerals of the mayenite group within a small area of the rock sample. Raman spectroscopy has also been successfully used for a determination of water type incorporated into the mineral structure as well as for a spatial distribution of phases by cluster approach analysis and/or integrated intensity analysis of bands in the hydroxyl region. In this study, Raman technique was for the first time used to reconstruct a 3D model of mayenite group mineral zonation, as well as to determine a way of water incorporation in the structure of these minerals. Moreover, for the first time, Raman data were correlated with alterations during the mineral-forming processes and used for reconstruction of the thermal history of studied rock. As a result, the influence of combustion gases has been proposed as a crucial factor responsible for the transformation between fluormayenite and fluorkyuygenite.

/pdf/raman-imaging-as-a-new-approach-to-identification-of-the-3o2y3hui48.pdf

Raman imaging as a new approach to identification of the mayenite group minerals.

Ariegilatite, BaCa12(SiO4)4(PO4)2F2O (R 3 ¯ m, a = 7.1551(6) A, c = 41.303(3) A, V = 1831.2(3) A3, Z = 3), is a new member of the nabimusaite group exhibiting a modular intercalated antiperovskite structure derived from hatrurite. It was found in a few outcrops of pyrometamorphic rocks of the Hatrurim Complex located in the territories of Israel, Palestine and Jordan. The holotype specimen is an altered spurrite marble from the Negev Desert near Arad city, Israel. Ariegilatite is associated with spurrite, calcite, brownmillerite, shulamitite, CO3-bearing fluorapatite, fluormayenite-fluorkyuygenite and a potentially new mineral, Ba2Ca18(SiO4)6(PO4)3(CO3)F3O. Ariegilatite is overgrown and partially replaced by stracherite, BaCa6(SiO4)2[(PO4)(CO3)]F. The mineral forms flat disc-shaped crystals up to 0.5 mm in size. It is colorless, transparent, with white steaks and vitreous luster. Optically, ariegilatite is uniaxial, negative: ω = 1.650(2), e = 1.647(2) (λ = 589 nm). The mean composition of the holotype ariegilatite, (Ba0.98K0.01Na0.01)Σ1(Ca11.77Na0.08Fe2+0.06Mn2+0.05Mg0.04)Σ12(Si3.95Al0.03Ti0.02)Σ4(P1.70C0.16Si0.10S6+0.03V0.01)Σ2F2.04O0.96, is close to the end-member formula. The structure of ariegilatite is described as a stacking of the two modules {F2OCa12(SiO4)4}4+ and {Ba(PO4)2}4− along (001). Ariegilatite, as well as associated stracherite, are high-temperature alteration products of minerals of an early clinker-like association. These alterations took place under the influence of pyrometamorphism by-products, such as gases and fluids generated by closely-spaced combustion foci.

/pdf/new-mineral-with-modular-structure-derived-from-hatrurite-50fuxr5o1d.pdf

New Mineral with Modular Structure Derived from Hatrurite from the Pyrometamorphic Rocks of the Hatrurim Complex: Ariegilatite, BaCa12(SiO4)4(PO4)2F2O, from Negev Desert, Israel

The intergrowths of Fe-rich corundum + Al-rich hematite + spinel + hibonite have been found as an assemblage in a plagioclase-clinopyroxene rock (paralava, former hornfels) at the Hatrurim Basin, Hatrurim combustion metamorphic Formation. Most spinels show oriented exsolution structures and vary from (Mg0.75)O4 (homogeneous) indicating a tendency towards magnesioferrite and magnetite, and enrichment in NiO (up to 1.9 wt.%) and ZnO (up to 1.4 wt.%). Hibonite is Ti rich (TiO2 > 8 wt.%) and close to CaAl9Fe3+(Mg,Fe2+)TiO19. Corundum varies in Fe2O3 (4.2–11.8 wt.%). Hematite is also inhomogeneous and contains oriented exsolution structures of corundum. It shows variable concentrations of TiO2 (0.7–5.6 wt.%), Al2O3 (0.7–8.6 wt.%), Cr2O3 (0.2–1.5 wt.%), V2O3 (0.1–1.0 wt.%) and MgO (0.3–2.0 wt.%). Crystallization of this specific assemblage is assumed to be at 1000–1200°C using evaluations for the corundum hematite pair with reference to published experimental data. The active role of superheated oxidised volatiles is suggested during both crystallisation of this corundum-bearing association and host-rock transformation (melting event for hornfels → paralava).

A hibonite-spinel-corundum-hematite assemblage in plagioclase-clinopyroxene pyrometamorphic rocks, Hatrurim Basin, Israel: mineral chemistry, genesis and formation temperatures

Dzierzanowskite, CaCu 2 S 2 ( P m 1, a  = 3.9400(4), c  = 6.523(1) A, V  = 87.69(2) A 3 , Z  = 1), a thiocuprate, was found in larnite pseudoconglomerate rocks of the Hatrurim Complex at Jabel Harmun, Palestinian Autonomy, Israel. Dzierzanowskite occurs in larnite pebbles, which are embedded in a low-temperature mineral matrix. Associated minerals are larnite, brownmillerite, fluorellestadite, ye9elimite, gehlenite, periclase, ternesite, nabimusaite, vorlanite, vapnikite, fluormayenite, fluorkyuygenite, oldhamite, jasmundite, covellite, chalcocite and pyrrhotite. Electron microprobe analyses yield an average composition of Cu 55.25, Fe 0.13, S 27.46 and Ca 16.99, total 99.83 wt.%. The empirical formula of dzierzanowskite, based on 5 atoms , is Ca 0.98 Cu 2.02 Fe 0.01 S 1.99 . Dzierzanowskite forms grains up to 15 μm in size or rims on oldhamite and laminar intergrowths with chalcocite and covellite. Dzierzanowskite is dark orange, has a cream streak and a submetallic lustre. In reflected light it is grey, with a cream tint and characteristic yellow-orange internal reflections. The calculated density of dzierzanowskite is 4.391 g cm –3 . Three bands at 300, 103 and 86 cm –1 are observed in the Raman spectrum. The strongest lines of the calculated powder diffraction pattern are [ d , A ( I ) hkl ]: 2.358(100) 102, 1.970(93)110, 3.023(78) 011, 6.523(36) 001, 3.412(28) 100, 1.834(28) 103. Dzierzanowskite was also found in unusual jasmundite rocks, forming small ‘paleofumaroles’ within areas of low-temperature hydrothermal rocks bearing larnite pseudoconglomerates at Jabel Harmun. Dzierzanowskite is a superimposed phase of the high-temperature alteration of pyrometamorphic rocks subjected to by-products (melts/fluids and gases) of pyrometamorphism originating in the deeper levels of combustion.

Dzierżanowskite, CaCu2S2 – a new natural thiocuprate from Jabel Harmun, Judean Desert, Palestine Autonomy, Israel

The new mineral gazeevite, BaCa 6 (SiO 4 ) 2 (SO 4 ) 2 O ( R m , a  = 7.1540(1), c  = 25.1242(5) A, V  = 1113.58(3) A 3 , Z  = 3), was found in an altered xenolith in rhyodacites of the Shadil-Khokh volcano, Southern Ossetia and at three localities in larnite pyrometamorphic rocks of the Hatrurim Complex; Nahal Darga and Jabel Harmun, Judean Mountains, Palestinian Autonomy, and Har Parsa, Negev Desert, Israel. Larnite, fluorellestadite–fluorapatite, srebrodolskite–brownmillerite and mayenite-supergroup minerals are the main minerals commonly associated with gazeevite. Gazeevite is isostructural with zadovite and aradite; the 1:1 type AB 6 ( T O 4 ) 2 ( T O 4 ) 2 W , occurs together with the structurally related minerals of the nabimusaite series, 3:1 type AB 12 ( T O 4 ) 4 ( T O 4 ) 2 W 3 , where A  = Ba, K, Sr…; B  = Ca, Na…; T  = Si, P, V 5+ , S 6+ , Al…; W  = O 2– , F – . Single antiperovskite layers {[ WB 6 ]( T O 4 ) 2 } in the structure type of gazeevite–zadovite and triple {[ W 3 B 12 ]( T O 4 ) 4 } layers in arctite–nabimusaite are intercalated with single A ( T O 4 ) layers. These minerals with an interrupted antiperovskite structure are characterized by a modular layered structure derived from hatrurite, Ca 3 (SiO 4 )O. Gazeevite is colourless, transparent, with a white streak and vitreous lustre. Gazeevite is brittle, shows pronounced parting and imperfect cleavage on {001}; it is uniaxial (–), ω = 1.640(3), e = 1.636(2) (λ = 589 nm) and nonpleochroic; Mohs’ hardness is ∼4.5, VHN 50  = 417 kg mm –2 . The calculated density is = 3.39 g cm –3 . The main lines of the calculated powder X-ray diffraction pattern are as follows ( d (A)/ I / hkl ): 3.58/100/110, 3.07/91/021, 2.76/47/116, 1.789/73/220, 3.29/60/113, 2.78/36/024, 2.12/25/125, 2.21/21/208. Raman spectra of gazeevite are compared with spectra of other minerals. The formation of gazeevite and minerals of the nabimusaite–dargaite series is connected with high-temperature alteration of an early assemblage of clinker minerals affected by later fluids generated by volcanic activity or combustion processes.

New minerals with a modular structure derived from hatrurite from the pyrometamorphic rocks. Part III. Gazeevite, BaCa6(SiO4)2(SO4)2O, from Israel and the Palestine Autonomy, South Levant, and from South Ossetia, Greater Caucasus

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New minerals with a modular structure derived from hatrurite from the pyrometamorphic rocks. Part III. Gazeevite, BaCa6(SiO4)2(SO4)2O, from Israel and the Palestine Autonomy, South Levant, and from South Ossetia, Greater Caucasus