Abstract
In this chapter, a synthesis is presented on the magmatic evolution that occurred in the eastern part of the Fennoscandian Shield between the initial rifting of the Archaean cratons of the shield and the commencement of the Svecofennian orogenic events, covering a prolonged inter-orogenic period from c. 2.5 to 1.95 Ga. The focus is on igneous events that took place on and in the Karelian and Kola cratons. These cratons were stabilised by c. 2.6 Ga, were in close connection or part of the Superia supercraton, started to drift apart after c. 2.45 Ga and were recombined during the Lapland-Kola orogeny at c. 1.93–1.91 Ga (Mertanen and Pesonen 2005; Bleeker and Ernst 2006; Daly et al. 2006; Mertanen and Korhonen 2011). Since the initial rifting of the cratons starting near the Archaean-Proterozoic boundary, the magmatic events over the following time period of c. 500 Ma took place in a continental, within-plate environment. There is no evidence for oceanic crust formation before c. 1.95–2.0 Ga. The 1.95–1.96 Ga age of the Jormua and Outokumpu Ophiolites (Peltonen et al. 1996, 2008) records the definite time limit of the final break-up of the Karelian craton. Before this break-up, both the Karelian and Kola cratons were subjected to extensional stresses and multiphase intraplate rifting, as attested by the presence of many generations of mafic dyke swarms in the Archaean basement (Huhma and Vuollo 2005), but whether any fragmentation and dispersion of the cratons happened between c. 2.45 and 2.0 Ga, is presently unkown.
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Hanski, E.J. (2013). 3.4 Evolution of the Palaeoproterozoic (2.50–1.95 Ga) Non-orogenic Magmatism in the Eastern Part of the Fennoscandian Shield. In: Melezhik, V., et al. Reading the Archive of Earth’s Oxygenation. Frontiers in Earth Sciences. Springer, Berlin, Heidelberg. https://doi.org/10.1007/978-3-642-29682-6_6
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