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The Fe-REE Ore Deposit hosted by carbonate-alkali ultrabasic complex in Hongcheon, S. Korea.
Published in Adam Piestrzyński, Mineral Deposits at the Beginning of the 21st Century, 2001
Studied area located on the marginal part of tectonic province of Gyunggi gneiss complexes of Korean peninsula includes banded gneiss, biotite gneiss and biotite-hornblende gneiss. Carbonates and alkali-ultramafic injection complexes showing narrow and long sheet shape (20∼50m width, 2500m total length) with norh-south trend are developed in biotite-hornblende gneisses. The major minerals of injection complexes are ferroan dolomite and magnetite, and accessories are monazite, strontianite, columbite, fergusonite, calcite, siderite, ankerite, chlorite, apatite, aegirine-augite, tirodite, acmite, pyrite, molybdenite and barite. Chemical formula of strontianite from microprobe analysis shows Ca0.02-0.16Sr0.84-0.98CO3 and Sr partly is replaced by Ca. Reddish part of columbite without Ta is mangano-columbite (Mn0.57Fe0.24Mg0.19)Nb2O6, and opaque part is ferrocolumbite (Fe0.82Mn0.15Mg0.03)Nb2O6. Fergusonite has minor P and no Ta and its formula is (REE0.90Ca0.06Th0.05)NbO4. Mineral textures from microscopic observation prove that monazite and magnetite originate from the same magma source that formed carbonate minerals.
Properties of the Elements and Inorganic Compounds
Published in W. M. Haynes, David R. Lide, Thomas J. Bruno, CRC Handbook of Chemistry and Physics, 2016
W. M. Haynes, David R. Lide, Thomas J. Bruno
Name Acanthite Actinolite Aegirine Akermanite Alabandite Albite Allanite Allemontite Almandine Altaite Aluminite Alunite Amblygonite Analcite Anatase Andalusite Andesine Andorite Andradite Anglesite Anhydrite Ankerite Anorthite Anorthoclase Anthophyllite Apatite Apophyllite Aragonite Argentite Arsenolite Arsenopyrite Atacamite Augelite Augite Autunite Axinite Azurite Baddeleyite Barite Benitoite Formula Ag2S Ca2(Mg,Fe)5Si8O22(OH,F)2 NaFe(SiO3)2 Ca2MgSi2O7 MnS NaAlSi3O8 (Ca,Mn,Ce,La,Y,Th)2(Fe,Ti)(Al,Fe) OOH(Si2O7)(SiO4) SbAs Fe3Al2Si3O12 PbTe Al2(SO4)(OH)47H2O KAl3(SO4)2(OH)6 (Li,Na)Al(PO4)(F,OH) NaAl(SiO3)2H2O TiO2 Al2OSiO4 NaAlSi3O8CaAl2Si2O8 PbAgSb3S6 Ca3Fe2Si3O12 PbSO4 CaSO4 Ca(Fe,Mg,Mn)(CO3)2 CaAl2Si2O8 (Na,K)AlSi3O8 Mg7Si8O22(OH)2 Ca5(PO4)3(OH,F,Cl) KFCa4Si8O208H2O CaCO3 Ag2S As2O3 FeAsS Cu2(OH)3Cl Al2(PO4)(OH)3 (Ca,Mg,Fe,Ti,Al)2(Si,Al)2O6 Ca(UO2)2(PO4)210H2O (Ca,Mn,Fe)3Al2BO3Si4O12(OH) Cu3(OH)2(CO3)2 ZrO2 BaSO4 BaTi(SiO3)3 Crystal system orthorhombic monoclinic monoclinic tetragonal cubic triclinic monoclinic hexagonal cubic cubic monoclinic rhombohedral triclinic cubic tetragonal orthorhombic triclinic rhombohedral cubic orthorhombic orthorhombic rhombohedral triclinic triclinic rhombohedral hexagonal tetragonal orthorhombic orthorhombic cubic monoclinic rhombohedral monoclinic monoclinic tetragonal triclinic monoclinic monoclinic orthorhombic rhombohedral /g cm-3 7.2 3.23 3.58 2.94 4.0 2.63 3.8 6.0 4.32 8.16 1.74 2.8 3.1 2.27 4.23 3.15 2.67 2.67 3.86 6.29 2.96 3.0 2.76 2.58 3.21 3.2 2.35 2.83 7.2 3.86 6.1 3.76 2.70 3.38 3.2 3.31 3.77 5.7 4.49 3.65 Hardness 2.3 5.5 6 5.5 3.8 6.3 5.8 3.5 6.8 3 1.5 3.8 5.8 5.5 5.8 7.5 6.3 3.3 6.8 2.8 3.5 3.8 6.3 6 5.8 5 4.8 3.5 2.3 1.5 5.8 3.3 4.8 6 2.3 6.8 3.8 6.5 3.3 6.3 n 1.624 1.763 1.632 1.527 1.75 1.830 1.459 1.572 1.591 1.486 2.488 1.635 1.550 1.887 1.877 1.570 1.529 1.577 1.523 1.645 1.645 1.535 1.531 1.755 1.831 1.574 1.703 1.553 1.684 1.730 2.13 1.636 1.757 1.861 1.576 1.707 1.577 1.691 1.758 2.19 1.637 1.804 1.880 1.588 1.738 1.694 1.838 2.20 1.648 1.464 1.592 1.604 2.561 1.639 1.553 1.470 1.613 n 1.655 1.800 1.640 1.531 1.78 n 1.664 1.815
Oldest syenitic intrusions of the Yilgarn Craton identified at Karari gold deposit, Carosue Dam camp, Western Australia?
Published in Australian Journal of Earth Sciences, 2023
W. K. Witt, C. Fisher, S. G. Hagemann, M. P. Roberts
Granitic rocks, which dominate the near-surface geology of the Yilgarn Craton, have been subdivided into two major and three minor groups, by Champion and Sheraton (1997). Cassidy et al. (2002) subdivided the groups into supersites and suites. One of the minor groups, named the Syenitic Group, is equivalent to the Gilgarna Supersuite of Witt and Davy (1997a, 1997b). This association comprises alkali-rich, quartz-poor intrusions classified as monzodiorite, syenite, quartz syenite, quartz monzonite and alkali granite. Ferromagnesian minerals are typically clinopyroxene (including aegirine and aegirine-augite) and, in some cases, blueish sodic amphibole (Libby, 1989; Witt & Davy, 1997a). Typical accessory minerals are magnetite, titanite and apatite. The Syenitic Group intrusions are mostly restricted to the Kurnalpi Terrane of the Kalgoorlie-Kurnalpi Rift, in the Eastern Goldfields Superterrane (Figure 1; Witt et al., 2018).
A review of major rare earth element and yttrium deposits in China
Published in Australian Journal of Earth Sciences, 2022
Early to middle Permian alkaline and calc-alkaline granitic complexes are located in an east-trending zone covering hundreds of square kilometres in the Northern Tarim Basin (Sui & Huang, 2007; Wang et al., 2007; Yang et al., 2001; Zou & Li, 2006). The types of intrusion present include syenite, alkali-feldspar granite and aegirine-pyroxene-bearing granite formed in a post-collisional extensional setting (Liu et al., 2004; Liu & Yuan, 1996; Zhang, 1997). REY mineralisation is present in Permian syenogranite, bioclastic limestone, fine-grained limestone interbedded with calcareous siltstone, and marble and schist in the Paleoproterozoic Xingditage Schist. Rich REY mineralisation is also present in pegmatite veins and sodium-aegirine granites at the top of granitic stocks, and in aegirine–albite granitic dykes intruding marble. A model showing the tectonic history and REY mineralisation in the district is illustrated in Figure 7.
Petrology and petrogenesis of an intraplate alkaline lamprophyre-phonolite-carbonatite association in the Alpine Dyke Swarm, New Zealand
Published in New Zealand Journal of Geology and Geophysics, 2020
The close spatial association of phonolites and carbonatites, their similar radiogenic and stable isotopic compositions (Barreiro and Cooper 1987; Cooper and Paterson 2008), coupled with the similarity in composition of minerals common to the two rock types (e.g aegirine-rich clinopyroxenes, Cooper 1986, his Figure 4) led to the interpretion that the two magmas most probably originated by immiscibility. In Figure 11, the most alkali-rich phonolites have compositions that plot along the silicate limb of a silicate melt-carbonatite miscibility gap defined by both experimental work (e.g. Brooker and Hamilton 1990; Lee and Wyllie 1997, 1998) and the compositions of natural melt inclusions in minerals from carbonatite complex rocks (e.g. Guzmics et al. 2011). The miscibility gap is dependent on P-T conditions, CO2 and H2O saturation, and parent-rock geochemistry, but with the solvus shown in Figure 11, the conjugate liquid that would coexist with alkali-rich ADS phonolite is an alkali-rich carbonatite. Compositions of ADS carbonatites, like the vast majority of carbonatites elsewhere in the world, cluster along the (SiO2 +Al2O3 +TiO2)–(CaO + MgO + FeO) join and are depleted in alkalis. The development of albite-aegirine ± riebeckite/arfvedsonite fenite from the country rock quartzofeldspathic schist along carbonatite contacts clearly demonstrates how alkalis can be removed from the host carbonatite as a metasomatic fenitising fluid.