The Proceedings of the Eighth International Conference on Creationism (2018)

Formation Location and (conventional age) Selected references and author(s) who made eolian identification (*) General description and notes about the formation Casper Sandstone Wyoming (Pennsylvanian and Permian) Knight 1929; McKee and Bigarella 1979*; Steidtmann 1974* McKee and Bigarella (1979) use this as one of their examples of “ancient sandstones considered to be eolian,” although they concede that its identification has been difficult to determine. They state (p. 221): “The cross-stratified sandstone of the Casper is fine grained and well sorted” and that the formation has a maximum thickness of about 700 ft. (200 m) thick. Knight (1929) believed the sandstone could only be explained by aqueous processes. Cedar Mesa Sandstone Utah (Permian) Baars 1979; Mack 1977; Mountney and Jagger 2004* This southeastern Utah sandstone is about 1280 m thick and consists of a variety of facies including cross-bedded sandstones, redbeds and mudstones. Baars (1979) and also Mack (1977) believed much of the sandstone was marine based on type and orientation of cross-strata, marine fossils and ripples. Mountney and Jagger (2004) believed that it was primarily eolian based on cross-bed spatial variation and architecture. They believed it was deposited in a wet eolian system with a fluctuating water table and occasional fluvial flooding. They give considerable data on cross-bed dips, many averaging about 20°. Coconino Sandstone Arizona, Nevada, California (Permian) Baars 1961*; Baltz 1982; Blakey and Knepp 1989; McKee and Bigarella 1979*; Middleton et al. 2003*, Whitmore et al. 2014. Whitmore et al. (2014) report that It is a nearly pure, subrounded to subangular, fine grained quartz sandstone that is poorly to moderately sorted. It contains occasional dolomite beds, clasts, ooids, cement and rhombs. Its greatest thickness is in the Pine area where it approaches 300 m. Baltz (1982) reports 27-177 m thick beds in the Arica mountains of California. The Glorieta Sandstone of New Mexico is a direct stratigraphic equivalent of the Coconino (Baars 1961). The Schnebley Hill Formation and the DeChelly Sandstone mostly lie stratigraphically below the Coconino; the upper parts interfinger with the Coconino (Blakey and Knepp 1989). The White Rim Sandstone of Utah probably is stratigraphically equivalent with the upper part of the Coconino (Blakey and Knepp 1989). Corrie Sandstone Scotland (Permian) Clemmensen and Abrahamsen 1983*; Gregory 1915*; Piper 1970* The Lower Permian Corrie Sandstone of the Isle of Arran in southwestern Scotland is at least 700 m thick (Clemmensen and Abrahamsen 1983). Piper (1970) described the sandstones in the type section at Corrie, Scotland as medium-grained, very well-sorted, rounded and with frosted grains. The Corrie Sandstone has long been regarded as eolian in origin (Gregory 1915) and more recent workers have agreed with this assessment. Clemmensen and Abrahamsen (1983) proposed that the sandstone was deposited as part of a small erg system bounded to the northwest by alluvial fans. Dawlish Sandstone England (Permian) Clemmensen et al. 1994*; Laming 1966*; Newell 2001* The Dawlish Sandstone Formation (Upper Permian) comprises a series of sandstones and conglomerates exposed along the Devon coast of southwest England identified by Clemmensen et al. (1994) as units produced by alternating arid-humid climatic fluctuations. Much of the formation, especially the lower part, is characterized by cross-bedded units with foresets dipping at angles up to 33 o (Laming 1966). Newell (2001) interpreted cross-bedded facies as eolian dune deposits and tabular facies as eolian sand sheets. De Chelly Sandstone Arizona, Utah, New Mexico (Permian) Baars 1979*; Blakey 1990*; Stanesco 1991* The type section is located in Canyon De Chelly National Monument in the Four Corners area of northeastern Arizona. To the northwest, north and northeast, it becomes part of the Cutler Group of Utah and Colorado where it likely correlates with part of the White Rim Formation. It is similar in cross-bed style and appearance to the Coconino except that it is more orange in color. To the south and east, it likely correlates with the Schnebly Hill Formation which lies conformably below and interfingers with the Coconino Sandstone in the Sedona area. To the southwest, the De Chelly correlates with the Meseta Blanca Sandstone Member of the Yeso Formation in New Mexico according to Baars (1979). The fine to medium-grained sand is bimodal and most of the grains are coated with iron oxide. Some beds have considerable silt content. Borsch et al. ◀ Micas in ancient sandstones ▶ 2018 ICC 323 APPENDIX I. Sandstones, location, references and general notes about sandstone formations referred to in this paper. Paul Garner was a significant contributor to the descriptions in this table.