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

horizontal ones. Most have identified the cracks as “mud cracks” or “playa cracks” (Abbott and Cook 2004; McKee 1934; White 1929). The cracks are deepest near the greatest displacement of the Bright Angel Fault (near Grand Canyon Village), become shallower with distance away from the fault and decreased displacement of the fault. They have a statistically significant preferred orientation with a directional mean of about 143º (Fig. 39) and have been interpreted as sand injectites by Whitmore and Strom (2010). J. Parabolic recumbent folds Large parabolic recumbent folds (Fig. 40) have been found in several places around the Sedona, Arizona area and near Doney Crater (Whitmore et al. 2015). In Sedona, the fold on “Lizard Head” is nearly 7 m thick and extends for at least 50 m along the face of the outcrop. Several sets of folds occur along Brins Ridge. They are 1-2 m thick and extend over a distance of 400 m before the outcrop disappears on one end and is eroded away on the other. It is likely they originally extended over a much greater distance. K. Marine interfingering TheCoconino interfingerswith a number of aqueous deposits, both laterally and vertically around its margins. Below the Coconino, Blakey (1984) has reported marine sand waves within the Schnebly Hill Formation that in turn grade into typical Coconino lithologies. In the Grand Canyon region, a transitional contact between the water-laid Hermit and the Coconino occurs along Tanner Trail (McKee, 1934) and in some places in Parashant Canyon (Fisher 1961). We located this transitional contact along the Tanner Trail (Fig. 41). Within the Coconino, Fisher (1961) reported tongues of fossiliferous marine limestone. We located dolomite beds at Andrus Point which are probably equivalent to Fisher’s limestone beds (Fig. 12). Laterally, the Coconino grades into water-deposited sediments. Peirce et al. (1977) describe what they think is a west to east transition of mostly eolian to mostly water-deposited Coconino along the Mogollon Rim. They report that nearly all of the 90 m of Coconino exposed near Show Low, in east central Arizona, was water deposited. West of a line from about Sedona to Page, the Coconino “intertongues with and is overlain by the Toroweap” (Blakey and Knepp 1989, p. 336). Some authors also report that cross-bedding style, dip direction and grain size in the Toroweap is indistinguishable from the Coconino in the Oak Creek Canyon area, causing them to think part of the Toroweap is eolian (Rawson and Turner-Peterson 1980). Blakey (1990) names the upper part of the Coconino the “Cave Spring Member” and claims that it grades laterally into the Toroweap according to data from Rawson and Turner- Peterson (1980). The Coconino also grades into Toroweap at locations above the Coconino. In northern Arizona, Whitmore and Garner ◀ The Coconino Sandstone ▶ 2018 ICC 587 Figure 7. Thin sections showing grain size and sorting within the Coconino Sandstone (from Whitmore et al 2014).