Regional and Specific Deposits by Karl H. Wolf (Eds.)

By Karl H. Wolf (Eds.)

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In turn, they are overlain by calcareous conglomerate, ferriferous shale and ferriferous claystone. In all three iron formations, a large proportion of the ooid nuclei are ooid fragments; most detrital quartz grains are subangular to angular, and fossils have been partially ferruginized. , 1965). , 1920). , 1952). R. The Lorraine ironstone beds are up to 5 m thick and are interbedded with sandstone, shale, and sandy, ferriferous, and/or oolitic limestone (Cayeux, 1922; Bichelonne and Angot, 1939; Bubenicek, 1971).

1971). 36). Middle Lower Jurassic SCOS-IF occurs in Germany and England. The OberbankEchte iron formation of Germany, 7 m thick, overlies oolitic marl and underlies oolitic limestone (Finkenwirth and Simon, 1969; Schellmann, 1969). Its epicontinental sea was bounded about 35 km to the east, 85 km to the west-southwest and 125 km to the north­ west; several other SCOS iron formations resulted from sedimentation in this sea (Berg and Hoffmann, 1942). The Marlstone, Cleveland, and Frodingham iron formations of England, from 5 to 9 m thick, respectively overlie ferriferous conglomerate, shale, and limestone.

Another unmistakable difference is that bauxite spherules commonly grow within older spherules and are enve­ loped within earlier-formed concentric layering (Bardossy and Mack, 1967). This was not observed at Paz de Rio or in any other SCOS iron formation and, consequently, Schellmann's (1969) suggestion that ferriferous oolitic structure forms diagenetically may be rejected. One-fifth to one-third of the ooids in all parts of the Paz de Rio iron formation contain fragments of ooids as cores. Ooid fragments without secondary growth are rare.

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