Halogen signatures of biotites from the Maher-Abad porphyry copper deposit, Iran: characterization of volatiles in syn- to post-magmatic hydrothermal fluids

Siahcheshm, Kamal; Calagari, Ali Asghar; Abedini, Ali; Lentz, David R.

doi:10.1080/00206814.2011.639487

Cited by 39 publications

(12 citation statements)

References 32 publications

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“…biotite generation, compositional variation, Lizhuang deposit, Mianning-Dechang REE belt, REE mineralization 1 | INTRODUCTION Understanding physicochemical conditions under which magmas and subsequent hydrothermal fluids originate and evolve is important for obtaining a clear insight into associated petrogenesis and ore-forming processes (Afshooni, Mirnejad, Esmaeily, & Haroni, 2013). In general, stable isotopes, melt or fluid inclusions, and mineral chemistry (e.g., apatite, chlorite, biotite, and epidote) are the most common approaches used to decipher the physicochemical attributes of magmatic-hydrothermal systems (Siahcheshm, Calagari, Abedini, & Lentz, 2012). Biotite, as a ubiquitous mineral phase in igneous rocks, is a complex trioctahedral mica with extensive isovalent and heterovalent substitutions and forms a solid-solution series among the three end-members of phlogopite, siderophyllite, and annite (Parsapoor, Khalili, Tepley, & Maghami, 2015;Reguir, Chakhmouradian, Halden, Malkovets, & Yang, 2009).…”

Section: Introductionmentioning

confidence: 99%

Contrasting composition of two biotite generations in the Lizhuang rare‐earth element deposit, Sichuan Province, Southwestern China

Shu

Liu

2020

Geological Journal

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Biotite is an important silicate mineral that can be used to decipher the physicochemical attributes of magmatic or hydrothermal systems. The Lizhuang rare‐earth element (REE) deposit in Sichuan Province, Southwestern China, formed from continuous magmatic‐hydrothermal processes is related to a Cenozoic carbonatite–syenite complex. Biotites are abundant in this deposit, which can be divided into two generations: generation I in intergrown with alkaline feldspar and aegirine‐augite and generation II in association with bastnäsite‐(Ce). We investigated chemical composition of the two biotite generations using electron‐microprobe(EMPA) and laser ablation–inductively coupled plasma–mass spectrometer (LA–ICP–MS) analyses to understand the development of REE mineralization. Generation I biotite has relatively high Al2O3 (10.2–12.4 wt%), TiO2 (0.49–1.85 wt%), and FeOtot (12.2–15.9 wt%), but low SiO2 (40.0–42.5 wt%) contents compared to generation II counterpart. These two generations of biotite also differ in some key trace elements. Specifically, generation I biotite has much higher concentrations of Sr (up to 234 ppm) and Ba (up to 20,796 ppm), but lower levels of Li (47.5–126 ppm) with respect to its generation II counterpart. When comparing Lizhuang biotites with those of other barren carbonatite complexes, we identified an unusual compositional trend in the generation II biotites termed as fluorphlogopite trend. This trend is marked by the continuous increase in the Mg content towards mineralization and, therefore, can serve as a diagnostic attribute in the determination of mineralized carbonatite complexes. Fluorine in biotite is an important parameter that can be used as a vector for REE exploration, because the generation II biotite presents much higher fluorine contents (2.20–4.06 wt%) than its generation I counterpart (0.87–1.59 wt%). The compositional data of the two biotite generations indicate a depletion of Fe and a progressive enrichment in Mg and F in the ore‐forming system during its evolutionary process. Physicochemical parameters estimated by biotite composition suggest that there is a trend of strongly decreasing temperature from the crystallization of generation I to generation II biotite. It is therefore concluded that temperature is a major factor favourable for REE mineralization in the Lizhuang deposit, particularly given related experimental studies. Taken together, we propose that biotite composition could serve as a proxy for REE mineralization processes and as a reliable index for REE routine exploration in a carbonatite‐related setting.

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Section: Introductionmentioning

confidence: 99%

Contrasting composition of two biotite generations in the Lizhuang rare‐earth element deposit, Sichuan Province, Southwestern China

Shu

Liu

2020

Geological Journal

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“…Amphibole and biotite thermobarometry have been used widely to estimate the emplacement pressure ( P ) and temperature ( T ) of calc-alkaline igneous rocks (Anderson and Smith, 1995; Putirka, 2008; Ridolfi et al , 2010). Similarly, the halogen (F, Cl) contents of biotite and hornblende have been used to investigate the characteristics and the evolution of the magmas and associated hydrothermal fluids (Imai, 2000; Selby and Nesbitt, 2000; Boomeri et al , 2009, 2010; Xianwu et al , 2009; Siahcheshm et al , 2012).…”

Section: Introductionmentioning

confidence: 99%

Magma chamber evolution of the Ardestan pluton, Central Iran: evidence from mineral chemistry, zircon composition and crystal size distribution

Babazadeh

Furman

Cottle

et al. 2019

MinMag

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The Oligo–Miocene Ardestan quartz diorite to tonalite is part of widespread Cenozoic magmatism within the Urumieh–Dokhtar Magmatic Assemblage of Iran. The Ardestan pluton is composed mainly of varying proportions of plagioclase feldspar (normally zoned from bytownite to andesine), amphibole (magnesio-hornblende) and biotite. Biotite exhibits a range of Al values (~2–2.8 apfu) over very restricted Fe# ratios (0.42–0.56) which are characteristic of continental arc magmatic suites. High Ti2O contents of biotite (<6.1 wt.%) suggest a magmatic origin. Ti-in-biotite geothermometery gives a mean crystallisation temperature of 730 ± 56°C, slightly higher than calculated TZr.Ti°C (716 ± 50°C) and similar to the average TZr.sat°C (735 ± 26°C). These results are consistent with the low bulk-rock SiO2 contents, which provide minimum estimates of temperature and indicate zircon crystallised from a fractionated magma. Zircons from the Ardestan pluton have high (Sm/La)N (>10) ratios suggesting a magmatic origin. T–$f_{{\rm O}_{\rm 2}}$ calculations of oxygen fugacity between –13.6 to –16.9 indicate oxidising crystallisation conditions between the Ni–NiO (NNO) and Fe2O3–Fe3O4 (HM) buffers. Tight linear trends of log (XF/XOH), log (XCl/XOH) and log (XCl/XOH) vs. XMg represent a narrow range of $f_{{\rm H}_2O}$, fHF and fHCl, clearly indicating that physico-chemical conditions were essentially constant throughout the formation of magmatic biotite. The shape of crystal size distribution curves along with the medium Al and Mg contents in amphibole and biotite, respectively, are consistent with a history of magma mixing involving injections of basic magma into the evolving felsic chamber. Calculated residence time for Ardestan plagioclase crystals of ~630 years support field evidence that these plutons were emplaced at shallow depths.

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“…Chemical composition of magmatic biotite is sensitive to chemical and physical factors associated with crystallization of the magma (Munoz, 1992;Abdel-Rahman, 1994) and also to exsolved hydrothermal fluids (Siahcheshm et al, 2012). The interlayer cations (K + , Na + , Ca 2+ , Ba + , and Cs + ) in biotite crystals could be leached out by later hydrothermal fluids and alteration processes (e.g., chloritization); the octahedral layer (Al 6+ , Mg 2+ , Fe 2+ , Fe 3+ , Li + , Ti 4+ , Mn 2+ , Zn 2+ , Cr 3+ , and V 3+ ) and tetrahedral layer cations (Si 4+ and Al 4+ ) are controlled by complex substitution mechanisms at different P-T-X conditions of a melt (magma) (Fleet, 2003).…”

Section: Introductionmentioning

confidence: 99%

Geochemical characteristics of biotite from felsic intrusive rocks around the Sisson Brook W–Mo–Cu deposit, west-central New Brunswick: An indicator of halogen and oxygen fugacity of magmatic systems

Zhang

Lentz

Thorne³

et al. 2016

Ore Geology Reviews

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The Sisson Brook W-Mo-Cu deposit was formed by hydrothermal fluids likely related to the Nashwaak Granites (muscovite-biotite granite, Group I; and biotite granite, Group II) and related dykes (biotite granitic dykes, Group III, and a feldspar-biotitequartz porphyry dyke, Group IV). Chemical data obtained using EPMA and LA-ICP-MS data of primary magmatic biotites were used to investigate magmatic processes and associated hydrothermal fluids. Trace element features of biotite in Group I two-mica granite suggest more magmatic processes along with a simple fractional crystallization. The K/Rb ratios and compatible elements (Cr, Ti, Co, V, and Ba) in biotite from Groups II, III, and IV decreases, whereas incompatible elements including Ta, Tl, Ga, Cs, Li, and Sn increase with magma fractionation. No correlation of Cu, W and Mo with K/Rb ratios is evident,  Corresponding author.

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Halogen signatures of biotites from the Maher-Abad porphyry copper deposit, Iran: characterization of volatiles in syn- to post-magmatic hydrothermal fluids

Cited by 39 publications

References 32 publications

Contrasting composition of two biotite generations in the Lizhuang rare‐earth element deposit, Sichuan Province, Southwestern China

Contrasting composition of two biotite generations in the Lizhuang rare‐earth element deposit, Sichuan Province, Southwestern China

Magma chamber evolution of the Ardestan pluton, Central Iran: evidence from mineral chemistry, zircon composition and crystal size distribution

Geochemical characteristics of biotite from felsic intrusive rocks around the Sisson Brook W–Mo–Cu deposit, west-central New Brunswick: An indicator of halogen and oxygen fugacity of magmatic systems

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