The characteristics and origin of the Hoidas Lake REE Deposit
01 Jan 2010-
About: The article was published on 2010-01-01 and is currently open access. It has received 11 citations till now. The article focuses on the topics: Allanite.
Citations
More filters
TL;DR: In this paper, the authors proposed that the ideal rare earth element (REE) development targets would be located in a politically stable jurisdiction with a pro-mining disposition such as Canada and Australia.
Abstract: China started to produce rare earth elements (REEs) in the 1980s, and since the mid-1990s, it has become the dominant producer. Rare earth element export quotas first introduced by the Chinese government in the early 2000s were severely reduced in 2010 and 2011. This led to strong government-created disparity between prices within China and the rest of the world. Industrialized countries identified several REEs as strategic metals. Because of rapid price increases of REE outside of China, we have witnessed a world-scale REE exploration rush. The REE resources are concentrated in carbonatite-related deposits, peralkaline igneous rocks, pegmatites, monazite ± apatite veins, ion adsorption clays, placers, and some deep ocean sediments. REE could also be derived as a by-product of phosphate fertilizer production, U processing, mining of Ti-Zr-bearing placers, and exploitation of Olympic Dam subtype iron oxide copper gold (IOCG) deposits. Currently, REEs are produced mostly from carbonatite-related deposits, but ion adsorption clay deposits are an important source of heavy REE (HREE). Small quantities of REE are derived from placer deposits and one peralkaline intrusion-related deposit. The ideal REE development targets would be located in a politically stable jurisdiction with a pro-mining disposition such as Canada and Australia. REE grade, HREE/light REE (LREE) ratio of the mineralization, tonnage, mineralogy, and permissive metallurgy are some of the key technical factors that could be used to screen potential development projects. As REEs are considered strategic metals from economic, national security, and environmental points of view, technical and economic parameters alone are unlikely to be used in REE project development decision-making. Recycling of REE is in its infancy and unless legislated, in the short term, it is not expected to contribute significantly to the supply of REE.
74 citations
Cites background from "The characteristics and origin of t..."
...5c) located in South Africa (Andreoli et al. 1994) and Hoidas-type deposits in Saskatchewan, Canada (Halpin 2010)....
[...]
...Several LREE-enriched veins, lenses, or dikes are known in Saskatchewan, Canada....
[...]
...Monazite, bastnaesite, and chevkinite are minor constituents (Halpin 2010)....
[...]
TL;DR: In this paper, the authors conducted geochemical and mineralogical investigations of the rare earth and yttrium (REY)-rich mud from the Minami-Torishima area in the Pacific in order to clarify the concentration of REY and their host-phase in the mud.
Abstract: We have conducted geochemical and mineralogical investigations of the rare earth and yttrium (REY)-rich mud from the Minami-Torishima area in the Pacific in order to clarify the concentration of REY and their host-phase in the mud. X-ray diffraction analysis shows that the mud is mainly composed of phillipsite, fluorapatite, quartz, albite, illite and montmorillonite. Whole-rock CaO, P2O5 and total REY contents of the mud are positively correlated. Relative abundance of apatite is also positively correlated to P2O5 and total REY contents. These correlations suggest that apatite is the main host of the P2O5 and REY in the mud. We make in situ compositional analyses of constituent minerals in the REY mud. The results show that the apatite is abundant in REY (9300–32,000 ppm) and is characterized by a negative Ce anomaly and enrichment in heavy rare-earth elements. This abundance and composition of REY of the mud is similar those of fish debris apatites. In contrast, phillipsite is less abundant in REY (60–170 ppm). Therefore we conclude that the main REY host phase of the mud is apatite.
73 citations
Cites background from "The characteristics and origin of t..."
...In contrast to the apatite of REY mud, negative Ce-anomalies are found rarely in the high-REE apatites from these deposits (Frietsch & Perdahl, 1995; Stalder & Rozendaal, 2004; Halpin, 2010; Mokhtari et al., 2013)....
[...]
...7c) from iron oxide apatite (IOA)-type ore deposits of Singhbum in India, Great Bear Lake and Iron Spring in the USA (Frietsch & Perdahl, 1995), Posht-e-Badam Block in Iran (Mokhtari et al., 2013) and hydrothermal apatites of Gamsberg in South Africa (Stalder & Rozendaal, 2004) and Hoidas Lake in Canada (Halpin, 2010)....
[...]
..., 2013) and hydrothermal apatites of Gamsberg in South Africa (Stalder & Rozendaal, 2004) and Hoidas Lake in Canada (Halpin, 2010)....
[...]
...…(IOA)-type ore deposits of Singhbum in India, Great Bear Lake and Iron Spring in the USA (Frietsch & Perdahl, 1995), Posht-e-Badam Block in Iran (Mokhtari et al., 2013) and hydrothermal apatites of Gamsberg in South Africa (Stalder & Rozendaal, 2004) and Hoidas Lake in Canada (Halpin, 2010)....
[...]
TL;DR: In this article, the potential sources of rare earth elements (REEs) are reviewed, including ion-adsorption types and apatite deposits, which are regarded as the most critical group of elements for the future green technologies.
Abstract: Recent increase of the demand for rare earth elements (REEs), especially dysprosium and terbium used in the permanent magnet industry is modifying a concept of the REE mineralogy and resources. This is amplified by the REE supply restrictions outside of China. Exploration has been extended worldwide to secure the supply of REEs, especially the heavy ones. In recent years, various attempts are made to produce heavy rare earth elements (HREEs) from unconventional sources, such as peralkaline igneous rocks, which have not been regarded as a REE source. Therefore, this paper reviews the potential sources of REEs, especially HREEs (ion-adsorption types and apatite deposits), which are regarded as the most critical group of elements for the future green technologies.
67 citations
01 Jan 2016
TL;DR: This article gave an overview of the major and minor ore minerals of the rare earths, and of the related major ore deposits, and indicated that the apparent dominance of China is economically and politically powered.
Abstract: This chapter gives an overview of the major and minor ore minerals of the rare earths, and of the related major ore deposits. As most of the rare earths are mined in China, the impression may arise that ore deposits of these metals occur in few other places on Earth. However, nothing is less true. The extensive overview of the ore deposits of the rare earths in this chapter is especially meant to indicate that deposits occur in quite a variety of countries, and that the apparent dominance of China is economically (and politically) powered.
21 citations
TL;DR: The Hoidas Lake rare earth element (REE) deposit, located in northern Saskatchewan, Canada, is a structurally controlled vein-type LREE deposit with allanite-(Ce) and fluorapatite as the main REE carriers.
Abstract: The Hoidas Lake rare earth element (REE) deposit, located in northern Saskatchewan, Canada, is a structurally controlled vein-type LREE deposit with allanite-(Ce) and fluorapatite as the main REE carriers. The mineralized veins cut Archean and Paleoproterozoic orthogneisses and supracrustal rocks of the southern Rae Subprovince. The paragenesis includes hyalophane-bearing pegmatite dikes, REE-mineralized allanite-, diopside-, hornblende-, hyalophane-, and titanite-bearing veins, and later breccia veins that contain several stages of apatite. The mineralized veins record hydrothermal alteration with nucleation of monazite and REE-carbonate inclusions in apatite and allanite, respectively. Barren quartz-, carbonate-, and hematite-rich veins represent the final stage of hydrothermal activity. Samples from the hyalophane-bearing pegmatites, apatite breccia veins, and quartz-carbonate veins, used for fluid inclusion petrography and microthermometry, indicate four distinct fluid inclusion assemblages (FIAs): (1) carbonic inclusions showing LCO2 (liquid CO2) + VCO2 (CO2 vapor) phase composition with 20–40 vol.% VCO2 at 0 °C; (2) aqueous inclusions showing L (liquid H2O) + V (H2O vapor) phase composition with 90–100 vol.% V at 20 °C; (3) aqueous inclusions showing L + V + H (halite) phase composition with 15 vol.% V at 20 °C; and (4) aqueous L + V inclusions with 15–20 vol.% V at 20 °C. Type 1 inclusions homogenize to liquid CO2 with Th(CO2) from 3.3 to 30.5 °C. Type 2 V-rich inclusions have high salinities and contain salts other than NaCl. Type 3 L-V-H inclusions have different homogenization behavior in quartz of the hyalophane-bearing pegmatites (L+V+H → L+V → L) compared to quartz-carbonate veins (L+V+H → L+H → L), and Th (total homogenization) values range from 180 to 315 °C with salinities of 30–40 wt.% eq. NaCl. In type 4 inclusions Th ranges from 90 to 290 °C, but for specific samples and FIAs (fluid inclusion assemblages) there is a more limited spread (from 5 to 25 °C). Salinities range from 8 to 24 wt.% eq. NaCl, and the inclusions have variable Na/(Na + Ca). Evaporate mound analysis shows average normalized (to 100%) cation contents of 48% Na, 24% Ca, 6% K, 5% Ba, 4% Mn, 2% Fe, 2% Mg, and 9% Sr for quartz-hosted inclusions in quartz-carbonate veins, and 61% Na, 32% Ca, and 7% K for quartz-hosted inclusions in hyalophane-bearing pegmatite dikes. The thermometric and chemical data suggest that evolution of the Hoidas Lake mineralization involved two fluid types with early entrapment of a carbonic fluid followed by introduction of a mixed Na-Ca-K-(Ba-Mn-Mg-Fe-Sr) aqueous fluid with variable salinities that was responsible for the late alteration of the mineralized veins. Furthermore, the inclusion data provide constraints on entrapment temperature (<310 °C) and also indicate that the pressure was transient (0.5 to 2 kbars) based on the homogenization temperature data for the carbonic (type 1) and aqueous L-V-H (type 3) inclusions.
17 citations
References
More filters
01 Jan 1989
TL;DR: In this article, trace-element data for mid-ocean ridge basalts and ocean island basalts are used to formulate chemical systematics for oceanic basalts, interpreted in terms of partial-melting conditions, variations in residual mineralogy, involvement of subducted sediment, recycling of oceanic lithosphere and processes within the low velocity zone.
Abstract: Summary Trace-element data for mid-ocean ridge basalts (MORBs) and ocean island basalts (OIB) are used to formulate chemical systematics for oceanic basalts. The data suggest that the order of trace-element incompatibility in oceanic basalts is Cs ≈ Rb ≈ (≈ Tl) ≈ Ba(≈ W) > Th > U ≈ Nb = Ta ≈ K > La > Ce ≈ Pb > Pr (≈ Mo) ≈ Sr > P ≈ Nd (> F) > Zr = Hf ≈ Sm > Eu ≈ Sn (≈ Sb) ≈ Ti > Dy ≈ (Li) > Ho = Y > Yb. This rule works in general and suggests that the overall fractionation processes operating during magma generation and evolution are relatively simple, involving no significant change in the environment of formation for MORBs and OIBs. In detail, minor differences in element ratios correlate with the isotopic characteristics of different types of OIB components (HIMU, EM, MORB). These systematics are interpreted in terms of partial-melting conditions, variations in residual mineralogy, involvement of subducted sediment, recycling of oceanic lithosphere and processes within the low velocity zone. Niobium data indicate that the mantle sources of MORB and OIB are not exact complementary reservoirs to the continental crust. Subduction of oceanic crust or separation of refractory eclogite material from the former oceanic crust into the lower mantle appears to be required. The negative europium anomalies observed in some EM-type OIBs and the systematics of their key element ratios suggest the addition of a small amount (⩽1% or less) of subducted sediment to their mantle sources. However, a general lack of a crustal signature in OIBs indicates that sediment recycling has not been an important process in the convecting mantle, at least not in more recent times (⩽2 Ga). Upward migration of silica-undersaturated melts from the low velocity zone can generate an enriched reservoir in the continental and oceanic lithospheric mantle. We propose that the HIMU type (eg St Helena) OIB component can be generated in this way. This enriched mantle can be re-introduced into the convective mantle by thermal erosion of the continental lithosphere and by the recycling of the enriched oceanic lithosphere back into the mantle.
19,221 citations
TL;DR: In this article, a data bank containing over 600 high quality trace element analyses of granites from known settings was used to demonstrate using ORG-normalized geochemical patterns and element-SiO2 plots that most of these granite groups exhibit distinctive trace element characteristics.
Abstract: Granites may be subdivided according to their intrusive settings into four main groups—ocean ridge granites (ORG), volcanic arc granites (VAG), within plate granites (WPG) and collision granites (COLG)—and the granites within each group may be further subdivided according to their precise settings and petrological characteristics. Using a data bank containing over 600 high quality trace element analyses of granites from known settings, it can be demonstrated using ORG-normalized geochemical patterns and element-SiO2 plots that most of these granite groups exhibit distinctive trace element characteristics. Discrimination of ORG, VAG, WPG and syn-COLG is most effective in Rb-Y-Nb and Rb-Yb-Ta space, particularly on projections of Y-Nb, Yb-Ta, Rb-(Y + Nb) and Rb—(Yb + Ta). Discrimination boundaries, though drawn empirically, can be shown by geochemical modelling to have a theoretical basis in the different petrogenetic histories of the various granite groups. Post-collision granites present the main problem of tectonic classification, since their characteristics depend on the thickness and composition of the lithosphere involved in the collision event and on the precise timing and location of magmatism. Provided they are coupled with a consideration of geological constraints, however, studies of trace element compositions in granites can clearly help in theelucidation of post-Archaean tectonic settings.
7,144 citations
Book•
01 Jan 1966
TL;DR: In this article, the authors define di-and ring silicates: olivine group humite group zircon sphene (titanite) garnet group, vesuvianite sillimanite, mullite, andalusite, kyanite topaz staurolite, chloritoid epidote group lawsonite, pumpellyite melilite group beryl, cordierite, tourmaline axinite.
Abstract: PART 1 ORTHO: Di- and ring silicates: olivine group humite group zircon sphene (titanite) garnet group, vesuvianite sillimanite, mullite, andalusite, kyanite topaz staurolite, chloritoid epidote group lawsonite, pumpellyite melilite group beryl, cordierite, tourmaline axinite. PART 2 CHAIN SILICATES: pyroxene group wollastonite sapphirine amphibole group. PART 3 SHEET SILICATES: mica group stilpnomelane pyrophyllite chlorite serpentine clay minerals apophyllite prehnite. PART 4 FRAMEWORK SILICATES: feldspar group silica minerals nepheline group petalite, leucite sodalite group cancrinite - vishnevite, scapolite analcite, zeolite group. PART 5 NON-SILICATES: oxides hydroxides sulphides sulphates carbonates phosphates halides
5,387 citations