DOCSLIB.ORG

Download the Scanned

Total Page：16

File Type：pdf, Size：1020Kb

Download full-text PDF Read full-text

Load more

American Mineralogist, Volume 61, pages 174-186, 1976 NEW MINERAL NAMES* MIcHeer-Flprscunn, Aoor-p Persr, J. A. MnNoanrNo GsoRce Y. CHno. ANDLours J. CnsRr Baumite* 102.7 percent, corresponding to (Pdor,_o 'Pto 14_ossNio os o14) (Te, .r-, Crrrporo Fr.onogl nNo JuN lro (1975) Zinc-rrchchlorites from ,oBio.o o,"). The mineral is hexagonalwith a : 4 005(5),c = 5.244(8)Afor Franklin, New Jersey, with a note on chlorite nomenclature. (Pdo",Pto,rNioor)(Te,rrBioru)and a : 4.036, c : 5.259 A for Neues Jahrb. Mineral. Abh. 123, I I l-l15. (Pdo6oPto roNio,,)(Te, u.Bio.r).The powder patternis similar to that Analysis by J. I. gave SiO,33.5, Al,Os 6.60, Fe,O, 1.65,FeO of merenskyitewith strongestlines (22 given,including B-lines and 9 80, MgO 17.l,ZnO 6.65,CuO 0.03,MnO l2.3,CaO0.07, Na,O I lines without indices): 5.22 6 001, 2.90 l0 101, 2.09 6 0.02, K,O 0.08, H,O-(140') 02, H,O+(140") ll9, sum 99.90 r02.2.01 5 t r0. t.5605 r03. percent, corresponding to the formula Under the binoculars,the mineral is white to bright white with strong metallicluster Mineral grainsare semi-rounded,prismatic, (Mg, nMn, ,F€+ 1rZn, oAlo?Fd+o s)(Si? rAloe)Oro(OH)16 and hexagonaltabular (0 I I X0.l I mm). Under reflectedlight, the mineral white : X-ray powder data are given (Fe radiation). The strongest lines is with a yellow tint. Anisotropic ReflectanceRg, 46.7(400nm) (500nm), of 7 given are 7.23 l0 001; 3.590 6 002;2.5t0 3 201; hence rhe 50.9 56.5 (530nm), 57 7 (590nm), 55.870 (650nm) VHN : mineral is a member of the septechlorite group. When heated at 92-2O5 kl/mm2 500' for I hour, the mineral gave a weak, diffuse pattern; when Both mineralsoccur in a Cu-Ni sulfide depositin fine-grained heatedat 600" gave no pattern. metagabbro and amphibolite in China (details on locality not given) The metallic minerals in the Color dull black. Found in massesup to a foot in size on the deposit are mainly pyrite, chalcopyrite, magnetite, and millerite. dump of the Buckwheat open pit; it contains angular fragments of Other platinum group mineralspresent willemite and calcite, and is cut by thin veinlets of greenish-black are michenerite,moncheite, and merenskyite. The names maganoanzincian brunsvigite(analysis and X-ray data given) In are apparentlyderived from composition,according to the authors' proposed thin section baumite is translucent with brownish-yellow color, classificationscheme based on Pt:pd ratio: biteplatinite, )4: 1; moncheite, nearly isotropic, mean n 1.598.Under the highest magnification it 4:l-l:l; biteplapalladite, l: l-l:4; and merenskyite,(l:4. is seento be composed ofminute birefringent fibers thar appear ro have parallel extinction. Discussion Unnecessary names for intermediate members of the The name is for John Leach Baum, formerly chief geologist of moncheile-merenskyitegroup. It is regrettablethat the authors do the New Jersey Zinc Company..M.F. not follow the generallyaccepted approach in dealingwith a two- end-membersolid solution series.GYC. LJC. Biteplatinite and Biteplapalladite ( = Moncheite-Merenskyite Series) HunNc VnN-KANG, YEH HsIBN-HsIBN,CHINc yupt-MrNc, Caysichite* CsurNc Tseu-Fu, lNo FrNc CHuN-MrNc (1974)Biteplatinite- DoNnlr D HocnnrH, Gsoncr Y. Cruo, A. GEoRcEpr_eNr, aNo merenskyite system and michenerite from a mining district in Henolp R. Srrncy (1974)Caysichite, a new silico-carbonateof China and problems concerning their classificationand yttrium and calcium. Can Mineral 12, 293-298. nomenclature. Geochimica,4,258-26j (in Chinese with English abstract) The mineral occurs in granite pegmatite at the abandoned Evans-Lou feldspar mine, in the province of The mine is Biteplatinite Quebec. about 22 miles north of Ottawa Caysichite lines cavities as a dull Electron microprobe analysisgave: Pt 39.2,pd 1.2,Te 58.1, Bi white pulverulent coating or as a cream-colored stain. Other. rarer. 6 0, sum 104.5percent, corresponding to (Ptospdo *)(Te, ,rBio,r). occurrences are as thin incrustations with a parallel to slightly White with a strong metallicluster. Mineral grainsare irregular divergent columnar structure with a reniform surface;as radiating to tabular(0.09X0.18-0.1I X0.165 mm). Anisotropic,white under groups and terminated crystals; and as stalactites up to one cm reflected light. Reflectance Rg' : 56.1 (green), 57 8 (orange), long. Most of the following data apply to colorless crusts. The 58.1%(red) VHN : 120-170kg/mm", correspondingro 2.5-3 5 hardnessis 4.! and the VHN is 551. The mineral is non-fluores- on Moh's scale. cent under long or short wave ultra-violet light, but shows a faint Biteplapalladite green cathodoluminescenceunder electron bombardment. Caysi- chite is colorless, white, pale yellow, and rarely greenish. It has a Electron microprobe analysesgave (range): pt pd 7.0_lg 2, vitreous luster and a white streak Caysichite effervescesslowly in l0 9-18 6, Ni l.l-2.1, Te 50.7-588, Bi 12.0-20.0,sum 95.2_ cold, dilute HCI The rare crystals are prismatic, elongated parallel to c and + Minerals marked with an asterisk after the name were ap_ terminated by {001}. A prism and dome were observed under high proved before publication by the Commission on New Minerals magnification but their Miller indices could not be determined. and Mineral Names of the International Mineralogical Associ- Caysichiteis orthorhombic, Ccm2,or Ccmm,a 13.30,b13.95, c9.74 ation. A (N.S. If the form identified as a dome is truly a dome. the choice 174 NEW MINERAL NAMES t75 of spacegroup is narrowed to Ccm2, JAM). The strongest lines in were found to be halhium-rich,in fact to havein part Hf)Zr. The the X-ray powder pattern (in A for CuKa radiation) are:6.93 100 nomenclatureorooosed is: 020.1I 1: 4.38 60 I 30: 4.22 60 310: 3.4860 040'.and 3.32 90 400. Zircon 0-10 mole % HfSiOn Caysichiteis biaxial (-) with a = 1.586+ 0.004,P : | 614 + 10-50 mole % HfSiO4 0.001,r = 1.621+0.001 ,2V meas: 53o,2Vcalc:54"30',X: hafnian Zircon : : b, Y a, Z c for the colorless material. Yellowish crystals are zirconian Hafnon 50-90 mole 7o HfSiOr biaxial(-)witha = 1.589+ 0.004,8 : 1.616+ 0001,.y : | 626 Hafnon 90-100 mole 70 HfSiO4 + 0001, 2V calc:'12"451'(For theseindices the calculated2V should be 61"46' JAM). In immersion mounts, fragments give Probe analysesby Jaakko Siivola on two crystalsfrom Muiane nearly centered acute bisectrix figures suggesting{010} cleavage. gave SiO, 28.32,27.20; HfO, 69.78,72.52; ZrO" 3.28, 1.21,sum Chemical analysis of colorless caysichite (H,O by a modified 101.38,100 93 percent,corresponding to ratios : ez.O, Penfield method; CO, by both loss on ignition minus H,O and by 1g.lwi*- titrimetry; all other constituents by electron microprobe) gave: 97.2, calc6 32,6 48. Crystalswere zoned, with highestHf contents CaO 10.04,Y,O, 28.18,RE oxides(details are given in the paper) at ihe outer edges Other samplesgave ratios 33-78. Plots of the 8.08, SiO, 28.84,Al,Os 0.58, CO, 15.7,H,O 8.6, total 100.02wt unit cells show both a and c to decreasenearly linearly and d to in- percent. Fourteen other elements ranging from 0.01 to 0.05 wt creasewith increasing ratio. End-members are calculated to have percent were determined by mass spectroscopy. The chemical the following parameters. analysis yields a formula of Y, ou Ca, ., REo ., Si. ,, Alo o.O,o," Hfsion (CO'), 3.93 HrO This was calculated on the basis of l9 ZrSiOn "o oxygens(not counting those in the HrO). If the data are recalcu- ao 6 63s 6 567 lated on the basis of a total of 23 (four from H,O) oxygens the resultis Yro" Carn. REo.. SisruAloo" Ororn(Co.)r.n.3.94 HrO In ce 6 02, either case, the ideal formula is (Y,Ca,RE).(Si,Al)4Oro(COs)g d 459 7.00 (measuredds are much lower) : 4H,O. For Z 4, the calculateddensity is 3.029 g/cms, which Crystalswere associatedwith cookeiteand cleavelandite, compares favorably with the measured density of 3.03 g/cm". The name is for the composition DTA, TCA, and IR data are given in the paper. The name is for the composition. Type material is preservedin Discussion the National Mineral Collection.Ottawa. JAM. X-ray powder data and optical data would be helpful.M.F. Jagowerite* Bazirite E. P. MsncHer., M. E. CoArEs,AND A. E. AHo (1973)Jagowerite: J. R. Hlwrss, R. J. MnnnrvlN, R. R. HlnorNc, ANDD. P F. a new barium phosphate from the Yukon Territory. Can. Min- DnnsysHtns(1975) Rockall Island:new geological,petrological, eral 12,135-136. chemicaland Rb-Sr agedata. Inst Geol. Sci.Gr Brit Rep.15/1, il-51. Analysis, recalculated after deducting admixed quartz, gave P,Ou 31.41, Al,O. 25 87, Fe,O, 0.26, BaO 38.41, HrO+ 4.09, preliminary granite A report. Aegirine-riebeckite from Rockall S 0.15, sum 100.19 percent, corresponding to the formula Island (between lceland and the British Isles) was reported by Ba, orAl, ,rFeoo'P, BoSoo2Os(OH)2, or BaAL(PO.)z(OH), Spectro- Sabine in 1960to contain a colorlessmineral containing Ba, Zr, scopic analysis showed the presenceof lessthan 0 I percent of Ca, andSi. Probeanalysis(av.of l9) by Mrs A. E TreshamgaveSiO, Cr,Ti,V,Ta,Nm,Cu, Be, and Sr.
Recommended publications
  • Paolovite Pd2sn C 2001-2005 Mineral Data Publishing, Version 1

    Paolovite Pd2sn C 2001-2005 Mineral Data Publishing, Version 1

    Paolovite Pd2Sn c 2001-2005 Mineral Data Publishing, version 1 Crystal Data: Orthorhombic. Point Group: 2/m 2/m 2/m. As irregular grains embedded in other minerals. Twinning: Polysynthetic. Physical Properties: Hardness = n.d. VHN = 329–378 (10 g load). D(meas.) = n.d. D(calc.) = 11.08 Optical Properties: Opaque. Color: Lilac-rose. Luster: Metallic. Pleochroism: Dark lilac-rose to pale rose. R1–R2: (400) — , (420) 44.4–46.5, (440) 44.6–47.2, (460) 45.0–48.2, (480) 45.5–49.1, (500) 45.9–50.3, (520) 46.7–51.6, (540) 47.7–52.8, (560) 49.0–54.1, (580) 50.9–55.4, (600) 52.9–56.7, (620) 55.3–57.7, (640) 57.7–59.2, (660) 59.8–59.5, (680) 61.5–60.3, (700) 62.7–60.6 Cell Data: Space Group: P bnm. a = 8.11(1) b = 5.662(6) c = 4.324(2) Z = 4 X-ray Powder Pattern: Oktyabr deposit, Russia. 2.28 (100), 2.16 (70), 1.955 (50), 2.36 (40), 1.397 (40), 1.315 (40), 1.120 (40) Chemistry: (1) (2) (3) Pd 64.8 64.3 64.19 Pt 2.5 Sn 35.5 35.0 35.81 Sb 0.3 Bi 0.2 Total 103.3 99.3 100.00 (1) Oktyabr deposit, Russia; by electron microprobe, corresponding to (Pd1.98Pt0.04)Σ=2.02Sn0.98. (2) Western Platinum mine, South Africa; by electron microprobe, corresponding to Pd2.02Sn0.98. (3) Pd2Sn. Occurrence: In Cu–Ni sulfide ores; in cubanite–chalcopyrite, cubanite–talnakhite, and cubanite–mooihoekite assemblages (Oktyabr deposit, Russia).
  • Podiform Chromite Deposits—Database and Grade and Tonnage Models

    Podiform Chromite Deposits—Database and Grade and Tonnage Models

    Podiform Chromite Deposits—Database and Grade and Tonnage Models Scientific Investigations Report 2012–5157 U.S. Department of the Interior U.S. Geological Survey COVER View of the abandoned Chrome Concentrating Company mill, opened in 1917, near the No. 5 chromite mine in Del Puerto Canyon, Stanislaus County, California (USGS photograph by Dan Mosier, 1972). Insets show (upper right) specimen of massive chromite ore from the Pillikin mine, El Dorado County, California, and (lower left) specimen showing disseminated layers of chromite in dunite from the No. 5 mine, Stanislaus County, California (USGS photographs by Dan Mosier, 2012). Podiform Chromite Deposits—Database and Grade and Tonnage Models By Dan L. Mosier, Donald A. Singer, Barry C. Moring, and John P. Galloway Scientific Investigations Report 2012-5157 U.S. Department of the Interior U.S. Geological Survey U.S. Department of the Interior KEN SALAZAR, Secretary U.S. Geological Survey Marcia K. McNutt, Director U.S. Geological Survey, Reston, Virginia: 2012 This report and any updates to it are available online at: http://pubs.usgs.gov/sir/2012/5157/ For more information on the USGS—the Federal source for science about the Earth, its natural and living resources, natural hazards, and the environment—visit http://www.usgs.gov or call 1–888–ASK–USGS For an overview of USGS information products, including maps, imagery, and publications, visit http://www.usgs.gov/pubprod To order this and other USGS information products, visit http://store.usgs.gov Suggested citation: Mosier, D.L., Singer, D.A., Moring, B.C., and Galloway, J.P., 2012, Podiform chromite deposits—database and grade and tonnage models: U.S.
  • Abstract in PDF Format

    Abstract in PDF Format

    PGM Associations in Copper-Rich Sulphide Ore of the Oktyabr Deposit, Talnakh Deposit Group, Russia Olga A. Yakovleva1, Sergey M. Kozyrev1 and Oleg I. Oleshkevich2 1Institute Gipronickel JS, St. Petersburg, Russia 2Mining and Metallurgical Company “Noril’sk Nickel” JS, Noril’sk, Russia e-mail: [email protected] The PGM assemblages of the Cu-rich 6%; the Ni content ranges 0.8 to 1.3%, and the ratio sulphide ores occurring in the western exocontact Cu/S = 0.1-0.2. zone of the Talnakh intrusion and the Kharaelakh Pyrrhotite-chalcopyrite ore occurs at the massive orebody have been studied. Eleven ore top of ore horizons. The ore-mineral content ranges samples, weighing 20 to 200 kg, were processed 50 to 60%, and pyrrhotite amount is <15%. The ore using gravity and flotation-gravity techniques. As a grades 1.1 to 1.3% Ni, and the ratio Cu/S = 0.35- result, the gravity concentrates were obtained from 0.7. the ores and flotation products. In the gravity Chalcopyrite ore occurs at the top and on concentrates, more than 20,000 PGM grains were the flanks of the orebodies. The concentration of found and identified, using light microscopy and sulphides ranges 50 to 60%, and pyrrhotite amount EPMA. The textural and chemical characteristics of is <1%; the Ni content ranges 1.3 to 3.4%, and the PGM were documented, as well as the PGM ratio Cu/S = 0.8-0.9. distribution in different size fractions. Also, the The ore types are distinctly distinguished balance of Pt, Pd and Au distribution in ores and by the PGE content which directly depends on the process products and the PGM mass portions in chalcopyrite quantity, but not on the total sulphide various ore types were calculated.
  • Chapter 9 Gold-Rich Porphyry Deposits: Descriptive and Genetic Models and Their Role in Exploration and Discovery

    Chapter 9 Gold-Rich Porphyry Deposits: Descriptive and Genetic Models and Their Role in Exploration and Discovery

    SEG Reviews Vol. 13, 2000, p. 315–345 Chapter 9 Gold-Rich Porphyry Deposits: Descriptive and Genetic Models and Their Role in Exploration and Discovery RICHARD H. SILLITOE 27 West Hill Park, Highgate Village, London N6 6ND, England Abstract Gold-rich porphyry deposits worldwide conform well to a generalized descriptive model. This model incorporates six main facies of hydrothermal alteration and mineralization, which are zoned upward and outward with respect to composite porphyry stocks of cylindrical form atop much larger parent plutons. This intrusive environment and its overlying advanced argillic lithocap span roughly 4 km vertically, an interval over which profound changes in the style and mineralogy of gold and associated copper miner- alization are observed. The model predicts a number of geologic attributes to be expected in association with superior gold-rich porphyry deposits. Most features of the descriptive model are adequately ex- plained by a genetic model that has developed progressively over the last century. This model is domi- nated by the consequences of the release and focused ascent of metalliferous fluid resulting from crys- tallization of the parent pluton. Within the porphyry system, gold- and copper-bearing brine and acidic volatiles interact in a complex manner with the stock, its wall rocks, and ambient meteoric and connate fluids. Although several processes involved in the evolution of gold-rich porphyry deposits remain to be fully clarified, the fundamental issues have been resolved to the satisfaction of most investigators. Explo- ration for gold-rich porphyry deposits worldwide involves geologic, geochemical, and geophysical work but generally employs the descriptive model in an unsophisticated manner and the genetic model hardly at all.
  • Mineral Processing

    Mineral Processing

    Mineral Processing Foundations of theory and practice of minerallurgy 1st English edition JAN DRZYMALA, C. Eng., Ph.D., D.Sc. Member of the Polish Mineral Processing Society Wroclaw University of Technology 2007 Translation: J. Drzymala, A. Swatek Reviewer: A. Luszczkiewicz Published as supplied by the author ©Copyright by Jan Drzymala, Wroclaw 2007 Computer typesetting: Danuta Szyszka Cover design: Danuta Szyszka Cover photo: Sebastian Bożek Oficyna Wydawnicza Politechniki Wrocławskiej Wybrzeze Wyspianskiego 27 50-370 Wroclaw Any part of this publication can be used in any form by any means provided that the usage is acknowledged by the citation: Drzymala, J., Mineral Processing, Foundations of theory and practice of minerallurgy, Oficyna Wydawnicza PWr., 2007, www.ig.pwr.wroc.pl/minproc ISBN 978-83-7493-362-9 Contents Introduction ....................................................................................................................9 Part I Introduction to mineral processing .....................................................................13 1. From the Big Bang to mineral processing................................................................14 1.1. The formation of matter ...................................................................................14 1.2. Elementary particles.........................................................................................16 1.3. Molecules .........................................................................................................18 1.4. Solids................................................................................................................19
  • Revision 1 Extreme Fractionation from Zircon to Hafnon in the Koktokay No

    Revision 1 Extreme Fractionation from Zircon to Hafnon in the Koktokay No

    This is a preprint, the final version is subject to change, of the American Mineralogist (MSA) Cite as Authors (Year) Title. American Mineralogist, in press. (DOI will not work until issue is live.) DOI: http://dx.doi.org/10.2138/am.2013.4494 6/19 1 Revision 1 2 3 Extreme fractionation from zircon to hafnon in the Koktokay No. 4 1 granitic pegmatite, Altai, northwestern China 5 6 Rong Yin1, Ru Cheng Wang1,*, Ai-Cheng Zhang1, Huan Hu1, Jin Chu Zhu1, Can Rao2, and 7 Hui Zhang3 8 9 1State Key Laboratory for Mineral Deposits Research, School of Earth Sciences and 10 Engineering, Nanjing University, Nanjing 210093, China; 11 2Department of Earth Sciences, Zhejiang University, Hangzhou 310027, China; 12 3Institute of Geochemistry, Chinese Academy of Sciences, Guiyang, 550002, China. 13 14 *E-mail: [email protected] 15 Always consult and cite the final, published document. See http://www.minsocam.org or GeoscienceWorld This is a preprint, the final version is subject to change, of the American Mineralogist (MSA) Cite as Authors (Year) Title. American Mineralogist, in press. (DOI will not work until issue is live.) DOI: http://dx.doi.org/10.2138/am.2013.4494 6/19 16 ABSTRACT 17 The Koktokay No. 1 pegmatite is a Li–Cs–Ta-rich granitic pegmatite located in Altai, 18 northwestern China. Zircon is present in most textural zones of this pegmatite and in its 19 contact zone with surrounding metagabbro. Here we describe the detailed associations of 20 zircon with other minerals, and the internal textures and chemistry of the zircons.
  • Thermal Annealing and Phase Transformation of Serpentine-Like Garnierite

    Thermal Annealing and Phase Transformation of Serpentine-Like Garnierite

    minerals Article Thermal Annealing and Phase Transformation of Serpentine-Like Garnierite Arun Kumar 1,2 , Michele Cassetta 1, Marco Giarola 3, Marco Zanatta 4 , Monique Le Guen 5, Gian Domenico Soraru 6 and Gino Mariotto 1,* 1 Department of Computer Science, University of Verona, 37134 Verona, Italy; [email protected] (A.K.); [email protected] (M.C.) 2 CNR-Institute for Microelectronics and Microsystems, Agrate Brianza, 20864 Agrate, Italy 3 Centro Piattaforme Tecnologiche (CPT), University of Verona, 37134 Verona, Italy; [email protected] 4 Department of Physics, University of Trento, 38123 Povo, Italy; [email protected] 5 Innovation Technology Direction, ERAMET IDEAS, 78190 Trappes, France; [email protected] 6 Department of Industrial Engineering, University of Trento, 38123 Povo, Italy; [email protected] * Correspondence: [email protected] Abstract: This study is focused on the vibrational and microstructural aspects of the thermally induced transformation of serpentine-like garnierite into quartz, forsterite, and enstatite occur- ring at about 620 ◦C. Powder specimens of garnierite were annealed in static air between room temperature and 1000 ◦C. The kinetic of the transformation was investigated by means of thermo- gravimetric and differential thermal analysis, and the final product was extensively characterized via micro-Raman spectroscopy and X-ray diffraction. Our study shows that serpentine-like garnierite consists of a mixture of different mineral species. Furthermore, these garnierites and their compo- sition can provide details based on the mineralogy and the crystalline phases resulting from the thermal treatment. Citation: Kumar, A.; Cassetta, M.; Giarola, M.; Zanatta, M.; Le Guen, M.; Keywords: garnierite; phase transformation; TGA/DSC; XRD; micro-Raman spectroscopy Soraru, G.D.; Mariotto, G.
  • Alamosite Pbsio3 C 2001 Mineral Data Publishing, Version 1.2 ° Crystal Data: Monoclinic

    Alamosite Pbsio3 C 2001 Mineral Data Publishing, Version 1.2 ° Crystal Data: Monoclinic

    Alamosite PbSiO3 c 2001 Mineral Data Publishing, version 1.2 ° Crystal Data: Monoclinic. Point Group: 2=m: Crystals ¯brous [010]; as radiating aggregates and balls, to 7.5 cm. k Physical Properties: Cleavage: Perfect on 010 . Hardness = 4.5 D(meas.) = 6.488(3) D(calc.) = [6.30] f g Optical Properties: Transparent to translucent. Color: Colorless to white, cream, or light gray. Luster: Adamantine. Optical Class: Biaxial ({). Orientation: Y = b. Dispersion: r < v; strong, weak inclined. ® = 1.945{1.947 ¯ = 1.955{1.961 ° = 1.959{1.968 2V(meas.) = 65± Cell Data: Space Group: P 2=n: a = 12.247 b = 7.059 c = 11.236 ¯ = 113:12± Z = 12 X-ray Powder Pattern: Tsumeb, Namibia. 3.34 (100), 3.56 (95), 3.53 (75), 2.300 (75), 3.23 (70), 2.987 (70), 3.25 (60) Chemistry: (1) (2) (3) SiO2 21.11 20.01 21.21 Al2O3 0.09 FeO 0.09 0.18 MnO 0.02 PbO 78.13 78.95 78.79 CaO trace 0.09 insol: 0.61 Total 99.94 99.34 100.00 (1) Alamos, Mexico. (2) Tsumeb, Namibia; by electron microprobe. (3) PbSiO3: Occurrence: As a rare secondary mineral in the oxidized zone of lead-bearing base metal deposits. Association: Wulfenite, leadhillite, cerussite (Alamos, Mexico); leadhillite, anglesite, melanotekite, °eischerite, kegelite, hematite (Tsumeb, Namibia); diaboleite, phosgenite, cerussite, wulfenite, willemite (Tiger, Arizona, USA); melanotekite, shattuckite, wickenburgite (Rawhide mine, Arizona, USA). Distribution: From Mexico, in Sonora, at Alamos, and the San Pascual mine, near Zimap¶an, Hidalgo. In the USA, from Arizona, in the Mammoth-St.
  • Wickenburgite Pb3caal2si10o27² 3H2O

    Wickenburgite Pb3caal2si10o27² 3H2O

    Wickenburgite Pb3CaAl2Si10O27 ² 3H2O c 2001 Mineral Data Publishing, version 1.2 ° Crystal Data: Hexagonal. Point Group: 6=m 2=m 2=m: Tabular holohedral crystals, dominated by 0001 and 1011 , to 1.5 mm. As spongy aggregates of small, highly perfect f g f g individuals; as subparallel aggregates or rosettes; granular. Physical Properties: Cleavage: 0001 , indistinct. Tenacity: Brittle but tough. Hardness = 5 D(meas.) = 3.85 D(cfalc.) g= 3.88 Fluoresces dull orange under SW UV. Optical Properties: Transparent to translucent. Color: Colorless to white; rarely salmon-pink. Luster: Vitreous. Optical Class: Uniaxial ({). Dispersion: r < v; moderate. ! = 1.692 ² = 1.648 Cell Data: Space Group: P 63=mmc: a = 8.53 c = 20.16 Z = 2 X-ray Powder Pattern: Near Wickenburg, Arizona, USA. 10.1 (100), 3.26 (80), 3.93 (60), 3.36 (40), 2.639 (40), 5.96 (30), 5.04 (30) Chemistry: (1) (2) SiO2 42.1 40.53 Al2O3 7.6 6.88 PbO 44.0 45.17 CaO 3.80 3.78 H2O 3.77 3.64 Total 101.27 100.00 (1) Near Wickenburg, Arizona, USA. (2) Pb3CaAl2Si10O24(OH)6: [needsnew??formula] Occurrence: In oxidized hydrothermal veins, carrying galena and sphalerite, in quartz and °uorite gangue (near Wickenburg, Arizona, USA). Association: Phoenicochroite, mimetite, cerussite, willemite, crocoite, duftite, hemihedrite, alamosite, melanotekite, luddenite, ajoite, shattuckite, vauquelinite, descloizite, laumontite. Distribution: In the USA, in Arizona, at several localities south of Wickenburg, Maricopa Co., including the Potter-Cramer property, Belmont Mountains, and the Moon Anchor mine; on dumps at a Pb-Ag-Cu prospect in the Artillery Peaks area, Mohave Co.; and in the Dives (Padre Kino) mine, Silver district, La Paz Co.
  • Chapter 11 Applications of Ore Microscopy in Mineral Technology

    Chapter 11 Applications of Ore Microscopy in Mineral Technology

    CHAPTER 11 APPLICATIONS OF ORE MICROSCOPY IN MINERAL TECHNOLOGY 11.1 INTRODUCTION The extraction of specific valuable minerals from their naturally occurring ores is variously termed "ore dressing," "mineral dressing," and "mineral beneficiation." For most metalliferous ores produced by mining operations, this extraction process is an important intermediatestep in the transformation of natural ore to pure metal. Although a few mined ores contain sufficient metal concentrations to require no beneficiation (e.g., some iron ores), most contain relatively small amounts of the valuable metal, from perhaps a few percent in the case ofbase metals to a few parts per million in the case ofpre­ cious metals. As Chapters 7, 9, and 10ofthis book have amply illustrated, the minerals containing valuable metals are commonly intergrown with eco­ nomically unimportant (gangue) minerals on a microscopic scale. It is important to note that the grain size of the ore and associated gangue minerals can also have a dramatic, and sometimes even limiting, effect on ore beneficiation. Figure 11.1 illustrates two rich base-metal ores, only one of which (11.1b) has been profitably extracted and processed. The McArthur River Deposit (Figure I 1.1 a) is large (>200 million tons) and rich (>9% Zn), but it contains much ore that is so fine grained that conventional processing cannot effectively separate the ore and gangue minerals. Consequently, the deposit remains unmined until some other technology is available that would make processing profitable. In contrast, the Ruttan Mine sample (Fig. 11.1 b), which has undergone metamorphism, is relativelycoarsegrained and is easily and economically separated into high-quality concentrates.
  • Chemical Composition and Petrogenetic Implications of Eudialyte-Group Mineral in the Peralkaline Lovozero Complex, Kola Peninsula, Russia

    Chemical Composition and Petrogenetic Implications of Eudialyte-Group Mineral in the Peralkaline Lovozero Complex, Kola Peninsula, Russia

    minerals Article Chemical Composition and Petrogenetic Implications of Eudialyte-Group Mineral in the Peralkaline Lovozero Complex, Kola Peninsula, Russia Lia Kogarko 1,* and Troels F. D. Nielsen 2 1 Vernadsky Institute of Geochemistry and Analytical Chemistry, Russian Academy of Sciences, 119991 Moscow, Russia 2 Geological Survey of Denmark and Greenland, 1350 Copenhagen, Denmark; [email protected] * Correspondence: [email protected] Received: 23 September 2020; Accepted: 16 November 2020; Published: 20 November 2020 Abstract: Lovozero complex, the world’s largest layered peralkaline intrusive complex hosts gigantic deposits of Zr-, Hf-, Nb-, LREE-, and HREE-rich Eudialyte Group of Mineral (EGM). The petrographic relations of EGM change with time and advancing crystallization up from Phase II (differentiated complex) to Phase III (eudialyte complex). EGM is anhedral interstitial in all of Phase II which indicates that EGM nucleated late relative to the main rock-forming and liquidus minerals of Phase II. Saturation in remaining bulk melt with components needed for nucleation of EGM was reached after the crystallization about 85 vol. % of the intrusion. Early euhedral and idiomorphic EGM of Phase III crystalized in a large convective volume of melt together with other liquidus minerals and was affected by layering processes and formation of EGM ore. Consequently, a prerequisite for the formation of the ore deposit is saturation of the alkaline bulk magma with EGM. It follows that the potential for EGM ores in Lovozero is restricted to the parts of the complex that hosts cumulus EGM. Phase II with only anhedral and interstitial EGM is not promising for this type of ore.
  • Fourth International Kimberlite Conference: Extended Abstracts

    Fourth International Kimberlite Conference: Extended Abstracts

    ROLE OP SULPIDES IN THE EVOLUTION OP MANTLE ROCKS OP BASIC AND ULTRABASIC COLPOSITION AND IN THE EMERGENCE OP KBvlBERLITE BODIES V.K.Garanin, G«P.Kudryavtseva and A.N.Krot Department of Geology, Moscow State University, USSR In kimberlite bodies sulfides occur in diamonds, in xenocrysts of garnet, olivine, zircon, pyroxene, ilmenite, chromespinel, in xenoliths of abyssal rocks of basic and ultrabasic composition and in kimberlite rocks themselves. Such heterogeneity is associated with the different stages in the evolution of mantle rocks and kimberlite melts. Sulfides are represented by magmatic, metasomatic and superimposed hydrothermal minerals. Sulfide nodules are developed in xenocrysts, diamonds and abyssal rocks have a complicated zonal structure. Core of nodules is composed either of quenched sulfide melt based on Pe and Ni or pyrrho- tite and pentlandite in various combinations; internal part (outside the core) broken rim is composed of Go-containing pentlandite, external one - of chalcopyrite (Pig.I), sometimes with bornite or djerfisherite (Pig.2). The latter is encountered only in ilmenitic rocks. In accordance with paragenesis of these minerals, diamond included, a regular evolution of the initial sulfide melt entrapped by minerals is traced (Pig.3). Composition of the initial sulfide melt in minerals of eclogitic paragenesis is extremelv poor in Ni (less than 3 mass.%) and enriched with Pe (over 55 mass.%}; in minerals of ultrabasic magne¬ sian-ferriferous (ilmenite) series the amount of Ni is greater (from 2,5 to 10 mass.%), while that of Pe is less (from 51 to 56 rnass.^); in minerals of ultrabasic magnesian paragenesis the melt is substantially enriched with Ni (20-26 mass./S) and poor in Pe (34-40 mass.%).