Peri-Amazonian, Avalonian-type and Ganderian-type terranes in the South Carpathians, Romania: The Danubian domain basement

Balintoni, Ioan; Balica, Constantin; Ducea, Mihai N.; Stremtan, Ciprian

doi:10.1016/j.gr.2010.10.002

Cited by 35 publications

(27 citation statements)

References 31 publications

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“…If we consider the most concordant age sets (between 305.4 and 318.6 and between 292.1 and 305.6 Ma) we get a weighted mean age of 301.5±6 Ma (Fig.5). Liégeois et al (1996), and Balintoni et al (2011) dated the Tismana, Şuşiţa, Novaci, and Olteţ plutons and their results bracketed the ages around 600 Ma. These plutons cross-cut a dense swarm of migmatic dykes characterized by black K-feldspar grains (Berza and Seghedi, 1983).…”

Section: Variscan Granites In the Danubian Domain Of Romanian South Cmentioning

confidence: 62%

“…Peri-Amazonian basement of the Alpine Danubian Domain of South Carpathians (Balintoni et al, 2011) was massively intruded by granite bodies and their accompanying dyke-swarms (Berza and Seghedi, 1983). There are Cadomian granites with their migmatic escort (Grünenfelder et al, 1983;Liégeois et al, 1996;Balintoni et al, 2011) and Variscan bodies accompanied by cross-cutting dykes (Balica et al, 2007;Balintoni et al, 2011).…”

Section: Variscan Granites In the Danubian Domain Of Romanian South Cmentioning

confidence: 99%

“…There are Cadomian granites with their migmatic escort (Grünenfelder et al, 1983;Liégeois et al, 1996;Balintoni et al, 2011) and Variscan bodies accompanied by cross-cutting dykes (Balica et al, 2007;Balintoni et al, 2011).…”

Section: Variscan Granites In the Danubian Domain Of Romanian South Cmentioning

confidence: 99%

“…Using the data from sample 227A, Balintoni et al (2011) obtained a crystallization weighted mean age of 591.0±3.5 Ma and a Concordia age of 591.6±1.8 Ma (Fig. 6a, b).…”

Section: Cadomian Granites and Migmatites Grünenfelder Et Al (1983)mentioning

confidence: 99%

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Zircon Recrystallization History as a Function of the U-Content and Its Geochronologic Implications: Empirical Facts on Zircons from Romanian Carpathians and Dobrogea

Balintoni¹,

Balica²

2012

Recrystallization

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IntroductionAccording to Davies et al. (2003), "…the age of Earth and the time scale of pre-human events are central to a civilization's sense of origin and purpose. Therefore, the quest for precise and reliable geochronometers has had a scientific and cultural importance that few other enterprises can match". In this respect, since the beginning of the last century it has been recognized that long-lived radioactive decay systems provide the only valid means of quantifying geologic time.One of the most reliable Earth's timekeeper has proven to be the mineral zircon, since it records the ages of Earth's earliest evolution stages, the oldest sediments, extinction episodes, mountain-building events and supercontinents' coalescence and dispersal (e.g. Rubatto and Hermann, 2007;Harley et al., 2007). Its widespread use in geochronology is based on the decay of uranium (U) and thorium (Th) to lead (Pb). They provide three distinct radioactive decay series involving the parent isotopes 238 U, 235 U and 232 Th and their daughter isotopes 206 Pb, 207 Pb and 208 Pb, respectively. Through the incorporation of U and Th at the time of growth, every zircon grain hosts three different clocks. In an ideal closed system, the three estimates would agree with each other within the analytical errors of measurements. However, in natural systems the zircon grains are not equally closed for Th and U with respect to post-crystallization effects. The usual approach in zircon geochronology is to consider the U-Pb system alone, as there is no natural non-nuclear ways of fractionating 235 U from 238 U. As the modern day-ratio of 235 U/ 238 U is well known (1/137.88) the need to actually analyze very low abundances of 235 U is obviated. Besides U and Th, zircon can incorporate some other incompatible elements such as P, Sc, Nb, Hf, Ti, and REE in trace (up to thousands of ppm) or minor (up to 3% wt) amounts. The primary control factor on the substitutions is the ionic radii of the substituting cations compared with Zr 4+ and Si 4+ cations. Substitutions that minimize strain effects on either or both sites will be favored. The crystal-chemical limitations are that Zr 4+ in 8-fold coordination has an ionic radius of 84*10 -3 nm and Si 4+ , in tetrahedral coordination, has an ionic radius of 26*10 -3 nm. U 4+ (ionic radius of 10*10 -2 nm in 8-fold coordination) and Th (105*10 -3 nm in 8-fold coordination) can be accommodated in the Zr 4+ sites. Uranium concentrations are usually www.intechopen.com Recrystallization 304 less than 5000 ppm and Th concentration less than 1000 ppm. Because of its ionic radius of 129*10 -3 nm (8-fold coordination), Pb 2+ is highly incompatible with growing zircon crystal lattice and therefore is not incorporated more than ppb levels, which is crucial in geochronology. Because of the same reason, Pb 2+ can easily escape from zircon lattice when some conditions are fulfilled.Based on idea of concordant ages between 235 U/ 207 Pb and 238 U/ 206 Pb, Wetherill (1956) has developed the Concordia diagram. Quite soon thou...

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Section: Variscan Granites In the Danubian Domain Of Romanian South Cmentioning

confidence: 62%

Section: Variscan Granites In the Danubian Domain Of Romanian South Cmentioning

confidence: 99%

Section: Variscan Granites In the Danubian Domain Of Romanian South Cmentioning

confidence: 99%

“…Using the data from sample 227A, Balintoni et al (2011) obtained a crystallization weighted mean age of 591.0±3.5 Ma and a Concordia age of 591.6±1.8 Ma (Fig. 6a, b).…”

Section: Cadomian Granites and Migmatites Grünenfelder Et Al (1983)mentioning

confidence: 99%

See 2 more Smart Citations

Zircon Recrystallization History as a Function of the U-Content and Its Geochronologic Implications: Empirical Facts on Zircons from Romanian Carpathians and Dobrogea

Balintoni¹,

Balica²

2012

Recrystallization

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“…Landing 2004;Shail and Leveridge 2009;Landing et al 2013a, b) and Germany (e.g. Meissner et al 1994;Cocks et al 1997;Verniers et al 2002) to the eastern Bohemian Massif in the Czech Republic (Finger et al 2000;Kalvoda et al 2008), the South Carpathians of Romania (Balintoni et al 2011), and the Pelagonian (Zlatkin et al 2014), Serbo-Macedonian (Meinhold et al 2010) and Istanbul zones (Okay et al 2008) of Greece and Turkey.…”

Section: Introductionmentioning

confidence: 99%