Group–Theoretical Representation of Holohedral Forms of Crystals By

Total Page:16

File Type:pdf, Size:1020Kb

Group–Theoretical Representation of Holohedral Forms of Crystals By Crystallography Reports, Vol. 45, No. 4, 2000, pp. 529–536. Translated from Kristallografiya, Vol. 45, No. 4, 2000, pp. 583–590. Original Russian Text Copyright © 2000 by Nizamutdinov, Vinokurov, Khakimov, Bulka, Galeev, Khasanova. CRYSTALLOGRAPHIC SYMMETRY Group–Theoretical Representation of Holohedral Forms of Crystals by Conjugated Simple Forms. Intergrowth of Crystals N. M. Nizamutdinov*, V. M. Vinokurov*, E. M. Khakimov**, G. R. Bulka*, A. A. Galeev*, and N. M. Khasanova* * Kazan State University, ul. Lenina 18, Kazan, 420008 Russia1 ** Kazan State Pedagogical University, Kazan, Russia Received June 8, 1998; in final form, April 12, 1999 Abstract—The schemes for division of holohedral simple forms of crystals into conjugated simple forms are derived by decomposition of the symmetry group of the primitive sublattice into double cosets. The number of equivalently oriented simple forms in the intergrowth of crystals, whose primitive space sublattices are parallel to one another, is equal to the number of holohedral permutational conjugated simple forms, which has the value 992 for all the 32 symmetry classes. © 2000 MAIK “Nauka/Interperiodica”. 1 INTRODUCTION disymmetrization [7]. If the orientations of the space lattices of individual crystals of the intergrowth coin- If the point group GK of the crystal does not coincide cide, the detection of such crystals by the diffraction [6] with the space group Gsp of the lattice, the faces of the and electron paramagnetic resonance (EPR) methods crystal equivalently oriented with respect to the three- becomes rather difficult because their diffraction pat- dimensional lattice are nonequivalently oriented with terns and EPR spectra become indistinguishable. The respect to the crystal structure. As a results of this non- present article is aimed at studying the intergrowth of equivalence, the holohedral form decomposes into con- individual crystals with the parallel primitive sublat- jugated simple forms allowed by the group GK [1, 2]. tices by the methods of the abstract theory of groups The division of holohedral forms into conjugated sim- and representations. We also consider their possible ple ones was derived geometrically rigorously in [1–4] detection by the EPR method. The study is performed on the basis of the theory of crystal symmetry. The in two main stages: (i) decomposition of the space present study is aimed to derive the schemes of division group of the primitive space sublattice Gssp into the of holohedral forms caused by lowering of the symme- adjacent classes with respect to the subgroup G and try of the point group G with respect to the group of K K double cosets by modulus (GK, GH), where GH is the the primitive sublattice Gssp (a holohedral group) by the group of a face of the holohedral simple form, and (ii) group-theoretical method. derivation of simple forms for cubic and rhombohedral ⊂ Under the condition that GK Gssp, the crystal struc- crystals from their holohedral forms. The mathematical apparatus of the abstract group theory [8] used in our ture can have nK equivalent orientations with respect to the primitive space sublattice [1]: study corresponds to the merohedry method of the the- ory of crystal form [1, 2]. ≡[] nK Gssp : G K = gG ()/ ssp gG (), K (1) where [Gssp : GK] is the index of the group GK in Gssp, GROUP–THEORETICAL METHOD and g(Gssp) and g(GK) are the orders of the groups Gssp OF DERIVATION OF CONJUGATED SIMPLE FORMS OF CRYSTALS and GK, respectively. The number nK is the number of individual crystals with parallel primitive sublattices in FROM THEIR HOLOHEDRAL FORMS the intergrowth, called hereafter holohedral inter- There are seven system space groups Gsp for crystals growth. Various individual crystals in the intergrowth of various systems—Ci, C2h, D2h, D3d, D4h, D6h, and Oh have different orientations and differently interact with [9, 10]. Only for the trigonal system (Gsp = D3d), the applied magnetic fields. The possible formation of primitive sublattice is characterized by the group differ- intergrown crystals of a substance is used in the inter- ent from Gsp (Gssp = D6h), which reduces the number of pretation of the nature of modulated crystal structures holohedral groups to six [1, 2, 11, 12]. [5, 6] and is also taken into account in the studies of Consider the holohedral class of crystals, GK = Gssp. 1 e-mail: [email protected] Let GH be the symmetry group of the face of the holo- 1063-7745/00/4504-0529 $20.00 © 2000 MAIK “Nauka/Interperiodica” 530 NIZAMUTDINOV et al. hedral form. This face can be divided into gH equivalent is equal to the index [GK : GKiH] of the group GKiH in GK: elementary (nonsymmetric) parts with respect to the ≡ [ ] ≤ ≤ nKiH = g(GK) : g ( G KiH) GK : G K iH , 1 i l. (6) symmetry elements of the group GH, where gH is the order of the group GH. If one of these parts, f, is multi- The groups GK of the crystals of the system under con- plied by the symmetry elements of the group GH, we sideration are invariant subgroups of the group G ∈ ssp arrive at the face GH f. Using the elements hi Gssp for and, therefore, expansion (3) acquires the form GH f, we arrive at all the other faces hiGH f of the simple l ( ) form, namely, ∑hi GH f. Applying the elements of the GKGssp = ∑ nKiHhi GKGH . (7) group Gssp to f, we can also represent this simple form i = 1 as Gssp f. Equating the holohedral forms obtained by The product (GKGH) in (7), which acts onto the elemen- these two methods, we obtain tary part of f, yields one conjugated form ≤ ≤ [ ] ( ) ( ) Gssp = ∑hiGH, 1 i nH, nH = Gssp: GH , (2) GKGH f = GK GH f . (8) i It follows from (7) and (8) that all the conjugated forms are of the same type. Therefore, we restrict our consid- where hiGH is the right coset with respect to GH [8]. To each face of the simple form in (2) there uniquely cor- eration to only one conjugated form GK(GH f). The group of the face G of conjugated form (8) is deter- responds one coset. The index nH of the subgroup GH in F mined as the intersection G = G ∩ G (5). Form (8) Gssp is equal to the number of faces of the holohedral F H K simple form. Hereafter, for the sake of brevity, the sim- can be obtained by multiplying the face (GF f) with the ple forms are referred to as forms. aid of the coset representatives in the expansion of GK with respect to the subgroup GF: Let a crystal of the system Gssp have the point group ⊂ GK Gssp. In order to determine the number of conju- ( ∩ ) gated forms l and their faces nKiH, apply the group oper- GK = ∑ h j GH GK = ∑ h jGF, (9) ations of GK to the face hiGH f of the holohedral form. j = 1 j = 1 With this aim, multiply hiGH in (2) by GK on the left- ≤ ≤ [ ] 1 j GK : G F = nKH. hand side. The product GKhiGH is the double coset by modulus (GK, GH) [8]. The product GKhiGH contains all The number l of the conjugated forms is calculated by the cosets corresponding to the faces equivalent with the formula respect to GK. The GKhiGH class uniquely corresponds [ ] [ ] l = gssp : gH : gK : gF to one simple form of the crystal with GK. The number (10) ≡ [ ] [ ] nKiH equals the number of the right cosets with respect Gssp : GH : GK : GF . to GH in the product GKhiGH. Multiplying the left-hand × × ≠ If GK' = GK G and GF' = GF G at G C1, then the side of (2) by GK, we arrive at the expansion substitution of GK by GK' and GF by GF ' in (9) does not l l change the system of the coset representatives {hi}. In G G = ∑ n G h G , n = ∑ n . (3) this case, the same form can be used for crystals with K ssp KiH K i H H KiH different symmetries, and the condition for the exist- i = 1 i = 1 ence of the same simple form can be written as Expansion (3) is, in fact, the scheme for making the faces of the holohedral form nonequivalent. Using the GK = ∑hiGF, GK' = ∑hi'GF', (11) –1 i i conjugated groups hiGH hi , we can represent expan- ≤ ≤ sion (2) in the form h i = h i' , 1 i n K H . –1 If G = G , then the condition for the admission of the G f = ∑(h G h )(h f ), 1 ≤ i ≤ n , (4) F F ' ssp i H i i H same simple form reduces to the condition of “equal i power” of the systems of representatives (11). In this –1 case, the groups GK and GK' are of the same order. where the group hiGHhi is the symmetry group of the ith face of the holohedral form, and hi f is one of the ele- mentary parts of this face. The symmetry group of the SIMPLE FORMS AND INTERGROWN face of the ith conjugated form (3) is determined as the CUBIC CRYSTALS –1 intersection of the groups GK and hiGH hi , For the cubic system, Gssp = Gsp = Oh. If GK = Oh, all the simple forms—a cube, a rhombododecahedron, tet- –1 ∩ ≤ ≤ GKiH = hiGHhi GK, 1 i l. (5) rahexahedron, octahedron, tetragon-trioctahedron, trigon-trioctahedron, and hexakis octahedron—are The number nKiH of the faces of the ith conjugated form holohedral. The following holohedral forms possess CRYSTALLOGRAPHY REPORTS Vol. 45 No. 4 2000 GROUP–THEORETICAL REPRESENTATION OF HOLOHEDRAL FORMS 531 the maximum number of faces having the highest pos- has the form sible symmetry. tetrahexahedra pentagon-dodecahedra A cube has the face group GH = G4V.
Recommended publications
  • Anorogenic Alkaline Granites from Northeastern Brazil: Major, Trace, and Rare Earth Elements in Magmatic and Metamorphic Biotite and Na-Ma®C Mineralsq
    Journal of Asian Earth Sciences 19 (2001) 375±397 www.elsevier.nl/locate/jseaes Anorogenic alkaline granites from northeastern Brazil: major, trace, and rare earth elements in magmatic and metamorphic biotite and Na-ma®c mineralsq J. Pla Cida,*, L.V.S. Nardia, H. ConceicËaÄob, B. Boninc aCurso de PoÂs-GraduacËaÄo em in GeocieÃncias UFRGS. Campus da Agronomia-Inst. de Geoc., Av. Bento GoncËalves, 9500, 91509-900 CEP RS Brazil bCPGG-PPPG/UFBA. Rua Caetano Moura, 123, Instituto de GeocieÃncias-UFBA, CEP- 40210-350, Salvador-BA Brazil cDepartement des Sciences de la Terre, Laboratoire de PeÂtrographie et Volcanologie-Universite Paris-Sud. Centre d'Orsay, Bat. 504, F-91504, Paris, France Accepted 29 August 2000 Abstract The anorogenic, alkaline silica-oversaturated Serra do Meio suite is located within the Riacho do Pontal fold belt, northeast Brazil. This suite, assumed to be Paleoproterozoic in age, encompasses metaluminous and peralkaline granites which have been deformed during the Neoproterozoic collisional event. Preserved late-magmatic to subsolidus amphiboles belong to the riebeckite±arfvedsonite and riebeckite± winchite solid solutions. Riebeckite±winchite is frequently rimmed by Ti±aegirine. Ti-aegirine cores are strongly enriched in Nb, Y, Hf, and REE, which signi®cantly decrease in concentrations towards the rims. REE patterns of Ti-aegirine are strikingly similar to Ti-pyroxenes from the IlõÂmaussaq peralkaline intrusion. Recrystallisation of mineral assemblages was associated with deformation although some original grains are still preserved. Magmatic annite was converted into magnetite and biotite with lower Fe/(Fe 1 Mg) ratios. Recrystallised amphibole is pure riebeckite. Magmatic Ti±Na-bearing pyroxene was converted to low-Ti aegirine 1 titanite ^ astrophyllite/aenigmatite.
    [Show full text]
  • Petrology of Nepheline Syenite Pegmatites in the Oslo Rift, Norway: Zr and Ti Mineral Assemblages in Miaskitic and Agpaitic Pegmatites in the Larvik Plutonic Complex
    MINERALOGIA, 44, No 3-4: 61-98, (2013) DOI: 10.2478/mipo-2013-0007 www.Mineralogia.pl MINERALOGICAL SOCIETY OF POLAND POLSKIE TOWARZYSTWO MINERALOGICZNE __________________________________________________________________________________________________________________________ Original paper Petrology of nepheline syenite pegmatites in the Oslo Rift, Norway: Zr and Ti mineral assemblages in miaskitic and agpaitic pegmatites in the Larvik Plutonic Complex Tom ANDERSEN1*, Muriel ERAMBERT1, Alf Olav LARSEN2, Rune S. SELBEKK3 1 Department of Geosciences, University of Oslo, PO Box 1047 Blindern, N-0316 Oslo Norway; e-mail: [email protected] 2 Statoil ASA, Hydroveien 67, N-3908 Porsgrunn, Norway 3 Natural History Museum, University of Oslo, Sars gate 1, N-0562 Oslo, Norway * Corresponding author Received: December, 2010 Received in revised form: May 15, 2012 Accepted: June 1, 2012 Available online: November 5, 2012 Abstract. Agpaitic nepheline syenites have complex, Na-Ca-Zr-Ti minerals as the main hosts for zirconium and titanium, rather than zircon and titanite, which are characteristic for miaskitic rocks. The transition from a miaskitic to an agpaitic crystallization regime in silica-undersaturated magma has traditionally been related to increasing peralkalinity of the magma, but halogen and water contents are also important parameters. The Larvik Plutonic Complex (LPC) in the Permian Oslo Rift, Norway consists of intrusions of hypersolvus monzonite (larvikite), nepheline monzonite (lardalite) and nepheline syenite. Pegmatites ranging in composition from miaskitic syenite with or without nepheline to mildly agpaitic nepheline syenite are the latest products of magmatic differentiation in the complex. The pegmatites can be grouped in (at least) four distinct suites from their magmatic Ti and Zr silicate mineral assemblages.
    [Show full text]
  • Titanite Ores of the Khibiny Apatite-Nepheline- Deposits: Selective Mining, Processing and Application for Titanosilicate Synthesis
    minerals Article Titanite Ores of the Khibiny Apatite-Nepheline- Deposits: Selective Mining, Processing and Application for Titanosilicate Synthesis Lidia G. Gerasimova 1,2, Anatoly I. Nikolaev 1,2,*, Marina V. Maslova 1,2, Ekaterina S. Shchukina 1,2, Gleb O. Samburov 2, Victor N. Yakovenchuk 1 and Gregory Yu. Ivanyuk 1 1 Nanomaterials Research Centre of Kola Science Centre, Russian Academy of Sciences, 14 Fersman Street, Apatity 184209, Russia; [email protected] (L.G.G.); [email protected] (M.V.M.); [email protected] (E.S.S.); [email protected] (V.N.Y.); [email protected] (G.Y.I.) 2 Tananaev Institute of Chemistry of Kola Science Centre, Russian Academy of Sciences, 26a Fersman Street, Apatity 184209, Russia; [email protected] * Correspondence: [email protected]; Tel.: +7-815-557-9231 Received: 4 September 2018; Accepted: 10 October 2018; Published: 12 October 2018 Abstract: Geological setting and mineral composition of (apatite)-nepheline-titanite ore from the Khibiny massif enable selective mining of titanite ore, and its processing with sulfuric-acid method, without preliminary concentration in flotation cells. In this process flow diagram, titanite losses are reduced by an order of magnitude in comparison with a conventional flotation technology. Further, dissolution of titanite in concentrated sulfuric acid produces titanyl sulfate, which, in turn, is a precursor for titanosilicate synthesis. In particular, synthetic analogues of the ivanyukite group minerals, SIV, was synthesized with hydrothermal method from the composition based on titanyl-sulfate, and assayed as a selective cation-exchanger for Cs and Sr.
    [Show full text]
  • Astrophyllite–Alkali Amphibole Rhyolite, an Evidence of Early Permian A-Type Alkaline Volcanism in the Western Mongolian Altai
    Journal of Geosciences, 61 (2016), 93–103 DOI: 10.3190/jgeosci.205 Original paper Astrophyllite–alkali amphibole rhyolite, an evidence of early Permian A-type alkaline volcanism in the western Mongolian Altai Vladimír Žáček1*, David BurIánek1, Zoltán Pécskay2, radek ŠkODa1 1 Czech Geological Survey, Klárov 3, 118 21 Prague 1, Czech Republic; [email protected] 2 Institute for Nuclear Research, Hungarian Academy of Sciences (ATOMKI), Bem tér 18/c, Debrecen, Hungary * Corresponding author A dyke of alkali rhyolite intrudes the Tsetseg and Zuun Nuruu volcanosedimentary sequence of Ordovician–Silurian age (Hovd Zone, Central Asian Orogenic Belt) at the Botgon bag, Mankhan Soum, Hovd District in Western Mongolia. The rock consists of quartz and K-feldspar phenocrysts set in fine-grained groundmass composed of quartz, K-feldspar, albite, blue alkali amphibole (riebeckite–arfvedsonite containing up to 1.94 wt. % ZrO2), tiny brown radial astrophyllite, annite and accessory zircon, ilmenite, fluorite, monazite, hematite, chevkinite and bastnäsite. Astrophyllite has unusual, highly ferroan composition and occurs as two sharply bound zones of astrophyllite I and II with the average empirical formulae: 2+ (K1.71 Na0.01Rb0.08Cs0.01) (Na0.93Ca0.07) (Fe 6.52Mn0.31Zn0.06) (Ti0.84Zr0.50Nb0.55) Si7.68Al0.32 O26 (OH)3.78 F0.66 (astrophyllite I, 2+ Zr–Nb-rich); (K1.52Rb0.07) (Na0.81Ca0.19) (Fe 6.31 Mn0.28Zn0.06) (Ti1.28Nb0.30Zr0.28) Si7.68Al0.32 O26 (OH)2.85 F0.67 (astrophyllite II). Geochemically, the rhyolite corresponds to strongly fractionated silicic alkaline A-type (ferroan) magmatic rock with t 75.5–75.9 wt.
    [Show full text]
  • 29 Devitoite, a New Heterophyllosilicate
    29 The Canadian Mineralogist Vol. 48, pp. 29-40 (2010) DOl: 1O.3749/canmin.48.1.29 DEVITOITE, A NEW HETEROPHYLLOSILICATE MINERAL WITH ASTROPHYLLITE-LiKE LAYERS FROM EASTERN FRESNO COUNTY, CALIFORNIA ANTHONY R. KAMPP§ Mineral Sciences Department, Natural History Museum of Los Angeles County, 900 Exposition Boulevard, Los Angeles, California 90007, USA. GEORGE R. ROSSMAN Division of Geological and Planetary Sciences, California Institute of Technology, Pasadena, California 91125-2500, USA. IAN M. STEELE AND JOSEPH J. PLUTH Department of the Geophysical Sciences, The University of Chicago, 5734 S. Ellis Avenue, Chicago, Illinois 60637, U.S.A. GAIL E. DUNNING 773 Durshire Way, Sunnyvale, California 94087, U.S.A. ROBERT E. WALSTROM P. O. Box 1978, Silver City, New Mexico 88062, USA. ABSTRACT Devitoite, [Ba6(P04MC03)] [Fe2+7Fe3+2(Si4012h02(OH)4], is a new mineral species from the Esquire #8 claim along Big Creek in eastern Fresno County, California, U.SA. It is also found at the nearby Esquire #7 claim and at Trumbull Peak in Mariposa County. The mineral is named for Alfred (Fred) DeVito (1937-2004). Devitoite crystallized very late in a sequence of minerals resulting from fluids interacting with a quartz-sanbornite vein along its margin with the country rock. The mineral occurs in subparallel intergrowths of very thin brown blades, flattened on {001} and elongate and striated parallel to [100]. The mineral has a cream to pale brown streak, a silky luster, a Mohs hardness of approximately 4, and two cleavages: {OO!} perfect and {01O} good. The calculated density is 4.044 g/cm '. It is optically biaxial (+), Cl 1.730(3), 13 1.735(6), 'Y 1.755(3); 2Vcalc = 53.6°; orientation: X = b, Y = c, Z = a; pleochroism: brown, Y»> X> Z.
    [Show full text]
  • High-Temperature Behaviour of Astrophyllite, K2nafe7 2+Ti2
    Phys Chem Minerals DOI 10.1007/s00269-017-0886-1 ORIGINAL PAPER High-temperature behaviour of astrophyllite, 2+ K2NaFe7 Ti2(Si4O12)2O2(OH)4F: a combined X-ray diffraction and Mössbauer spectroscopic study Elena S. Zhitova1,2 · Sergey V. Krivovichev1,3 · Frank C. Hawthorne4 · Maria G. Krzhizhanovskaya1 · Andrey A. Zolotarev1 · Yassir A. Abdu4,5 · Viktor N. Yakovenchuk3 · Yakov A. Pakhomovsky3 · Alexey G. Goncharov1 Received: 27 May 2016 / Accepted: 14 March 2017 © Springer-Verlag Berlin Heidelberg 2017 Abstract High-temperature X-ray powder-diffraction c = 11.4332(9) Å, α = 112.530(8), β = 94.539(6), 2+ 3 study of astrophyllite, K2NaFe7 Ti2(Si4O12)2O2(OH)4F, γ = 103.683(7)º, V = 633.01(9) Å for the HT (annealed) and investigation of the samples annealed at 600 and modification of astrophyllite. The oxidation of iron is 700 °C, reveal the occurrence of a phase transformation due confirmed: (1) by the presence of an exothermic effect to the thermal iron oxidation coupled with (1) deprotonation at 584 °C in the DTA/TG curves in an Ar–O atmosphere 2+ − 3+ 2− according to the scheme Fe + OH → Fe + O + ½H2 ↑, and its absence in an Ar–Ar atmosphere and (2) by ex situ and (2) defluorination according to the scheme Mössbauer spectroscopy that showed the oxidation of Fe2+ Fe2+ + F− → Fe3+ + O2−. The phase transformation occurs to Fe3+ in the samples heated to 700 °C. Deprotonation at 500 °C, it is irreversible and without symmetry changes. was detected by the evolution of IR spectra in the region The mineral decomposes at 775 °C.
    [Show full text]
  • 4F, a New Astrophyllite-Super- Group Mineral from Mont Saint-Hilaire, Quebec,´ Canada
    201 The Canadian Mineralogist Vol. 57, pp. 201-213 (2019) DOI: 10.3749/canmin.1800071 LAVEROVITE, K2NaMn7Zr2(Si4O12)2O2(OH)4F, A NEW ASTROPHYLLITE-SUPER- GROUP MINERAL FROM MONT SAINT-HILAIRE, QUEBEC,´ CANADA § ELENA SOKOLOVA ,MAXWELL C. DAY, AND FRANK C. HAWTHORNE Department of Geological Sciences, University of Manitoba, Winnipeg, Manitoba R3T 2N2 Canada ANATOLY V. KASATKIN Fersman Mineralogical Museum, Russian Academy of Sciences, Leninskii Prospekt, 18-2, 119071 Moscow, Russia ROBERT T. DOWNS Department of Geosciences, University of Arizona, 1040 E 4th Street, Tucson, Arizona 85721-0077, USA LA´ SZLO´ HORVATH´ AND ELSA PFENNINGER-HORVATH´ 594 Main Road, Hudson Heights, Quebec´ J0P 1J0, Canada ABSTRACT Laverovite (IMA 2017-009b), ideally K2NaMn7Zr2(Si4O12)2O2(OH)4F, is a kupletskite-group (astrophyllite-supergroup) mineral from Mont Saint-Hilaire, Quebec,´ Canada. Associated minerals are zircophyllite, kupletskite, astrophyllite, aegirine, analcime, orthoclase, and albite. Laverovite is brown, transparent in thin grains, and has a vitreous luster. Mohs hardness is 3, 3 Dcalc. ¼ 3.367 g/cm . Laverovite is biaxial (–) with refractive indices (k ¼ 589 nm) a ¼ 1.670(2), b ¼ 1.710(5), c ¼ 1.740(5); 2Vmeas. ¼ 82(2)8,2Vcalc. ¼ 808, strong dispersion: r . v. Cleavage is perfect parallel to {001}. Chemical analysis by electron microprobe gave Nb2O5 0.56, ZrO2 9.78, TiO2 4.69, SiO2 33.52, Al2O3 0.94, SrO 0.13, ZnO 0.07, FeO 13.94, MnO 20.51, CaO 0.48, MgO 0.76, Cs2O 0.05, K2O 6.00, Na2O 2.28, F 1.80, H2Ocalc. 2.57, sum 97.32 wt.%; H2O was calculated from crystal-structure analysis.
    [Show full text]
  • Lorenzenite Na2ti2si2o9 C 2001 Mineral Data Publishing, Version 1.2 ° Crystal Data: Orthorhombic
    Lorenzenite Na2Ti2Si2O9 c 2001 Mineral Data Publishing, version 1.2 ° Crystal Data: Orthorhombic. Point Group: 2=m 2=m 2=m: Crystals equant, bladed prismatic, to needlelike, to 6 cm; ¯brous, felted, lamellar aggregates. Physical Properties: Cleavage: Distinct on 010 . Fracture: Uneven. Hardness = 6 f g D(meas.) = 3.42{3.45 D(calc.) = 3.44 May °uoresce pale yellow to dull green under SW UV, with green cathodoluminescence. Optical Properties: Transparent to opaque. Color: Pale purple-brown, pale pink to mauve, brown to black. Luster: Vitreous, adamantine to submetallic, or silky, dull. Optical Class: Biaxial ({). Pleochroism: Weak; X = Y = pale reddish yellow, yellowish brown to light brown; Z = pale yellow, brownish to dark brown. Orientation: X = b; Y = a; Z = c. Dispersion: r > v; distinct. ® = 1.91{1.95 ¯ = 2.01{2.04 ° = 2.03{2.06 2V(meas.) = 38±{41± Cell Data: Space Group: P bcn: a = 8.7128(10) b = 5.2327(5) c = 14.487(2) Z = 4 X-ray Powder Pattern: Lovozero massif, Russia. (ICDD 18-1262). 2.74 (100), 3.33 (70), 1.60 (50), 5.56 (40), 2.45 (40), 1.64 (40), 3.12 (30) Chemistry: (1) (2) (3) (1) (2) (3) SiO2 35.40 35.3 35.15 FeO 0.34 TiO2 43.16 43.7 46.72 MnO trace 0.12 ZrO2 0.07 CaO 0.19 0.14 Al2O3 0.00 0.11 SrO 0.01 Y2O3 0.02 Na2O 16.23 17.4 18.13 La2O3 0.01 F 0.38 + Ce2O3 0.04 H2O 0.42 Fe2O3 0.99 H2O¡ 0.17 Nb O 3.89 2.20 O = F 0.16 2 5 ¡ 2 Total 100.17 99.96 100.00 (1) Narss^arssuk, Greenland; traces of V, Sc, Mn.
    [Show full text]
  • Yuksporite K4(Ca,Na)14(Sr,Ba)2( ,Mn,Fe)(Ti,Nb)4(O,OH)4(Si6o17)2(Si2o7)3(H2O,OH)3
    Yuksporite K4(Ca,Na)14(Sr,Ba)2( ,Mn,Fe)(Ti,Nb)4(O,OH)4(Si6O17)2(Si2O7)3(H2O,OH)3 Crystal Data: Monoclinic. Point Group: 2/m. Fibrous, scaly, or lamellar; in radial aggregates, to 10 cm. Physical Properties: Hardness = 5 D(meas.) = 3.05(3) D(calc.) = [2.98] Optical Properties: Semitransparent. Color: Rose-red to straw-yellow. Optical Class: Biaxial (+). α = 1.644(2) β = n.d. γ = 1.660(2) 2V(meas.) = 46°-76° Pleochroism: Marked; X = pale rose-yellow; Y = Z = rose-yellow. Cell Data: Space Group: P21/m. a = 7.126(3) b = 24.913(6) c = 17.075(7) β = 101.89(3)° Z = n.d. X-ray Powder Pattern: Khibiny massif, Russia. 2.778 (10), 3.00 (9), 1.786 (9), 3.10 (8), 3.05 (8), 1.888 (7), 2.92 (6) Chemistry: (1) (2) (1) (2) SiO2 40.92 38.40 BaO 8.60 TiO2 11.00 Na2O 7.94 3.84 Al2O3 0.07 K2O 12.57 6.15 Fe2O3 9.10 0.75 F 3.05 MnO 0.91 0.29 Cl 0.80 + MgO 0.42 H2O 2.20 CaO 20.56 18.90 H2O 8.52 SrO 5.87 - O = (F,Cl)2 1.46 Total 100.94 [98.46] (1) Khibiny massif, Russia. (2) Murun massif, Russia; original total given as 99.07%, corresponds to 3+ (K0.70Ba0.30)Σ=1.00(Na0.66Sr0.30)Σ=0.96(Ca1.80Ti0.19Fe 0.06Mn0.02)Σ=2.07(Si3.42Ti0.57Al0.01)Σ=4.00O11[F0.86Cl0.12 (OH)0.02]Σ=1.00∙0.6H2O.
    [Show full text]
  • New Mineral Names*
    American Mineralogist, Volume 89, pages 249–253, 2004 New Mineral Names* JOHN L. JAMBOR1,† AND ANDREW C. ROBERTS2 1Department of Earth and Ocean Sciences, University of British Columbia, Vancouver, British Columbia V6T 1Z4, Canada 2Geological Survey of Canada, 601 Booth Street, Ottawa K1A 0E8, Canada ARTSMITHITE* analysis gave BaO 47.66, SiO2 36.38, BeO (by AA) 14.90, A.C. Roberts, M.A. Cooper, F.C. Hawthorne, R.A. Gault, J.D. sum 98.94 wt%, corresponding to Ba1.03Be1.97Si2.00O7.00. The Grice, A.J. Nikischer (2003) Artsmithite, a new Hg1+–Al mineral forms radial aggregates and platy to prismatic crystals phosphate–hydroxide from the Funderburk prospect, Pike that are elongate [001] and up to 1 × 4 × 20 mm, typically flattened on {100} or less commonly on {010}. Observed forms County, Arkansas, U.S.A. Can. Mineral., 41, 721–725. – are {100}, {010}, {201}, and {201}, with less common {610}, – {101}, and {101}. Colorless, transparent, vitreous luster, brittle, Electron microprobe analysis gave Hg2O 78.28, Al2O3 5.02, H = 6½, perfect {100} and less perfect {001} and {101} cleav- P2O5 11.39, H2O (calc.) 1.63, sum 96.32 wt%, from which the 3 structure-derived formula corresponds to Hg1+ Al P ages, Dmeas = 3.97(7), Dcalc = 4.05 g/cm for Z = 2. Optically 4 .00 1.05 1.71 α β γ O H , generalized as Hg Al(PO ) (OH) , where x = 0.26. biaxial positive, = 1.698(3), = 1.700(3), = 1.705(5), 2Vmeas 8.74 1.78 4 4 2–x 1+3x ∧ ∧ The mineral occurs as a matted nest of randomly scattered fi- = 70(10), 2Vcalc = 65°, orientation Z = b, X a = 6°, Y c = 5– bres, elongate [001] and some >1 mm in length, with 6°.
    [Show full text]
  • Geochemistry of Niobium and Tantalum
    Geochemistry of Niobium and Tantalum GEOLOGICAL SURVEY PROFESSIONAL PAPER 612 Geochemistry of Niobium and Tantalum By RAYMOND L. PARKER and MICHAEL FLEISCHER GEOLOGICAL SURVEY PROFESSIONAL PAPER 612 A review of the geochemistry of niobium and tantalum and a glossary of niobium and tantalum minerals UNITED STATES GOVERNMENT PRINTING OFFICE, WASHINGTON : 1968 UNITED STATES DEPARTMENT OF THE INTERIOR STEWART L. UDALL, Secretary GEOLOGICAL SURVEY William T. Pecora, Director Library of Congress catalog-card No. GS 68-344 For sale by the Superintendent of Documents, U.S. Government Printing Office Washington, D.C. 20402 - Price 50 cents (paper cover) CONTENTS Page Page Abstract_ _ __-_.. _____________________ 1 Geochemical behavior Continued Introduction. _________________________ 2 Magmatic rocks Continued General geochemical considerations. _____ 2 Volcanic rock series______--____---__.__-_-__ 2. Abundance of niobium and tantalum_____ 3 Sedimentary rocks______________________________ 2. Crustal abundance-________________ 3 Deposits of niobium and tantalum.___________________ 2£ Limitations of data________________ 3 Suggestions for future work__--___-_------__-___---_- 26 Abundance in rocks._______________ 5 References, exclusive of glossary______________________ 27 Qualifying statement.__________ 5 Glossary of niobium and tantalum minerals.___________ 3C Igneous rocks_________________ 6 Part I Classification of minerals of niobium and Sedimentary rocks.____________ 10 tantalum according to chemical types_________ 31 Abundance in meteorites and tektites. 12 Part II Niobium and tantalum minerals..-_______ 32 Isomorphous substitution.______________ 13 Part III Minerals reported to contain 1-5 percent Geochemical behavior._________________ 15 niobium and tantalum_______________________ 38 Magma tic rocks ___________________ 15 Part IV Minerals in which niobium and tantalum Granitic rocks_________________ 16 have been detected in quantities less than 1 Albitized and greisenized granitic rocks.
    [Show full text]
  • NALIVKINITE1, Li2nafe2+ a NEW MINERAL of THE
    New Data on Minerals. М., 2008. Volume 43 5 1 2+ NALIVKINITE , Li2NaFe7 Ti2(Si8O24)O2(OH)4F, A NEW MINERAL OF THE ASTROPHYLLITE GROUP FROM THE DARAI-PIOZ MASSIF, TADJIKISTAN Atali A. Agakhanov Fersman Mineralogical Museum, RAS, Moscow, [email protected] Leonid A. Pautov Fersman Mineralogical Museum, RAS, Moscow, [email protected] Yulia A. Uvarova Queen’s University, Kingston, Ontario, Canada Elena Sokolova University of Manitoba, Manitoba, Winnipeg, Canada Frank C. Hawthorne University of Manitoba, Manitoba, Winnipeg, Canada Vladimir Y. Karpenko Fersman Mineralogical Museum, RAS, Moscow, [email protected] Nalivkinite, a new astrophyllite-group mineral, was discovered in the moraine of the Darai-Pioz alkaline massif located at the intersection of the Zeravshansky, Turkestansky and Alaisky Ridges, Tadjikistan. Nalivkinite occurs in the amphibole-quartz-feldspar rock in association with calcybeborosilite-(Y), bafertisite, jinshajiangite, zircon and thorite. Nalivkinite is brown with a bronze hue and a vitreous luster; in thin plates, it is transparent. Mohs hard- 3 3 ness is 3, Dmeas. = 3.32(2) g/cm , Dcalc. = 3.315 g/cm . It is biaxial positive, np = 1.703(2), nm= 1.716(2), ng =1.745(2), 2Vmeas. = +68(2)°, 2Vcalc. = +68.6°. Nalivkinite is triclinic, space group P1, a = 5.3745(6) Å; b = 11.9299(15) Å; c = 11.6509(14) Å; a =113.325(3)°, b = 94.524(2)°, g = 103.080(2)°, V = 656.2(2) Å3, Z = 1. Cell dimensions refined from X-ray powder diffraction data are as follows: a = 5.3707(2) Å; b = 11.9327(5) Å; c = 11.6546(4) Å; a =113.384(1)°, b = 94.547(1)°, 103.047(1)°, V = 655.85(2) Å3.
    [Show full text]