Precambrian Research 358 (2021) 106185 0301-9268/© 2021 Elsevier B.V. All rights reserved. The early Statherian (ca. 1800–1750 Ma) Prutivka-Novogol large igneous province of Sarmatia: Geochronology and implication for the Nuna/ Columbia supercontinent reconstruction Leonid Shumlyanskyy a, * , Richard E. Ernst b, c , Aleksander Albekov d , Ulf S¨ oderlund e , Simon A. Wilde a , Andrey Bekker f, g a School of Earth and Planetary Sciences, Curtin University, Australia b Department of Earth Sciences, Carleton University, Ottawa, Canada c Faculty of Geology and Geography, Tomsk State University, Tomsk, Russia d Faculty of Geology, Voronezh State University, Voronezh, Russia e Department of Earth and Ecosystem Sciences, Lund University, Lund, Sweden f Department of Earth and Planetary Sciences, University of California, Riverside, CA 92501, USA g Department of Geology, University of Johannesburg, Auckland Park 2006, South Africa A R T I C L E INFO Keywords: Early Statherian Baltica Sarmatia Mafc-ultramafc magmatism Nuna/Columbia supercontinent Large igneous province ABSTRACT The Ukrainian Shield and Voronezh Crystalline Massif constitute the Sarmatian segment of Baltica. Here, only a few mafc-ultramafc dykes and layered intrusions have been dated, recording early Statherian (ca. 1800–1750 Ma) ages. We have determined new U-Pb baddeleyite ages for the Novogol sill (1789 ± 2 Ma) and the Gre- myachye intrusion (1781 ± 7 Ma), which fall within the previously established age range of mafc magmatism in Sarmatia. Overall, mafc magmatism started at ca. 1800 Ma and reached a peak at ca. 1790 Ma. Several in- trusions were emplaced between ca. 1785 and 1775 Ma. The next signifcant peak in magmatic activity took place at ca. 1760 Ma, although a few dykes are dated as late as ca. 1750. Together, these rocks constitute the Prutivka-Novogol large igneous province (LIP), with the main components consisting of tholeiitic dolerite, sub- alkaline olivine gabbro, high-Ti (picrite, camptonite) dykes, and kimberlite. Abundant anorthosite-mangerite- charnockite-granite (AMCG) magmatism also occurred throughout the Ukrainian Shield, coeval with tholeiitic magmatism. Early Statherian mafc magmatism was widespread in many parts of the Nuna/Columbia supercontinent, and magmatic barcoding demonstrates that the Sarmatia, Amazonia, S˜ ao Francisco, West Africa, and North China cratons record similar events and were therefore probably in close proximity. This suggests that the Prutivka- Novogol LIP was part of a much larger superplume that affected an extensive area within the newly-formed supercontinent. 1. Introduction Mafc magmatism in an intracontinental anorogenic tectonic setting is typically represented by tholeiitic mafc dykes and layered mafc- ultramafc intrusions, that are the result of crystallisation of mantle- derived melts and commonly signify important global events in the geological history of our planet. Their formation requires signifcant mantle disturbance that has large-scale consequences in the form of continental food basalt provinces, crustal extension resulting in conti- nental rifting and, in some cases, continent breakup, climate change, and extinction events. There is an ongoing debate regarding the cause of extensive mantle melting beneath stable continents, with models of either tectonically induced decompression mantle melting or arrival of a hot mantle plume being prevalent (e.g. White and McKenzie, 1989; Richards et al., 1989; Campbell and Griffths, 1990; Maruyama, 1994; van Wijk et al., 2001; Courtillot et al., 2003; Ernst, 2014; Doucet et al., 2020; Ernst et al., 2021). Regardless of the details of their origin, mafc dykes and layered intrusions occur over large areas that may be considered as the roots of large igneous provinces (LIPs) (Ernst, 2014). These provinces may occur * Corresponding author. E-mail address: Leonid.Shumlyanskyy@curtin.edu.au (L. Shumlyanskyy). Contents lists available at ScienceDirect Precambrian Research journal homepage: www.elsevier.com/locate/precamres https://doi.org/10.1016/j.precamres.2021.106185 Received 28 December 2020; Received in revised form 8 March 2021; Accepted 11 March 2021