Origin of red beds in the Paleoproterozoic Franceville Basin, Gabon, and implications for sandstone-hosted uranium mineralization

Abstract

International audienc

Iron formations: A global record of Neoarchaean to Palaeoproterozoic environmental history

“…2.4 Ga because of greater iron solubility under reducing conditions (e.g., Rye and Holland, 1998); (3) the appearance of red beds after ca. 2.3 Ga (e.g., Roscoe, 1969;Chandler, 1980;Melezhik et al, 2005;Bankole et al, 2016); (4) the loss of S-MIF in sulfide and sulfate minerals in sedimentary rocks deposited after 2.3 Ga (Farquhar et al, 2000;Bekker et al, 2004;Papineau et al, 2007;Partridge et al, 2008;Guo et al, 2009;Williford et al, 2011;Luo et al, 2016;Gumsley et al, 2017); and (5) the increase in Cr and U contents in IF at 2.45 Ga that records the onset of oxidative continental weathering Partin et al, 2013a). anomaly (Alibert and McCulloch, 1993), suggesting a strong hydrothermal imprint on the REE systematics during its deposition, although, as noted above (Fig.…”

Impacts of rock properties on Danxia landform formation based on lithological experiments at Kongtongshan National Geopark, northwest China

“…Although the term ‘Danxia landform’ is not as popular in other countries as in China, extensive international research has been conducted on continental red beds and the development of sandstone and conglomerate landforms [20–25]. Many spectacular red bed landscapes outside China have a similar appearance to Danxia landform, such as the ‘rose-red’ cliffs of Petra, Jordan [26].…”

Clay mineral diagenesis and red bed colouration: A SEM study of the Gercus Formation (Middle Eocene), northern Iraq

“…In addition, a microbial origin has also been proposed for haematite in carbonate rocks (e.g., Boulvain, De Ridder, Mamet, Preat, & Gillan, 2001;Mamet & Preat, 2006;Preat, Mamet, De Ridder, Boulvain, & Gillan, 2000); and clastic rocks (Eren & Kadir, 2013). conditions (Bankole et al, 2016). Typical areas for their formation include fluvial, lacustrine, aeolian, and paralic environments located within rapidly subsiding, fault-bounded basins in extensional settings (Turner, 1980), although other sedimentary environments have also been noted (e.g., Hu et al, 2012;Neuhuber, Wagreich, Wendler, & Spötl, 2007; Song et al, 2017).…”

“…Continental red beds occur across a broad range of sedimentary facies found within non‐marine depositional environments including alluvial fans, river floodplains, deserts, lakes, and deltas (Turner, 1980). They also show a broad stratigraphic range, with examples from the Precambrian (e.g., Bankole et al, 2016; Eriksson & Cheney, 1992) through to the Carboniferous (e.g., Bilardello & Kodama, 2010), Permo‐Triassic (e.g., Sheldon, 2005), Jurassic (e.g., Rubio‐Cisneros & Lawton, 2011), and up into the Holocene (e.g., Walker, 1976). Red beds form in oxidizing conditions with the distinctive red colour being related to the presence of disseminated ferric oxides, typically haematite (Chandler, 1980; Eriksson & Cheney, 1992; Mucke, 1994; Turner, 1980).…”