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Home , Craton, Mozambique, Platform (geology), Shield (geology)

160 NATURE VOL. 237 19 1972 apparently formed on the thick granito-gneissic . Some Aspects of This is shown by the type of sedimentation (mainly terrigenous Development in East rocks) and specific character of magmatism (absence of ultra­ THE development of the African is often considered basic and basic rocks). In some cases the underlying sialic as a progressive growth of the stable areas, or . This crust could be either Archaean or rejuvenated Archaean, growth was achieved through consolidation of mobile belts though this is not established. and around eight primary cores or nuclei, older The following succession of Precambrian events may be than 2,500 m.y. (ref. 1). The of the ancient nuclei is suggested at least for a larger part of South and East-Central small compared with that of the present African . Africa. First, formation of large Archaean craton (older than 2 For other Precambrian shields, such as the Canadian , 2,500 m.y.); second, accumulation of cover over the it has been suggested that the stable areas grew around primary great part of the craton (2,500-2,000 or 1,800 m.y.); third, nuclei. But there is evidence that the process was reversed in development of the first mobile belts (, Ubenda) during the , especially in the Upper marking the beginning of disruption of the protocraton Proterozoic. (2,000-1,800 m.y.); fourth, large scale rejuvenation of the It is now known that mobile belts (or Clifford's vestigeo­ ancient in the Upper Proterozoic (younger than synclines) developed widely in Africa and are formed mostly 1,600 m.y.). Formation of: (a) mobile belts (, by old cratonic material (older than 2,500 m.y.) subjected to , Namaqualand) and (b) miogeosynclines on the tectono-metamorphic rejuvenation at various times. Thus rejuvenated basement (Kibarides, Katangides). the Archaean rocks in the Limpopo belt, and probably those The ancient massifs such as the Tanganyika, and in the Ubendian-Ruzizian belt, were rejuvenated 2,000 to Kaapwaal cratons should be considered not as nuclei but as 1,800 m.y. ago; for those in the Namaqualand belt rejuvena­ the relics of a large Archaean craton. 1 tion occurred 1,250 to 900 m.y. ago •3 • Extensive areas in V. KAZMIN Eastern and North-Central Africa underwent the tectono­ PO Box 5580, metamorphic rejuvenation during Damaran-Katangan Addis-Ababa, (550± 100 m.y.). It seems that the largest mobile belt of this epoch-the Mozambique belt-is mostly built up of Archaean Received December 6, 1971. rocks, as emphasized by the wide distribution of (shown in standard survey maps of and , 1 Clifford, T. N., in African Magmatism and (Edinburgh, 1970). 1 : 125,000) uncommon in metamorphic complexes younger 2 Goodwin, A. M., Geo/. Assoc. , Proc., 19 (1968). than Archaean. Direct transition from the Archaean 3 Anhaeusser, C.R., Mason, R., Viljoen, M. J., and Viljoen, R. P., of the Tanganyika and Rodesia shields to the Mozambique A Reappraisa[of Some Aspects of Precambrian Shield Geology, 4 6 gneisses has been established in a number of localities - • University of the , , Inf. Circ. No. 49 (1968). The Archaean Mozambique gneisses extend to the north as 4 J. V., and Kennerley, J.B., Quart. J. Geo/. Soc. London, 7 Hepworth, far as Ethiopia • 125, 4 (1970). Besides the older gneisses one can distinguish in the Mozam­ 5 Jonson, R. L., Bull. Geo/. Soc. Amer., 19, 513 (1968). bique belt some metasediments (, arocosses, lime­ 6 Sanders, L. D., Geology of the Contact Between the Nyanza Shield and the Mozambique Belt in Western Kenya, Ministry of stones and so on) which once formed a cover on the Archaean of Kenya Bull. No. 7 (1965). 6 Natural Resources, Geol. Survey rocks. In Kenya they were recognized as the Turoka series , 7 Kazmin, V., Nature, 230, 176 (1971). which should probably be correlated with the graphite­ 8 Quennel, A. M., Mckinlay, A. C. M., and Aitchen, W. G., Summary limestone series of Tanzania8 and the Wadera series of southern of the Geology of Tanganyika, P.l. Introduction and Strati­ 7 graphy (Government Printer, , 1956). Ethiopia • The sediments were folded and metamorphosed 9 Cox, K. G., in African Magmatism and Tectonics (Edinburgh, together with the ancient basement during the Mozambique (1970). tectono-metamorphic event. Since the ancient platform cover is older than Upper Proterozoic (in Ethiopia it acts as a "basement" for the Upper Proterozoic folded belts) and younger than Archaean, its age can be tentatively placed within Lower-Middle Proterozoic. Major Strike-slip Fault of Late It therefore appears roughly contemporaneous with the platform cover on the cratonic massifs of . Thus Hercynian Age in it is probable that in pre-Mozambique (or pre-Pan-African) IN Morocco, there are two main zones of Hercynian outcrops, time the belt was a part of a large Archaean craton together one north and one south of the so-called "South Atlastic with what now constitutes the Tanganyika, Rhodesia and Fault"1 (Fig. 1). In the southern part, the intensity of folding Kaapwaal cratons. Tectono-metamorphic activation of the remains moderate, gradually decreasing southward towards old cratonic material led to the formation of the mobile belt the tabular platform of the Sahara Shield. By contrast, the which acted as a zone of weakness and instability during the northern part seems to be the heart of the folded belt: deforma­ later stages of the geological history. In Karroo time the tion is more marked, with an outstanding development of slaty Mozambique and Zambezi belts controlled the distribution cleavage and some , with several intrusions of of sedimentation troughs and volcanism. There is some granitic plutons. evidence that the separation of (or at least the In the alpine zones of the Middle and High Atlas, these separation of from Africa) took place along the Hercynian units have been deformed again by Cainozoic 9 Mozambique belt • The Tertiary- in East tectonics, but not intensely enough to obliterate the Hercynian Africa also follow the pattern of the mobile belts, reflecting a structures. new stage of disruption of the African continent. The principal features of the Hercynian tectonics in most Thus it is hard to accept that the formation of the Mozam­ massives are well known. Because of the widespread post­ bique belt was a "cratonization"; on the contrary, it looks Hercynian deposits, however, only isolated blocks outcrop in like the beginning of disruption of an ancient Archaean this northern zone, so that the general pattern of the folds craton. A somewhat similar idea has already been expressed has not yet been settled. In this communication we show that, 3 by Anhaeusser et al. • If this conclusion is justified for other when attempting to restore the pattern of these Hercynian mobile belts, as is likely to be the case, the area of the Archaean folds, one must take into account the existence of late Her­ protocraton could be very large. cynian strike-slip faults which altered the original features; One must also remember that many Upper Proterozoic and we give a first outline of one of the most important of folded belts in Africa (Kibarides, Katangides) are miogeo- these strike-slip faults.

© 1972 Nature Publishing Group