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REE Mineralogy and Resources Chapter 279 197 (Y,REE)3Si6O182H2O], kainosite-(Y) [Ca2(Y,Ce)2Si4O12(CO3)H2O], etc. (Kerr and Rafuse, 2012). The Strange Lake deposit is hosted by the 1.2 Ga Strange Lake peralkaline granite, a cylindrical body about 6 km in diameter, which intruded in Archean basement rocks in northeastern Canada. The rare earth mineralization was found at Main zone and B zone, which are hosted in subsolvus granite, con- taining discrete K-feldspar and albite crystals, that fringes the fresh less evolved hypersolvus granite core. The main zone consists of lower grade part where REE-bearing minerals are disseminated in the subsolvus granite, and higher grade pegmatite and aplite lens enriched in Zr, Nb, and REEs. The B zone is similar to the high-grade part of the Main zone with pervasive alteration with hematite (Kerr and Rafuse, 2012). Salvi and Williams-Jones (1996) interpreted that the REE mineralization at Strange Lake, which is enriched in Ca-silicates, occurred at low temperature ( 200°C) condition by the introduction of Ca-rich meteoric or formation water subsequent to high temperature (!350°C) alteration attributed to Ca-free magmatic fluids. The rare earth deposits associated with alkaline volcanic rocks are Dubbo in Australia and Round Top in the United States. The Dubbo deposit is com- posed of the Jurassic Toongi trachyte plug, 800 m 400 m in size, which intruded in the basement sedimentary and volcanic rocks. This trachyte is disseminated with zirconosilicates (eudialyte and armstrogite), natroniobite, and calcian bastnäsite. Because trachyte is enriched in zirconium (1.96 wt.% ZrO2), REEs are planned to be recovered as by-product (Verbaan et al., 2015). The Round Top deposit in western Texas, United States, is located in the southern extension of the Basin and Range region. This deposit is hosted by 36 Ma peraluminous rhyolite laccolith, 2 km 1.5 km in size, with hydrothermal alteration. The rhyolite is heavily enriched in incompatible ele- ments, with hydrothermal zircon, bastnäsite-(Ce), columbite, xenotime-(Y), etc. (Price et al., 1990; Rubin et al., 1989). 4.1.3 IOA Deposits IOA deposits, represented by Kiirunavaara in Sweden, are an important source of iron. This deposit type is characterized by the variable concentra- tions of magnetite, fluorapatite, and actinolite, and is found in northern Sweden, Missouri in the United States, Benjamin River in Canada, Chile and central Iran. The genesis of the deposits has been debatable: direct crys- tallization of immiscible Fe-rich melt that separated from a parent silicate magma (Jonsson et al., 2013; Naslund et al., 2002), or deposition of iron oxi- des from hydrothermal fluids either magmatic or crustal origin (Hildebrand, 1986; Nabatian et al., 2014; Nold et al., 2013), or mixture of the two processes (Nold et al., 2013). Whichever the origin, it has been well known that apatite associated with iron oxides of this deposit type generally contain 200–7000 ppm of REEs (Frietsch and Perdahl, 1995), some are significantly enriched in REEs,PDF Image | HANDBOOK ON THE PHYSICS AND CHEMISTRY OF RARE EARTHS
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