Palaeomagnetism of Precambrian rocks from Gabon, Congo craton, Africa

Shrimp U–Pb zircon age evidence for Paleoproterozoic sedimentation and 2.05Ga syntectonic plutonism in the Nyong Group, South-Western Cameroon: consequences for the Eburnean–Transamazonian belt of NE Brazil and Central Africa

“…The geological features described in both regions are part of a N-S collisional belt refered to as the West Central African Belt (WCAB, Feybesse et al, 1998;Penaye et al, 2004) and recognized in NE Brazil as the Transamazonian granulite belt (Ledru et al, 1994;Teixeira and Figueiredo, 1991;Van Schmus et al, 1995;D'Agrella-Filho et al, 1996;Almeida et al, 2000;Barbosa and Sabaté, 2002). In both belts, the age range of the orogenic cycle is constrained between 2.4 and 1.9 Ga with a peak of tectono-metamorphic and plutonic activity between 2.1 and 2.0 Ga.…”

Neocomian to early Aptian syn-rift evolution of the normal to oblique-rifted North Gabon Margin (Interior and N'Komi Basins)

“…The final stage between 2.8 and 2.5 Ga was related to the emplacement of the Kinguele ultrabasic rocks (ca. Maurin, 1993;D'Agrella-Filho et al, 1996;Feybesse et al, 1998). The Precambrian grain controls the nature of the early rifting of Neocomian to early Barremian age (syn-rift 1-2).…”

“…The Congo Craton is an amalgamation of Archaean tectonic units that were reworked during the Early Proterozoic (Ledru et al, 1989). The Late Proterozoic mobile belt in the study domain consists of tectonic units that accreted during the Pan-African collisional event (Ledru et al, 1989;De Matos, 1992;D'Agrella-Filho et al, 1996;Feybesse et al, 1998). The Pan-African fold belt was generated by rifting (ca.…”

Tearing up Rodinia: the Neoproterozoic palaeogeography of South American cratonic fragments

“…750 Ma break‐up recorded around the Rodinian continents, South American and African continental masses experienced rifting and collisional events almost simultaneously in the 1.0–0.75 Ga interval. An early attempt to break up the Congo – São Francisco junction may have been recorded by a voluminous set of 1.1–0.9 Ga mafic dykes, which crop out along the border of these blocks (Machado et al ., 1989; D'Agrella‐Filho et al ., 1990, 1996; Renne et al ., 1990). This process led to the development of a relatively restricted oceanic domain, the Adamastor ocean, from which ophiolitic remnants are dated at 0.8 Ga (Pedrosa‐Soares et al ., 1998, 2001; Tack et al ., 2001).…”