Abstract The Neoproterozoic successions of the São Francisco Craton are primarily represented by the Bambuí and Una groups, deposited in cratonic epicontinental basins, and by the Vazante and Vaza Barris/Miaba groups, which accumulated on passive margins on the edges of the craton. The epicontinental basins comprise three megasequences: glaciogenic, carbonate platform (marine) and dominantly continental siliciclastics. Possible correlative sequences are observed in the passive margin deposits. At least two major transgressive–regressive sea-level cycles occurred during the evolution of the carbonate megasequence, which lies above glaciomarine diamictites of probable early Cryogenian (i.e. Sturtian) age. C, O, Sr and S isotope trends from analyses of well-preserved samples, together with lithostratigraphic observations, provide reasonable correlations for most of the Neoproterozoic successions of the São Francisco Craton. The 87 Sr/ 86 Sr record of these successions, ranging from 0.70769 to 0.70780, supports the proposed correlation with the Bambuí, Una and Vaza/Barris successions, and with the basal units of the Vazante Group. In addition, C-isotope positive excursions ranging from +8.7 to +14‰ and negative excursions from –5.7 to –7‰ VPDB in the Bambuí, Una and Vaza-Barris successions provide key markers for correlations. The precise ages of the sedimentation in these successions remains a matter of debate, but organic shales of two units of the Vazante Group have been dated by Re–Os techniques in two different laboratories, both yielding Mesoproterozoic ages. The Neoproterozoic and Mesoproterozoic successions preserve significant glaciogenic deposits.

Abstract The Congo (CC) and the São Francisco (SFC) cratons were joined at about 2.05 Ga; northern parts of Palaeoproterozoic basement subsequently underwent extension at about 1 Ga, forming intracratonic basins. Neoproterozoic metasedimentary rocks in these basins yield detrital zircons as young as 630 Ma. The Brasiliano and Pan-African ( c. 620–580 Ma) assembly of West Gondwana extensively altered this system. The Sergipano domain occurs north of the SFC, and the comparable Yaoundé domain occurs north of the CC. Crust north of the Sergipano domain comprises the Pernambuco–Alagoas (PEAL) domain. The NE–SW-striking Tcholliré–Banyo fault in Cameroon may extend southwestwards between the PEAL and Sergipano domains, defining northern limits of abundant SFC/CC basement. The Adamawa–Yadé domain in Africa does not appear to extend into Brazil. The Transverse domain of Brazil is a collage of Palaeoproterozoic crustal blocks, the 1.0 Ga Cariris Velhos orogen (CVO), late Neoproterozoic basins, and Brasiliano granites. The CVO extends ENE for more than 700 km in Brazil, but eastern continuation into Africa has not been identified. North of the Transverse domain contiguous c. 2.15 Ga gneisses comprise basement of Rio Grande do Norte and Ceará domains, which continue eastwards into western Nigeria and western Sahara.

Abstract Most Palaeozoic magmatic rocks in Spain were produced during the Variscan orogeny, and there are excellent and abundant examples of both volcanic and plutonic lithologies. Volcanic units include those in the world-famous Iberian Pyrite Belt, and plutonic rocks exposed in the Iberian Massif include some of the largest and best granite outcrops in the European Variscides. Magmatic rocks are present in all the Iberian tectonostratigraphic zones into which the Variscan orogen in Spain has been classically divided. In addition to these Variscan igneous rocks, there is also evidence for earlier magmatism, including widespread exposures of Neo-proterozoic–Cambrian (Cadomian) age, and the diatreme-like breccias linked to the origin of the remarkable mercury mineralization at Almaden. In this chapter we deal initially with Palaeozoic volcanic rocks, with special emphasis on the volcanism related to the generation of the Iberian Pyrite Belt. With regard to the Variscan granitoid rocks we have grouped these according to compositional features and relative age, rather than by tectonostratigraphic zones (the latter approach does not contribute to a better understanding of the magmatism because the emphasis is on differences and not on similarities). However, Variscan granites of the Iberian Massif are described separately from other granitic massifs in the Pyrenees and Catalonian Coastal ranges, because of their geographic separation and the lack of obvious direct links between them. Outcrops of distinctive mafic and ultramafic rocks, mostly related to granitoids of the appinite–granodiorite association (cf. Pitcher 1997 ), are treated separately, not least because of their importance in international