Biotite from Čierna hora Mountains granitoids (Western Carpathians, Slovakia) and estimation of water contents in granitoid melts

Bónová, Katarína; Broska, Igor; Petrík, Igor

doi:10.2478/v10096-009-0040-1

Cited by 14 publications

(5 citation statements)

References 44 publications

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“…Experiments indicate a beginning of dehydration melting in biotite-plagioclase-quartz assemblage of tonalite composition at 760 °C and 0.5 GPa, using biotite chemistry close to ~50 mol. % annite, 0.5 apfu Al and 0.3 apfu Ti in octahedral site (Singh & Johannes 1996) which is similar to the biotite composition of investigated West-Carpathian granitic rocks (Petrík 1980;Petrík & Broska 1989Bónová et al 2010).…”

Section: Titanite Age and Originsupporting

confidence: 77%

“…Textural patterns indicate titanite crystallization at the ex pense of magmatic Ti-rich magnetite, magnesian biotite and Ca-rich plagioclase which can be observed as armoured inclusions in titanite, where re-equilibration involved oxidation of the ulvöspinel (Fe 2+ 2 TiO 4 ) component in Ti-rich magnetite produced titanite and Ti-poor magnetite in the Tribeč I-type granites (Broska et al 2007). Titanite and epidote partly replace magmatic biotite and late-magmatic, Ti-poor magnetite is commonly overgrown by titanite in the Čierna Hora granitic rocks (Bónová et al 2010). The calculation of a model mineral equilibrium in the K 2 O-CaO-FeO-Al 2 O 3 -TiO 2 -SiO 2 -H 2 O-O 2 (KCFATSHO) system indicates that pure magnetite + titanite forms in granites as a product of the reaction between the early magmatic Ti-rich magnetite, Mg-rich biotite (phlogopite), and anorthite-rich plagioclase in a fluid-rich environment derived from a melt under relatively oxidizing conditions (Broska et al 2007;Broska & Petrík 2011).…”

Section: Titanite Age and Originmentioning

confidence: 99%

“…The above-mentioned authors suggest a late-magmatic origin of titanite; assuming equilibrium among biotite, K-feldspar and magnetite, where the intersection of the calculated biotite stability curves with the curve of minimum water content in the haplogranite system (after Johannes & Holtz 1996) gives 4.8 wt.% H 2 O at 744 °C and 0.4 GPa for the titanite-bearing tonalite of the Čierna Hora Mts. (Bónová et al 2010). Application of the Fe-Ti oxide geothermometry (Sauerzapf et al 2008;Ghiorso & Evans 2008) show ~630 to 780 °C interval for the equilibrium of magnetite-ilmenite pair for the titanitebearing granitic rocks (Tribeč, Čierna Hora; Broska & Petrík 2011).…”

Section: Titanite Age and Originmentioning

confidence: 99%

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Titanite composition and SHRIMP U–Pb dating as indicators of post-magmatic tectono-thermal activity: Variscan I-type tonalites to granodiorites, the Western Carpathians

Uher

Broska

Krzemińska

et al. 2019

Geologica Carpathica

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Titanite belongs to the common accessory minerals in Variscan (~360–350 Ma) metaluminous to slightly peraluminous tonalites to granodiorites of I-type affinity in the Tatric and Veporic Units, the Western Carpathians, Slovakia. It forms brown tabular prismatic-dipyramidal crystals (~0.5 to 10 mm in size) in association with quartz, plagioclase, and biotite. Titanite crystals commonly shows oscillatory, sector and convolute irregular zonal textures, reflecting mainly variations in Ca and Ti versus Al (1–2 wt. % Al2O3, 0.04–0.08 Al apfu), Fe (0.6–1.6 wt. % Fe2O3, 0.02–0.04 Fe apfu), REE (La to Lu + Y; ≤4.8 wt. % REE2O3, ≤ 0.06 REE apfu), and Nb (up to 0.5 wt. % Nb2O5, ≤0.01 Nb apfu). Fluorine content is up to 0.5 wt. % (0.06 F apfu). The compositional variations indicate the following principal substitutions in titanite: REE3+ + Fe3+ = Ca2+ + Ti4+, 2REE3+ + Fe2+ = 2Ca2+ + Ti4+, and (Al, Fe)3+ + (OH, F)− = Ti4+ + O2−. The U–Pb SHRIMP dating of titanite reveal their Variscan ages in an interval of 351.0 ± 6.5 to 337.9 ± 6.1 Ma (Tournaisian to Visean); titanite U–Pb ages are thus ~5 to 19 Ma younger than the primary magmatic zircon of the host rocks. The Zr-in-titanite thermometry indicates a relatively high temperature range of titanite precipitation (~650–750 °C), calculated for assumed pressures of 0.2 to 0.4 GPa and a(TiO2) = 0.6–1.0. Consequently, the textural, geochronological and compositional data indicate relatively high-temperature, most probably early post-magmatic (subsolidus) precipitation of titanite. Such titanite origin could be connected with a subsequent Variscan tectono-thermal event (~340 ± 10 Ma), probably related with younger small granite intrusions and/or increased fluid activity. Moreover, some titanite crystals show partial alteration and formation of secondary titanite (depleted in Fe and REE) + allanite-(Ce) veinlets (Sihla tonalite, Veporic Unit), which probably reflects younger Alpine (Cretaceous) tectono-thermal overprint of the Variscan basement of the Western Carpathians.

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Section: Titanite Age and Originsupporting

confidence: 77%

Section: Titanite Age and Originmentioning

confidence: 99%

Section: Titanite Age and Originmentioning

confidence: 99%

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Titanite composition and SHRIMP U–Pb dating as indicators of post-magmatic tectono-thermal activity: Variscan I-type tonalites to granodiorites, the Western Carpathians

Uher

Broska

Krzemińska

et al. 2019

Geologica Carpathica

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“…8d, e), biotite of older granites falls within the calc-alkaline magma (C) field, the biotite of monzo-syenogranites falls close to the boundary between the (C) field and the (A) field, while biotite from alkali feldspar granites falls mostly within the (A) type. Biotite is used as an appropriate pointer of the oxidation-reduction state in a melt (Bónová et al 2010). Ti content of biotite reflects the temperature of the crystallization and the oxygen fugacity (fO2) of biotite (Henry et al 2005) where low Ti content relates to the low temperature of crystallization and the low oxygen fugacity (Henry et al 2005).…”

Section: Biotitementioning

confidence: 99%

Petrogenesis and tectonic evolution of syn-to late granitoid rocks from Um Taghir NE Egyptian Nubian Shield Desert of Egypt: subduction to post-collision magmatism

2021

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The Pan-African rocks of Um Taghir area encompass metavolcanics, synorogenic granites, Dokhan Volcanics, younger gabbros, post-collision granites, and they are cross-cut by dikes. The current granitoid rocks comprise older weakly deformed tonalite-granodiorites intruded by late tectonic undeformed granite including monzo-syenogranites and alkali feldspar granites. The weakly deformed tonalite-granodiorite is characterized by a restricted range of SiO 2 (65.78-69.43%) with reasonable enrichment in the LILE (Ba, Rb, and K 2 O), small negative Nb anomaly, and low Rb/Sr ratio which is the distinguishing of most of the synorogenic and subducted I-type granitoids in the Egyptian Nubian Shield (ANS). It is supposed that tonalitegranodiorite was formed by fractional crystallization of the Abu Furad metagabbro-diorite which is designated by their more or less lined trend on variation diagrams and their elements contents are ascribed to fractional crystallization of ferromagnesian minerals and feldspars. The monzo-syenogranites and alkali feldspar granites show SiO 2 ranges of 71.86-75.88% and 73.74-78.62%, respectively, formed through limited melting of the tonalite-granodiorite crust by rising of asthenosphere fluids with fractional crystallization of feldspars and amphibole. They are enhanced in LILE and Nb, formed in shallower depth, and categorized as A-type post-collision granite. On the basis of the geodynamic model, granite phases are consistent with the prevalent change from compressional toward post-collisional setting in the North Eastern Desert (NED). The monzosyenogranites were partially transformed into episyenitized rocks (episyenitized monzo-syenogranites) via desilicification, displaying SiO 2 contents of 65.44-66.36%, where gains and losses in mass are generally minimal (7.52 and 8.98%, respectively) and most other elements are close to the isocon line. Both older-and younger-granite types are in harmony with their formation by fractional crystallization process and are dependable with the dominant transitional tectonic setting in NED.

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“…Biotite composition can be used to determine the tectonic environment of host rocks (Abdel-Rahman, 1994;Shabani et al, 2003;Machev et al, 2004;Bónová et al, 2010 and Pathak, 2010; Zhang et al, 2016). In this study we use the biotite tectonomagmatic characterization of Abdel-Rahman (1994) and Shabani et al (2003).…”

Section: Tectonomagmatic Evolution Of Guéra Massif Granitesmentioning

confidence: 99%

An Assessment of the Magmatic Conditions of Late Neoproterozoic Collisional and Post-collisional Granites From the Guéra Massif, South-Central Chad

Pham

Shellnutt²,

Yeh

et al. 2020

Front. Earth Sci.

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The Guéra Massif, in South-Central Chad hosts granitic rocks that were emplaced during distinct intervals (595-590; ∼570; ∼560 Ma) of the Late Ediacaran Central African Orogenic Belt. To the northwest of the Guéra Massif, younger post-collisional granites (554-545 Ma) are found near Lake Fitri. The older (≥590 Ma) rocks have geochemical characteristics of collisional granites whereas the younger (≤570 Ma) rocks are similar to post-collisional granites. Biotite and amphibole were analyzed to constrain the magmatic conditions of the granites. The biotite from the collisional granites tends to have higher Al and Ti and lower Fe# (Fe# average ≈ 0.67) than the post-collisional granites (Fe# average ≈ 0.88). The average crystallization temperatures range from 696 ± 37 to 612 ± 8 • C, with the average pressure of crystallization from 0.25 ± 0.09 to 0.13 ± 0.02 GPa, and redox conditions between the nickel-nickel oxide (NNO) and quartz-fayalite-magnetite (QFM) buffers. The biotite crystallization temperatures of the post-collisional rocks are generally lower than the collisional rocks (570 Ma = 630 ± 26 to 619 ± 30 • C, 560 Ma = 626 ± 20 to 607 ± 4 • C, 550 Ma = 639 ± 18 to 612 ± 13 • C), but the crystallization pressures are similar (0.27 ± 0.05 to 0.14 ± 0.04 GPa). The redox conditions transition from the QFM buffer to the wüstite-magnetite (WM) buffer. In contrast, the biotite from the Lake Fitri post-collisional granites crystallized at higher pressure (0.39 ± 0.08 to 0.35 ± 0.03 GPa) but similar redox conditions. The amphiboles in the younger (∼590 Ma) collisional granites and the post-collisional granites yielded crystallization pressure estimates that are generally higher (∼0.6 to 0.1 GPa) than the biotite estimates but there is overlap. The difference in pressure may be due to the timing of crystallization and/or crystal redistribution. Overall, there appears to be a secular change from high to low temperature and pressure whereas the redox conditions appear to be spatially related. The biotite crystallization pressure of the Lake Fitri granites suggests they were likely emplaced into a different domain/terrane of the Saharan Metacraton than the Guéra Massif.

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Biotite from Čierna hora Mountains granitoids (Western Carpathians, Slovakia) and estimation of water contents in granitoid melts

Cited by 14 publications

References 44 publications

Titanite composition and SHRIMP U–Pb dating as indicators of post-magmatic tectono-thermal activity: Variscan I-type tonalites to granodiorites, the Western Carpathians

Titanite composition and SHRIMP U–Pb dating as indicators of post-magmatic tectono-thermal activity: Variscan I-type tonalites to granodiorites, the Western Carpathians

Petrogenesis and tectonic evolution of syn-to late granitoid rocks from Um Taghir NE Egyptian Nubian Shield Desert of Egypt: subduction to post-collision magmatism

An Assessment of the Magmatic Conditions of Late Neoproterozoic Collisional and Post-collisional Granites From the Guéra Massif, South-Central Chad

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