Abstract The Jerusalem field produces dry gas from two sands in the lower part of the Atoka Series. The upper sand is called the “Allen” and the lower sand the “Barton” or “Barton ‘B’.” A third sand, the McGuire, overlies the Allen Sand and may prove to be productive over a very small area on the structurally highest part of the field. The gas is trapped in a faulted anticline. The Allen reservoir is limited downdip on both sides of the fault by a gas-water interface. The Barton Sand reservoir is limited on the west and the north flanks by lack of permeability and porosity, on the south by a normal fault, and on the east by a gas-water interface. The oldest rock penetrated by drilling in the Jerusalem field was in the Carter Oil Co. No. 1 Morrilton Lumber Co. This well bottomed at 3,500 ft in the Fayetteville Shale of Mississippian age. The deeper formations have not been tested in this area. Three formations of Ordovician age can be considered to be potential reservoirs, not only here but also in a large part of the Arkansas valley, particularly along the north rim of the basin—the St. Peter Sandstone, the Cotter Dolomite, and the Powell Dolomite. Twelve wells have been drilled in the process of defining the field limits. Six were producing wells and six were dry holes. Two of the producing wells are completed dually. The writer believes Jerusalem field is one of many small but economical fields which will be discovered on the north rim of the basin. The estimated gas reserve attributed to this field ranges from 18 to 25 billion cu ft.

Abstract This field trip explores the role of geology in the origins and production of a distinctly American distilled spirit. Bourbon whiskey originated in the late 1700s and early 1800s in the Bluegrass region of north-central Kentucky. The Inner Bluegrass is marked by fertile, residual soils developed on karstified Ordovician limestones. Corn was grown, ground, fermented, and distilled to yield a high-value product that would not spoil. The chemistry of limestone water (dilute calcium-bicarbonate type with near-neutral pH) limits dissolved iron and promotes fermentation. Many farms and settlements were located near perennial springs, whose relatively cool temperatures (~13–15 °C) facilitated condensation of steam during distillation. We will visit three historically significant springs. Royal Spring in Georgetown was an early site of whiskey production and is one of the few springs in Kentucky still used for municipal water supply. McConnell Springs was the purported site of Lexington’s founding and occupies a karst window in which distilleries once operated. Cove Spring in Frankfort was the site of the first public water supply west of the Allegheny Mountains. We will also tour two distilleries: Woodford Reserve (among the oldest and smallest in the state, and a National Historic Landmark) and Four Roses (listed on the National Register of Historic Places).

Data collected from outcrops of the Cretaceous Ferron Sandstone, central Utah, support the theory that stratigraphic heterogeneities are predictable and can be related to position within a stratigraphic cycle ( Gardner 1993 ; Barton 1994 ; Barton 1995 ). Specifically, strongly progradational parts of the fluvial-deltaic Ferron system are characterized by mud-rich, internally heterogeneous delta front deposits interpreted to have been rapidly deposited along a river-dominated coastline under conditions of low accommodation and high sediment supply. In contrast, aggradational to retrogradational parts of the system are characterized by sand-rich, internally homogeneous delta front deposits interpreted to have been deposited along a wave-dominated coastline under conditions of relatively high accommodation and low sediment supply. Data collected from Ferron outcrops was integrated with borehole and production data from the nearby Ferron gas field. The Ferron gas field is located just 5 km to the northwest of outcrops studied and produces largely from the Ferron Sandstone. The description of reservoir architecture within the Ferron gas field was aided by calibrating key surfaces and facies successions identified in borehole data with nearby outcrop equivalents. The gas field is positioned near the seaward extent of the Ferron system and consists of four upward shoaling, shallow marine successions. The basal succession steps strongly basinward, the overlying succession is vertically stacked, and the upper two successions are arranged in a backstepping pattern. A comparison of sandstone body geometry and cumulative production on a well-by-well basis for each succession illustrates areas of unrecovered gas and styles of reservoir compartmentation. Aggradational and backstepping shallow marine successions contain relatively large reservoir volumes that are effectively contacted and drained by conventional well patterns. Favorable sites for stratigraphic entrapment, however, exist near the landward pinchouts of these successions where they interfinger with lagoonal mudstones. In contrast, offlapping and downstepping shallow-marine successions are highly compartmentalized by marginal marine and marine mudstones. Past completions have contacted only small reservoir volumes. Optimal reservoir drainage within these units may require additional infill wells outside the standard field limits or at intervals less then conventional well spacing. All factors being equal, these types of shallow-marine deposits possess the greatest amount of reserve growth potential.

Abstract Water wells completed in the Lissie and Beaumont show that artesian conditions exist in spite of supposed lenticularity. Analyses of 1,400 water samples yield a salinity map based on regional, smoothed-out lines of equal chlorine concentration (isosalinity lines) ranging from 500 to 4,000 parts per million. Inability to correlate individual sands requires that the Lissie-Beaumont be treated as a single water sand. Sands, the water of which was sampled, lie beneath a shallow zone of highly saline ground water which is replaced under sandy soil by fresh water of surface origin. The strongest Lissie-Beaumont water analyzed had 9,578 parts, and immediately beneath the Lissie is water with more than 22,000 parts of chlorine. After analogy with the Woodbine artesian sand of the East Texas basin, where isosalinity lines and structural contours are parallel, a wide swing of the lines around the head of Nueces-Corpus Christi Bay is considered to establish a Corpus Christi structural basin, provided the hypothesis of the down-dip flow of surface waters mixing with the original brines may be accepted as the explanation of the observed distribution of salinity in both regions. This hypothesis is favored. Adjustment of the ancient, high-level delta of Nueces River of the Pleistocene to the postulated structural basin, and entrenchment in it of the present Nueces River with its drowned-valley bays, support the structural interpretation of the salinity map. Outside the "basin" the lines are parallel with the gulf shore line. The Beaumont outcrop in Nueces and San Patricio counties is the area covered by the survey. Barton's top-of-salt contours for salt domes suggest that the other bays of Texas may lie in structural basins. Theoretical stages in the evolution of mixed waters of coastal-plain aquifers (reservoir beds) are developed, several being found which could produce the observed salinity gradients of Corpus Christi and East Texas. Opposing interpretations are briefly discussed. The probably varied nature of the connate waters of the Pleistocene may require a combination of methods to explain the observed salinity gradients with the numerous local chlorine "highs." One of the "highs" covers a producing gas field. Other "highs" are believed to be associated with diastrophic structure. Some are probably due to lenses of impervious sediments obstructing down-dip flow in the water sands. Their pattern does not seem to be that of shore-line features, such as lagoon and bay basins. The structural interpretation of the local chlorine "highs" is not studied in detail.

Abstract The west Texas and southeast New Mexico area contains several basins and surrounding platforms that formed and evolved during the Carboniferous and Permian. The collision of Gondwana with Laurasia led to the Ouachita and Marathon orogenies that formed the small intracratonic foreland basins that include the Delaware basin. The Delaware basin is rimmed by a carbonate ramp that evolved into a carbonate platform; it contains thick carbonate and evaporite and thin siliciclastic deposits. The basin is dominated by thick sandstones and siltstones with minor, fine-grained carbonate mudstones and very fine-grained siltstones separating the more sand-rich intervals. Deposition was strongly controlled by sea level fluctuations (glacially controlled eustatic cycles); highstand deposits are dominated by carbonates and lowstand deposits are dominated by siliciclastics. Fine-grained siltstones, with minor shales, are also the background sediments in the basin, particularly during the deposition of the Brushy and cherry Canyon Formations. The Brushy Canyon, formed during a major third-order lowstand cycle with exposure of the carbonate ramp/evolving shelf, is dominated by basinal sandstone deposition. It has been divided into the lower, middle, and upper Brushy Canyon. These probable fourth-order cycles also contain numerous fifth-order cycles. The cherry Canyon Formation is dominated by siltstone deposits. A notable exception is at Last chance Canyon, located near Sitting Bull Falls, which was a feeder canyon supplying coarser grained, high net-to-gross (N/G) sands and silts to the basin. Three outcrops are shown on the following pages that illustrate three distinct channel architectures: single channel (cut-aggrade-abandon), multiple channels (cut-drape-fill), and nested channels with single and amalgamated channels. Contributions from Beaubouef et al., O’Byrne et al., and Barton et al. (chapters 105, 108, 109, this volume) show other channel architectures and facies from the Brushy Canyon Formation.

Abstract The Condor channel complex, part of the Campanian Cerro Toro Formation (see overview by Fildani et al., chapter 32, this volume) forms part of an extensive outcrop belt exposed in the Pare Nacional Torres Del Paine in southern chile. The data presented here illustrate large, coarse-grained, barform elements that are interpreted as deposits within a deep-water channel complex. The photomosaics in Figures 1 and 2 are from the easternmost extent of a continuous but variably dip- and strike-oriented exposure, which is more than a kilometer (0.6 mi) long. It can be traced into the younger section of the Condor channel complex described in detail by Barton et al. (chapter 39, this volume). The lowest exposed part of the cliff section in this eastern panel ( Figure 2 ) contains slumps and thin-bedded channel fills in a low net-to-gross background with lags, collapsed margins, and heterolithic channel fills. These are interpreted as the product of through-going, large-volume, high-density flows interstratified with deposits of sporadic, low-density flows. The upper two-thirds of the cliff face comprises three distinct sand-rich intervals here termed channel story sets (CSS; see paper by O’Byrne et al., chapter 30, this volume, for further definition). The lower two have similar erosional channel features at their base that are filled with thin-bedded tail, lag, and slump deposits ( Figure 2 ). This implies that each channel story set initially had an efficient erosion-and bypass-dominated phase prior to accumulation of dune and interdune/suspension deposits ( Figure 3 ),