Pan-African displaced terranes in the Tuareg shield (central Sahara)

Black, Russell; Latouche, Louis; Liégeois, Jean-Paul; Caby, Renaud; Bertrand, J.

doi:10.1130/0091-7613(1994)022<0641:padtit>2.3.co;2

Cited by 267 publications

(124 citation statements)

References 15 publications

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“…grades and origins represents a major advance in the understanding of the tectonic and crustal accretion history: see Berthelsen ( 1980) for the eastern Sveconorwegian province; Rivers et al ( 1989) for the Grenville province and Black et al ( 1994) for the more recent Pan-African province of the Tuareg shield. Time markers are necessary in each domain to allow some correlations between the different crustal segments of a given erogenic belt.…”

Section: Introductionmentioning

confidence: 99%

The 1160 Ma Hidderskog meta-charnockite: implications of this A-type pluton for the Sveconorwegian belt in Vest Agder (SW Norway)

Zhou

Bingen

Demaiffe

et al. 1995

Lithos

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Section: Introductionmentioning

confidence: 99%

The 1160 Ma Hidderskog meta-charnockite: implications of this A-type pluton for the Sveconorwegian belt in Vest Agder (SW Norway)

Zhou

Bingen

Demaiffe

et al. 1995

Lithos

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“…During the main Pan-African orogenic phase, the WAC was subjected to convergence on all its boundaries, from the north in the Anti-Atlas (Hefferan et al 2000;Ennih & Liégeois 2001), to the east along the Trans-Saharan belt (Black et al 1979(Black et al , 1994Affaton et al 1991;Attoh & Nude), to the south with the Rockelides and the Bassarides belts and to the east with the Mauritanides belt (Villeneuve), with several thrust sheets preserved on the craton itself, such as in Mali (Caby et al). These collisions partly remobilized other cratonic regions to the east of the WAC in the Tuareg shield (Liégeois et al …”

Section: The West African Cratonmentioning

confidence: 99%

The boundaries of the West African craton, with special reference to the basement of the Moroccan metacratonic Anti-Atlas belt

Ennih

Liégeois

2008

168

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The West African craton (WAC) was constructed during the Archaean and the c. 2 Ga Palaeoproterozoic Eburnian orogeny. Mesoproterozoic quiescence at c. 1.7-1.0 Ga allowed cratonization. In the absence of Mesoproterozoic activity, there are no known WAC palaeogeographical positions for that time. At the beginning of the Neoproterozoic, the WAC was affected by several extensional events suggesting that it was subjected to continental breakup. The most important event is the formation of the Gourma aulacogen in Mali, and the Taoudeni cratonic subcircular basin and deposition of platform sediments in the Anti-Atlas. At the end of the Neoproterozoic, the WAC was subjected to convergence on all its boundaries, from the north in the Anti-Atlas, to the east along the Trans-Saharan belt, to the south along the Rockelides and the Bassarides and to the east along the Mauritanides. This led to a partial remobilization of its cratonic boundaries giving rise to a metacratonic evolution. The WAC boundaries experienced Pan-African Neoproterozoic to Early Cambrian transpression and transtension, intrusion of granitoids and extrusion of huge volcanic sequences in such as in the Anti-Atlas (Ouarzazate Supergroup). Pan-African tectonism generated large sediment influxes around the WAC within the Peri-Gondwanan terranes whose sedimentary sequences are marked by distinctive zircon ages of 1.8-2.2 Ga and 0.55-0.75 Ga.WAC rocks experienced Pan-African low grade metamorphism and large movements of mineralizing fluids. In the Anti-Atlas, this Pan-African metacratonic evolution led to remobilization of REE in the Eburnian granitoids due to the activity of F-rich fluids linked to extrusion of the Ouarzazate Supergroup. During the Phanerozoic, the western WAC boundary was subjected to the Variscan orogeny, for which it constituted the foreland and was, therefore moderately affected, showing typical thick-skin tectonics in the basement and thin-skin tectonics in the cover. During the Mesozoic, the eastern and southern boundaries of the WAC were subjected to the Atlantic opening including Jurassic dolerite intrusion and capture of its extreme southern tip by South America. The Jurassic is also marked by the development of rifts on its eastern and northern sides (future Atlas belt). Finally, the Cenozoic period was marked by the convergence of the African and European continents, generating the High Atlas range and Cenozoic volcanism encircling the northern part of the WAC. The northern metacratonic boundary of the WAC is currently uplifted, forming the Anti-Atlas Mountains.The boundaries of the WAC, metacratonized during the Pan-African orogeny have been periodically rejuvenated. This is a defining characteristic of the metacratonic areas: rigid, stable cratonic regions that can be periodically cut by faults and affected by magmatism and hydrothermal alteration -making these areas important for mineralization.

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“…Two principal sutures were identified within West Gondwana: one along the Gariep and Kaoko belts of SW Africa and the Dom Feliciano and Brasilia belts of South America (4; site of the Adamastor Ocean: Hartnady et al 1985), and one along the Pampean, Paraguay and Araguaia belts of South America (5; site of the Clymene Ocean: Trindade et al 2006). Extrapolation of these belts into northern Africa is hindered by a poor understanding of the Saharan Metacraton (Abdelsalam et al 2002) but potential extensions include the Tuareg Shield (6: Black et al 1994) and the Oubanguides Belt (7: Pin & Poidevin 1987). Pre-Grenvillian cratons: AMZ, Amazon; CG, Congo; EAN, East Antarctic; IN, Indian; KH, Kalahari; NA, North Australian; RP, Río de la Plata; SA, South Australian; WA, West Australian; WAF, West African.…”

Section: From Rodinia To Gondwanamentioning

confidence: 99%

Antarctica and supercontinent evolution: historical perspectives, recent advances and unresolved issues

Harley

Fitzsimons

Zhao

2013

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The Antarctic rock record spans some 3.5 billion years of history, and has made important contributions to our understanding of how Earth's continents assemble and disperse through time. Correlations between Antarctica and other southern continents were critical to the concept of Gondwana, the Palaeozoic supercontinent used to support early arguments for continental drift, while evidence for Proterozoic connections between Antarctica and North America led to the 'SWEAT' configuration (linking SW USA to East Antarctica) for an early Neoproterozoic supercontinent known as Rodinia. Antarctica also contains relicts of an older Palaeo-to Mesoproterozoic supercontinent known as Nuna, along with several Archaean fragments that belonged to one or more 'supercratons' in Neoarchaean times. It thus seems likely that Antarctica contains remnants of most, if not all, of Earth's supercontinents, and Antarctic research continues to provide insights into their palaeogeography and geological evolution. One area of research is the latest Neoproterozoic-Mesozoic active margin of Gondwana, preserved in Antarctica as the Ross Orogen and a number of outboard terranes that now form West Antarctica. Major episodes of magmatism, deformation and metamorphism along this palaeo-Pacific margin at 590 -500 and 300-230 Ma can be linked to reduced convergence along the internal collisional orogens that formed Gondwana and Pangaea, respectively; indicating that accretionary systems are sensitive to changes in the global plate tectonic budget. Other research has focused on Grenville-age (c. 1.0 Ga) and PanAfrican (c. 0.5 Ga) metamorphism in the East Antarctic Craton. These global-scale events record the amalgamation of Rodinia and Gondwana, respectively. Three coastal segments of Grenville-age metamorphism in the Indian Ocean sector of Antarctica are each linked to the c. 1.0 Ga collision between older cratons but are separated by two regions of pervasive Pan-African metamorphism ascribed to Neoproterozoic ocean closure. The tectonic setting of these events is poorly constrained given the sparse exposure, deep erosion level and likelihood that younger metamorphic events have reactivated older structures. The projection of these orogens under the ice is also controversial, but it is likely that at least one of the Pan-African orogens links up with the Shackleton Range on the palaeo-Pacific margin of the craton. Sedimentary detritus and glacial erratics at the edge of the ice sheet provide evidence for the c.

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Pan-African displaced terranes in the Tuareg shield (central Sahara)

Cited by 267 publications

References 15 publications

The 1160 Ma Hidderskog meta-charnockite: implications of this A-type pluton for the Sveconorwegian belt in Vest Agder (SW Norway)

The 1160 Ma Hidderskog meta-charnockite: implications of this A-type pluton for the Sveconorwegian belt in Vest Agder (SW Norway)

The boundaries of the West African craton, with special reference to the basement of the Moroccan metacratonic Anti-Atlas belt

Antarctica and supercontinent evolution: historical perspectives, recent advances and unresolved issues

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