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Systems Based on AlP
Published in Vasyl Tomashyk, Multinary Alloys Based on III-V Semiconductors, 2018
The (Sm,Nd)Al3(PO4)2(OH)6 multinary phase [mineral florencite-(Sm)], which crystallizes in the trigonal structure with the lattice parameters a = 697.2 ± 0.4 and c = 1,618.2 ± 0.7 pm and the calculated and experimental densities of 3.666 and 3.753 (for two mineral compositions) and 3.60 ± 0.01 g cm−3, respectively, is formed in the Al–H–Nd–Sm–O–P system (Repina et al. 2011; Belakovskiy et al. 2012).
Occurrence, geochemistry and provenance of REE-bearing minerals in marine placers on the West Coast of the South Island, New Zealand
Published in New Zealand Journal of Geology and Geophysics, 2021
Stephanie L. Tay, James M. Scott, Marshall C. Palmer, Malcolm R. Reid, Claudine H. Stirling
The Karamea Batholith is the largest of the Western Province batholiths. Contiguous plutons within the batholith belong to Karamea, Ridge, Foulwind, Tobin, Separation Point, Rahu suites, with the S-type Karamea Suite dominant (Tulloch 1988; Muir et al. 1995; Waight et al. 1997; Tulloch et al. 2009; Turnbull et al. 2016). The Karamea Batholith consists of mica- and quartz-rich granitoids that have accessory REE-bearing minerals including zircon, epidote, allanite, titanite, apatite, monazite and xenotime (Tulloch 1983; Minehan 1989; Muir et al. 1996; Christie et al. 2010). Averaging 10 km wide and 120 km long, the Early Cretaceous Separation Point Batholith is the most eastern batholith and is found within the Takaka terrane. Accessory REE-bearing minerals in this batholith include titanite, epidote, zircon, monazite and apatite (Tulloch 1983; Muir et al. 1995). The Rahu Suite is restricted to Victoria Range and Buller Valley area, Paparoa Range and along the Hohonu Range (Brathwaite and Pirajno 1993; Waight et al. 1997). Rahu Suite rocks contain allanite, monazite, titanite, epidote, apatite, zircon and garnet, as well as rare tourmaline (Graham and White 1990; Waight et al. 1997). Morgenstern et al. (2018) report that the Cretaceous French Creek Granite (Waight et al. 1998b) contains bastnäsite group minerals as well as allanite, zircon, fergusonite, (fluor)apatite, monazite, xenotime, florencite and perrierite–loparite. French Creek Granite has been the focus of REE exploration in the past.
Tectonothermal events in the Olympic IOCG Province constrained by apatite and REE-phosphate geochronology
Published in Australian Journal of Earth Sciences, 2018
A. R. Cherry, V. S. Kamenetsky, J. McPhie, J. M. Thompson, K. Ehrig, S. Meffre, M. B. Kamenetsky, S. Krneta
The apatite grains contain zones that are distinguished by differing BSE brightness (Figure 4) that also correspond to differences in trace-element concentration. Bright zones have elevated concentrations of trace elements (e.g. REE, Y, U, Th, Na, Si) relative to the dark zones (Figure 5; Supplementary Papers, Table S2). More than two shades of different BSE brightness are present in some samples (Figure 4c). The dark zones are commonly distributed as a fine network through the apatite grains (Figure 4d), as well as patches throughout or projecting inwards from the rims of apatite grains (Figure 4e). In contrast, the cores of some apatite grains in one sample (OD743) almost entirely comprise dark apatite surrounded by a rim of mostly bright apatite (Figure 4f). The dark zones contain abundant fine inclusions (<50 µm, e.g. monazite, xenotime, iron oxide, barite, florencite, chalcopyrite, pyrite) (Figure 6) and the darkest BSE zone is associated with the majority of the inclusions. Some dark zones have abundant fine pores (<10 µm) apparent under SEM. In contrast, the bright areas contain little-to-no inclusions and are texturally homogeneous. The dark zones of samples OD742 and OD743 appear to contain the highest abundance of inclusions whereas dark zones in OD306 have the lowest abundance of inclusions (e.g. Figure 4a–d)