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Permian Reef Complex Virtual Field Trip
Stop II-3: Brushy Canyon Fm. – Basinal Fan-Channel

Geographic location and stratigraphic 
 position of this stop.
Geographic location and stratigraphic position of this stop.

BE CAREFUL TRAFFIC IS ESPECIALLY HAZARDOUS AT THIS OUTCROP!

submarine fan channel
"Overbank" and channel deposits associated with a submarine fan in the Brushy Canyon Formation. Note soft sediment deformation in the overbank siltstones and shales. Upper part of outcrop shows part of a sand filled channel which cross-cuts and overlies the overbank deposits. Roadside outcrop along U.S. Highway 62-180 south of Guadalupe Pass and near El Capitan scenic turnout, Culberson Co., Texas.
© Peter A. Scholle, 1999
channel deposits associated with a submarine fan
"Overbank" and channel deposits associated with a submarine fan in the Brushy Canyon Formation. Note soft sediment deformation in the overbank siltstones and shales. Upper part of outcrop shows part of a sand filled channel which cross-cuts and overlies the overbank deposits. Roadside outcrop along U.S. Highway 62-180 south of Guadalupe Pass and near El Capitan scenic turnout, Culberson Co., Texas.
© Peter A. Scholle, 1999

An exposure of basinal Brushy Canyon Formation, the lowest unit in the Delaware Mountain Group. The feature of special interest at this locality is the exposed margin of a submarine channel (see photo). Such channels are common in this formation and, at least in this area, generally trend northwest-southeast, that is, perpendicular to the shelf margin. At this locality, we can see dark-colored, graded, relatively fine-grained sandstones, siltstones, and shales in thin beds with some soft-sediment deformation features (see photo). These beds are abruptly cut by a uniform, thick-bedded, sandstone-filled channel. Both types of sediments were clearly soft, even fluid, at the time of deposition, as shown by the fact that the channel margins are extensively deformed by sand injection. Channel cutting and filling most likely were separate events, perhaps separated by considerable time. That is, the channel was cut, acted as a sediment conduit for some time, and then was filled and abandoned. Evidence for this comes from the commonly observed shale drapes which lie between the cut channels and the multiple episodes of later sand fillings (Harms, 1974; Harms and Williamson, 1988).

model of density "overflow" sedimentation
Harms (1974) model of density "overflow" sedimentation of laminated terrigenous sediment in the Delaware basin. Low-density sand-bearing flows were unable to displace dense, saline, basin-center brines and thus moved across the upper interface of the brines dropping their sediment load as they lost velocity. Rarer, denser currents displaced basinal brines yielding classic traction deposits. Process could have operated during both relative high- and low-stands of sea level.

Hayes (1964), Jacka et al. (1968), Payne (1979), Berg (1979), Williamson (1977 and 1979), Bashman (1996) and other authors have interpreted these or similar deposits as part of larger submarine fans and/or as part of a basinally restricted deep-water wedge of siliciclastic sediment (Rossen, 1985; Rossen and Sarg, 1988). The graded, finer-grained sediments are considered to be interchannel or overbank turbidity-current deposits. The cut and fill, massive, amalgamated sandstones are interpreted as part of an anastomosing system of fan channels, eventually abandoned or filled by multiple episodes of sand transport, possibly by grain flows (Watson, 1979). Harms (1974), on the other hand, proposed that the finer-grained sediments were deposited by density overflows (see diagram) which dropped suspended sediments as they moved out over density interfaces within the water column rather than at the sediment-water interface. The channels were cut, according to Harms, by saline and cold density currents (rather than turbidity currents) which formed on the shelf. The sand fillings of the channels were also laid down by density currents.

In either case, these large (commonly more than 0.8 km/1-2 mi wide and 15-30 m / 50-100 ft thick) channelized sandstones, surrounded by lower permeability siltstones and shales, represent significant potential stratigraphic traps. This is especially true because of the close spatial association of these sandstones and the potential basinal source rocks. Indeed, exploration efforts to date have located more than 100 oil and gas fields which produce from channel-sandstone reservoirs of the Delaware Mountain Group, primarily (but not exclusively) from the Bell Canyon Formation (see Table 3).

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