PČ

Petr Černý

Jan Evangelista Purkyně University in Ústí nad Labem

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F. C. Hawthorne

University of Manitoba

Ron Chapman

University of Manitoba

Milan Novák

Masaryk University

David K. Teertstra

University of Manitoba

T. S. Ercit

Canadian Museum of Nature

Michael A. Wise

National Museum of Natural History

J. B. Selway

University of Manitoba

Pavel Uher

Comenius University Bratislava

Luisa Ottolini

Institute of Geosciences and Earth Resources

MÁ

Miguel Ángel Galliski

Centro Científico Tecnológico - Mendoza

Cooperative Institutions

University of Manitoba

University of Winnipeg

Masaryk University

Uppsala University

Queen's University

Geological Survey of Canada

Charles University

University of British Columbia

Consejo Nacional de Investigaciones Científicas y Técnicas

Geological Institute

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Parabariomicrolite, a new species, and its structural relationship to the pyrochlore group

The Canadian Mineralogist (1986)

T. S. Ercit F. C. Hawthorne Petr Černý

Parabariomicrolite _BaTa401O(OHh.2H20 is rhomb,9hedral, spac~ group R3m, with a 7.4290(6), c 18.505(2) A, V 884.5(1) A, Z = 3. The ~trongest six lines in the X-ray powder pattern [d in A(I)(hkl)] are 6.18(50)(00.3), 3.172(65)(02.1), 3.085(41)(00.6), 3.040(10.0)(20.2), 2.641(50)(02.4), 1.591(42)(22.6). Electron-microprobe anal ysis gives Na20 0.4, K20 0.3, srO 0.8, BaO 10.5, PbO 0.4, Nb20s'1.5, Ta20S 80.6, 1: = 94.5 wt. %; crystal-structure arguments indicate 5.2 wt.% H20, to give a total 1: =99.7 wt. %. Parabariomicrolite is translucent, white to pale pink, has a white streak and a vitreous to pearly lustre. It has well-developed {OOl} and {101} cleavages, is very brittle and has a Mohs hardness of 4; D(calc) 5.97 g/cm3• It is optically anisotropic, with all n in excess of 2.0. Parabario microlite typically occurs as topotaxic replacements of microlite and more rarely as open-space fillings in oxide mineral assemblages of the Alto do Giz pegmatite, Brazil. Its crystal structure was solved by crystal-chemical argu ments, augmented by X-ray powder-diffraction data. Its layer structure is derived from that of pyrochlore. One layer has 6- and 3-membered rings of corner-sharing (TaO~ octahedra, with [8]-co-ordinated Balying at the centre of the 6-membered rings; this layer is topologically identical with the analogous layer in pyrochlore. The second layer is very sparsely occupied by (TaO~ octahedra; the analo gous layer in pyrochlore is much more densely occupied (by large cations). It is the relative ordering of large cations in the fIrst layer and vacancies in the second layer that result in the lowering of symmetry from Fd3m to R3m.

Pegmatite

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Citations (16)

The Greer Lake leucogranite, Manitoba, and the origin of lepidolite-subtype granitic pegmatites

Lithos (2004)

Petr Černý M. Masau Bruce E. Goad K. Ferreira

Pegmatite

Leucogranite

Anatexis

Greenstone belt

10.1016/j.lithos.2003.11.003

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Citations (52)

RADIOGENIC ISOTOPE SYSTEMATICS OF THE HURON CLAIM PEGMATITE AND THE SHATFORD LAKE PEGMATITE GROUP, WINNIPEG RIVER PEGMATITE DISTRICT, MANITOBA

The Canadian Mineralogist (2014)

Alfredo Camacho H. Baadsgaard Brian J. Paul Petr Černý

Abstract The Huron Claim pegmatite and members of the Shatford Lake group are a NYF-like granitic pegmatite population located amidst the dominant LCT-family pegmatites of the Winnipeg River pegmatite district, Manitoba. The age of intrusion of the Shatford Lake pegmatites was established by the U/Pb method using gadolinite-(Y) and gave a concordant 2656.1 ± 1.4 Ma age. A subsequent age-resetting event at ~2580 Ma was given by U/Pb analyses of uraninite from the Huron Claim pegmatite and is supported in some measure by Rb-Sr data from micas. Monazite-(Ce) and ferrocolumbite U/Pb analyses yielded ages between the gadolinite-(Y) and uraninite ages, indicating partial age-resetting of both minerals. A further resetting event is revealed by post-2580 Ma gains and losses in radiogenic Sr and Pb in feldspars. These NYF pegmatites are in close proximity to or cut by crustal-scale shear zones. Consequently, we interpret the ca. 2580 and post-2580 Ma overprints to indicate late-stage reactivation and fluid flow along these major structures.

Pegmatite

Radiogenic nuclide

10.3749/canmin.1400041

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Citations (1)

Compositional variations in ferrotapiolite+tantalite pairs fromthe beryl-columbite pegmatite at Moravany nad Váhom, Slovakia.

Mineralogy and Petrology (2000)

Milan Novák Pavel Uher Petr Černý Pavol Siman

Pegmatite

Columbite

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Citations (6)

Bederite, a new pegmatite phosphate mineral from Nevados de Palermo, Argentina; description and crystal structure

American Mineralogist (1999)

Miguel Ángel Galliski Mark A. Cooper F. C. Hawthorne Petr Černý

Galliski and Sureda (1982) reported nodules of a phosphate mineral that they classified generically as a member of the alluaudite group.The X-ray diffraction pattern was similar to that of wicksite (Sturman et al. 1981), but wet-chemical analysis (Galliski and Sureda 1982) gave a significantly different chemical composition, with MnO dominant over FeO, and suggested strong similarities with the unnamed wicksite-like phase of Peacor et al. (1985).Solution of the crystal structure of the phase showed that it is isostructural but chemically distinct from wicksite.The Commission of New Minerals and Mineral Names of the International Mineralogical Association has approved the mineral and the name: bederite.The name honors Roberto Beder (born in Basel, Switzerland and died in Córdoba, Argentina: 1888-1930) for his major contribution to the development of Mineralogy in Argentina, particularly his work in morphological crystallography.Holotype and cotype samples

Pegmatite

Phosphate minerals

10.2138/am-1999-1022

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Citations (10)

FERUVITE FROM LEPIDOLITE PEGMATITES AT RED CROSS LAKE, MANITOBA

The Canadian Mineralogist (1998)

J. B. Selway Petr Černý F. C. Hawthorne

Feruvite occurs in the Ca-rich exocontacts of lepidolite-subty pe granitic pegmatites in the Red Cross Lake pegmatite field, northeastern Manitoba. The pegmatites intrude meta-andesitic to metabasaltic host-rocks. ln addition to tourmaline, exocontacts contain Cs-and Rb-rich biotite, Fe-rich muscovite, epidote, apatite, Ca-rich garnet, titanite, calcite, quartz and arsenopyrite. The tourmaline is commonly zoned, with a core offeruvite surrounded by schorl or dravite, and rimmed by uvite. The most extreme composition of feruvite analyzed is (Ca0_5 6Na0_39)l:0 .95 (Fe2 •�. 9oMg0_8 1Li0_18Ti0_04 Mn001));3 _00(Al,_31Mg o_6 9)l:6.oo(BO,),Si6 .o70 rs [(OH3 51)F0_4 9]);4_00; the X, Y, and Z sites are dominated by Ca, Fe and AI, respectively. Magnesium is a significant component at the Y and Z sites. In plane-polarized light, uvite and dravite are mainly pale blue or blue, and feruvite and schorl are mainly dark blue. Brown schorl and feruvite tend to be rich inTi. The meta-andesitic and metabasaltic wallrocks provided the Fe and Ca for contact-metasoma tic reactions between the wallrocks and the intruding pegmatite to produce feruvite.

Pegmatite

Tourmaline

Titanite

Muscovite

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Citations (21)

Subsolidus behavior of niobian rutile from Vezna, CzechRepublic: a model for exsolution in phases with Fe2+ >> Fe3+.

Journal of Geosciences (2000)

Petr Černý Milan Novák Ron Chapman M. Masau

Subsolidus behavior of niobian rutile from Vezna, Czech Republic: a model for exsolution in phases with Fe2+ >> Fe3+.

Rutile