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NARROW
GeoRef Subject
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all geography including DSDP/ODP Sites and Legs
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Africa
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ytterbium (1)
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Primary terms
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Africa
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Barberton greenstone belt (1)
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The Sukari Gold Deposit, Egypt: Geochemical and Geochronological Constraints on the Ore Genesis and Implications for Regional Exploration
Neoproterozoic magmatic evolution of the southern Ouaddaï Massif (Chad)
First Evidence of Late Paleoproterozoic/Early Mesoproterozoic Sediment Deposition and Magmatism in the Central Aravalli Orogen (NW India)
Alabandite (MnS) in metamorphosed manganiferous rocks at Morro da Mina, Brazil: palaeoenvironmental significance
Celebrating the Centenary of “The Geology of Central Minas Gerais, Brazil”: An Insight from the Sítio Largo Amphibolite
LATE CAMBRIAN Au-Pd MINERALIZATION AND Fe ENRICHMENT IN THE ITABIRA DISTRICT, MINAS GERAIS, BRAZIL, AT 496 Ma: CONSTRAINTS FROM U-Pb MONAZITE DATING OF A JACUTINGA LODE
U–Pb and Hf isotope data of detrital zircons from the Barberton Greenstone Belt: constraints on provenance and Archaean crustal evolution
Hafnium isotope record of the Ancient Gneiss Complex, Swaziland, southern Africa: evidence for Archaean crust–mantle formation and crust reworking between 3.66 and 2.73 Ga
Published whole-rock Sm-Nd and zircon Lu-Hf data from the Limpopo Complex and adjoining areas of the Zimbabwe and Kaapvaal Cratons provide insight into the regional crustal evolution and tectonic processes that shaped the complex. The Northern Marginal Zone of the complex, and the Francistown area of the Zimbabwe craton, represent an accretionary margin (active at 2.6–2.7 Ga) at the southern edge of that craton, at deep and shallow crustal levels, respectively. The Southern Marginal Zone represents a deep crustal level of the northern Kaapvaal Craton and was not an accretionary margin at the time of high-grade metamorphism (2.72–2.65 Ga). The syntectonic Matok granite was produced by crustal anatexis. In the Central Zone, the presence of ca. 3.5–3.3 Ga crust is indicated throughout its E-W extent by T Nd,DM model ages of metapelites and by zircon xenocrysts and their T Hf,DM model ages. The ca. 2.65 Ga granitoids in the Central Zone (the Singelele-type quartzofeldspathic gneisses in the Musina area, granitoids in the Phikwe Complex, Botswana, the so-called gray gneisses, and the Bulai charnockite) were formed by anatexis of such old crust, whereas 2.6 Ga juvenile (arc-related?) magmatism produced the Bulai enderbite, and may be a component in the Zanzibar gneiss. The Mahalapye granitoid complex in Botswana was formed by crustal anatexis at 2.0 Ga, but mafic and hybrid rocks of this age have a mantle-derived component. The data do not prohibit a collisional model for the Neoarchean high-grade metamorphic event in the Central Zone and Southern Marginal Zone of the Limpopo Complex.
The behavior of the Hf isotope system in radiation-damaged zircon during experimental hydrothermal alteration
Precambrian
Abstract Around 88% of the history of the Earth occurred during the Precambrian period, which can be subdivided into the Archaean and the Proterozoic eons (Figs. 2.1 & 2.2 ). The Archaean eon (Greek archaia — ancient ones; 4.56-2.5 Ga) comprises the Eo-Palaeo-, Meso-and Neoarchaean eras. For the early Archaean the term Hadean is also used (Greek hades — unseen or hell; 4.56-3.8 Ga) (Fig. 2.1). The Proterozoic eon (Greek proteros — first, zoon — creature; 2.5-0.542 Ga) is composed of the Palaeo-, Meso-and Neoproterozoic eras (Fig. 2.2). The latter eras can be subdivided into different periods defined by the International Commission on Stratigraphy on the basis of geochronological data and characteristic features such as particular geotectonic settings and events ( Gradstein et al. 2004 ). Palaeoproterozoic periods include the Siderian (Greek sideros — iron; 2.5-2.3 Ga), the Rhyacian (Greek rhyax — steam of lava; 2.3-2.05 Ga), the Orosirian (Greek orosira — mountain range; 2.05-1.8 Ga) and the Statherian (Greek statheros — stable; 1.8-1.6 Ga). The Calymmian (Greek calymma — cover; 1.6-1.4 Ga), Ectasian (Greek ectasis — extension; 1.4-1.2 Ga), and Stenian (Greek stenos — narrow; 1.2-1.0 Ga) are the Mesoproterozoic periods, while the Neoproterozoic is subdivided into the Tonian (Greek tonas — stretch; 1.0-0.85 Ga), Cryogenian (Greek cryos — ice, genesis — birth; 0.85-0.635 Ga), and finally Ediacaran (0.635-0.542 Ma). This latter is named after the Ediacara Hills (Flinders Ranges, Australia) and characteristically contains the Ediacara biota which represents the dawn of evolved life-forms. The Ediacaran period
Variscan tectonics
Abstract The Variscan Orogeny is the major Middle to Late Palaeozoic tectonometamorphic event in Central Europe representing the final collision of Gondwana with the northern continent of Laurussia. Thus, large areas of the pre-Permian basement consist of continental crust that achieved its final form during this event. The Variscan Orogeny represents the European version of the evolution of the supercontinent of Pangaea at the end of the Palaeozoic. Western Pangaea, including the Variscan Orogen, formed as a result of the continuous closing of the oceanic domains between Gondwana and Laurussia (Old Red Continent: North American Craton + East European Craton + Avalonia). Coeval accretion of large volumes of oceanic crust along the Eastern Uralides and Altaids (Sengör et al. 1993) as well as Precambrian continental crust (e.g. Siberia and Kazakhstan) along the eastern edge of Laurussia represents the formation of eastern Pangaea. Following the Permian termination of collisional tectonics along western Pangaea there was ongoing convergence in the Asian part until the Early Mesozoic, as demonstrated by the evidence of Triassic continental subduction within the Qinling–Dabie–Sulu Belt between the northern Sino- Korean Craton and the southern Yangtze Craton ( Ernst 2001 , and references therein). Despite the occurrence of both pre- and synorogenic subduction processes within the area of the Variscan Orogen, the accretion of juvenile crust plays a relatively minor role in terms of the crustal evolution of the region. Recycling of basement formed during the Neoproterozoic–Early Cambrian Cadomian Orogeny and its Early Palaeozoic cover can be considered to be one
Petrological evolution in the roof of the high-grade metamorphic Central Zone of the Limpopo Belt, South Africa
Abstract During Late Carboniferous-Early Permian times dextral transtensional movements along the NW-trending Franconian Fault System and parallel faults caused complex block faulting in the Thuringian Forest region, Germany, accompanied by intense magmatism. This is well constrained by geochronological data ( 207 Pb/ 206 Pb single zircon, SHRIMP, 40 Ar/ 39 Armica, zircon fission-track ages), field relations, and the sedimentary record from the Ruhla Crystalline Complex (RCC) and surroundings. The combined dataset indicates that the Ruhla Crystalline Complex was faulted into three nearly N–S-trending segments, which underwent different exhumation histories during Late Carboniferous–Permian times. The central segment of the RCC was exhumed by several kilometres as a horst block, while the eastern and western segments subsided simultaneously, forming the basement to the Oberhof and Eisenach molasse basins, respectively. Late Carboniferous–Permian uplift of the central segment is constrained by 40 Ar/ 39 Ar cooling ages of 311 ± 3 (muscovite) and 294−288 ± 3 Ma (biotite), a weighted zircon fission-track age of 272 ± 7 Ma and overlying Zechstein sediments. In contrast, the eastern segment shows much older 40 Ar/ 39 Albiotite cooling ages between 336 ± 4 and 323 ± 3 Ma, was exposed at c. 300 Ma, and subsequently covered by molasse sediments and volcanic rocks between 300 and c. 275 Ma. A similar Late Carboniferous evolution is inferred for the western segment, as it is also overlain by Lower Permian volcanic rocks and has a 297 ± 29 Ma single zircon fission-track age. Simultaneous horst and basin formation is additionally constrained by granite pebbles in conglomerates of the Oberhof and Eisenach basins. These pebbles can partly be derived from granites in the central segment of the RCC. Age data and the orientation of granitoid bodies and dykes in the Ruhla Crystalline Complex and its surroundings provide evidence for the opening of NE-trending structures between 300 and 294 Ma, and formation or reactivation of W- to NW-trending structures between 290 and 275 Ma. Magmatic activity in the Thuringian Forest region may have been caused by widespread mantle upwelling in central Europe during the Late Carboniferous-Early Permian.