Rare earths and other trace elements in minerals from skarn assemblages, Hillside iron oxide–copper–gold deposit, Yorke Peninsula, South Australia

Ismail, Rohani; Ciobanu, Cristiana L.; Cook, Nigel J.; Teale, Graham S.; Giles, David; Mumm, Andreas Schmidt; Wade, Benjamin P.

doi:10.1016/j.lithos.2013.07.023

Cited by 103 publications

(64 citation statements)

References 29 publications

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“…Similarly, the LREE-enriched signatures characteristic for DM and DS apatite (REY-, S-and Cl-rich cores and REY-, S-rich cores, respectively) are almost identical to apatite REY-signatures measured in apatite from similar magnetite-apatite ± pyrite assemblages elsewhere within the Olympic Cu-Au Province [1,10,47], as well as globally [11,14]. Such an observation reinforces the interpretation of [10] that although not unique to early high-temperature apatite associated with magnetite ± pyrite assemblages in IOCG systems, LREE-enriched apatite signatures are certainly characteristic for such apatite.…”

Section: Rey-signatures In Apatite and The Transition From Magmatic Tsupporting

confidence: 53%

“…The concentrations of trace elements within hydrothermal minerals and their variation can provide valuable information on fluid parameters and the conditions of ore deposition if the studied assemblages are well constrained with respect to their paragenetic position [1]. Rare earth elements and yttrium (REY) have proven particularly instructive, as they display a systematic decrease in atomic radius with an increased atomic number which causes a divergence in their geochemical behaviour [2].…”

Section: Introductionmentioning

confidence: 99%

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Rare Earth Element Behaviour in Apatite from the Olympic Dam Cu–U–Au–Ag Deposit, South Australia

et al. 2017

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Abstract:Apatite is a common magmatic accessory in the intrusive rocks hosting the giant~1590 Ma Olympic Dam (OD) iron-oxide copper gold (IOCG) ore system, South Australia. Moreover, hydrothermal apatite is a locally abundant mineral throughout the altered and mineralized rocks within and enclosing the deposit. Based on compositional data for zoned apatite, we evaluate whether changes in the morphology and the rare earth element and Y (REY) chemistry of apatite can be used to constrain the fluid evolution from early to late hydrothermal stages at OD. The~1.6 Ga Roxby Downs granite (RDG), host to the OD deposit, contains apatite as a magmatic accessory, locally in the high concentrations associated with mafic enclaves. Magmatic apatite commonly contains REY-poor cores and REY-enriched margins. The cores display a light rare earth element (LREE)-enriched chondrite-normalized fractionation pattern with a strong negative Eu anomaly. In contrast, later hydrothermal apatite, confined to samples where magmatic apatite has been obliterated due to advanced hematite-sericite alteration, displays a conspicuous, convex, middle rare earth element (MREE)-enriched pattern with a weak negative Eu anomaly. Such grains contain abundant inclusions of florencite and sericite. Within high-grade bornite ores from the deposit, apatite displays an extremely highly MREE-enriched chondrite-normalized fractionation trend with a positive Eu anomaly. Concentrations of U and Th in apatite mimic the behaviour of ∑REY and are richest in magmatic apatite hosted by RDG and the hydrothermal rims surrounding them. The shift from characteristic LREE-enriched magmatic and early hydrothermal apatite to later hydrothermal apatite displaying marked MREE-enriched trends (with lower U, Th, Pb and ∑REY concentrations) reflects the magmatic to hydrothermal transition. Additionally, the strong positive Eu anomaly in the MREE-enriched trends of apatite in high-grade bornite ores are attributable to alkaline fluid conditions.

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Section: Rey-signatures In Apatite and The Transition From Magmatic Tsupporting

confidence: 53%

Section: Introductionmentioning

confidence: 99%

Rare Earth Element Behaviour in Apatite from the Olympic Dam Cu–U–Au–Ag Deposit, South Australia

et al. 2017

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“…Prior investigation of as large a volume of representative samples as possible by optical and scanning electron microscopy is strongly recommended prior to LA-ICP-MS microanalysis, to facilitate an adequate appreciation of multiple generations and overprinting (if present), features that might indicate compositional zoning, or evidence for mineral-mineral or mineral-fluid reactions. Single mineral grains may preserve compositionally or texturally-distinct domains that can be interpreted as multiple generations; examples include growth-zoned pyrite from metamorphosed ores that preserve pre-metamorphic grain cores (e.g., [52]), or skarn garnet recoding prograde and superposed retrograde growth cycles [53].…”

Section: Mineral Texturesmentioning

confidence: 99%

Trace Element Analysis of Minerals in Magmatic-Hydrothermal Ores by Laser Ablation Inductively-Coupled Plasma Mass Spectrometry: Approaches and Opportunities

et al. 2016

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Laser ablation inductively-coupled plasma mass spectrometry (LA-ICP-MS) has rapidly established itself as the method of choice for generation of multi-element datasets for specific minerals, with broad applications in Earth science. Variation in absolute concentrations of different trace elements within common, widely distributed phases, such as pyrite, iron-oxides (magnetite and hematite), and key accessory minerals, such as apatite and titanite, can be particularly valuable for understanding processes of ore formation, and when trace element distributions vary systematically within a mineral system, for a vector approach in mineral exploration. LA-ICP-MS trace element data can assist in element deportment and geometallurgical studies, providing proof of which minerals host key elements of economic relevance, or elements that are deleterious to various metallurgical processes. This contribution reviews recent advances in LA-ICP-MS methodology, reference standards, the application of the method to new mineral matrices, outstanding analytical uncertainties that impact on the quality and usefulness of trace element data, and future applications of the technique. We illustrate how data interpretation is highly dependent on an adequate understanding of prevailing mineral textures, geological history, and in some cases, crystal structure.

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“…Unlike the hematite-sericite associated mineralization in altered RDG, such apatite displays a positive Eu-anomaly (high-grade bornite ore hosted apatite, Figure 2, Table 1; [17]). Such a signature is very unusual for IOCG apatite in the Olympic Province (e.g., [15][16][17][18]), however it has also been observed from the Acropolis deposit [16], where it is shown to be the result of crystallization from late-stage neutral to alkaline fluids based on mineral stabilities and Eu-speciation. [42][43][44] has provided insights into the formation of these deposits by defining the temperatures and salinities of fluids.…”

Section: Ree Trends In Fluorapatite From the Olympic Dam Depositmentioning

confidence: 96%

Numerical Modeling of REE Fractionation Patterns in Fluorapatite from the Olympic Dam Deposit (South Australia)

et al. 2018

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Trace element signatures in apatite are used to study hydrothermal processes due to the ability of this mineral to chemically record and preserve the impact of individual hydrothermal events. Interpretation of rare earth element (REE)-signatures in hydrothermal apatite can be complex due to not only evolving f O 2 , f S 2 and fluid composition, but also to variety of different REE-complexes (Cl-, F-, P-, SO 4, CO 3 , oxide, OH − etc.) in hydrothermal fluid, and the significant differences in solubility and stability that these complexes exhibit. This contribution applies numerical modeling to evolving REE-signatures in apatite within the Olympic Dam iron-oxide-copper-gold deposit, South Australia with the aim of constraining fluid evolution. The REE-signatures of three unique types of apatite from hydrothermal assemblages that crystallized under partially constrained conditions have been numerically modeled, and the partitioning coefficients between apatite and fluid calculated in each case. Results of these calculations replicate the measured data well and show a transition from early light rare earth element (LREE)-to later middle rare earth element (MREE)-enriched apatite, which can be achieved by an evolution in the proportions of different REE-complexes. Modeling also efficiently explains the switch from REE-signatures with negative to positive Eu-anomalies. REE transport in hydrothermal fluids at Olympic Dam is attributed to REE-chloride complexes, thus explaining both the LREE-enriched character of the deposit and the relatively LREE-depleted nature of later generations of apatite. REE deposition may, however, have been induced by a weakening of REE-Cl activity and subsequent REE complexation with fluoride species. The conspicuous positive Eu-anomalies displayed by later apatite with are attributed to crystallization from high pH fluids characterized by the presence of Eu 3+ species.

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Rare earths and other trace elements in minerals from skarn assemblages, Hillside iron oxide–copper–gold deposit, Yorke Peninsula, South Australia

Cited by 103 publications

References 29 publications

Rare Earth Element Behaviour in Apatite from the Olympic Dam Cu–U–Au–Ag Deposit, South Australia

Rare Earth Element Behaviour in Apatite from the Olympic Dam Cu–U–Au–Ag Deposit, South Australia

Trace Element Analysis of Minerals in Magmatic-Hydrothermal Ores by Laser Ablation Inductively-Coupled Plasma Mass Spectrometry: Approaches and Opportunities

Numerical Modeling of REE Fractionation Patterns in Fluorapatite from the Olympic Dam Deposit (South Australia)

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