bluuebunny/crossref_metadata_2025_split huggingface dataset:
Simulation of the Capitan Shelf Margin (Late Permian, Guadalupian) of West Texas/New Mexico, A Response to Eustatic Change and an example of the use of Sedpak
Authors: Kendall C. G. St. C. , Strobel J. , Tang J. , Bezdek J. , Moore P. , Cannon R. , Biswas G. 
Published: November 2010

Abstract
The interactive computer simulation, SEDPAK, can track the sedimentary geometries produced by the filling of a two-dimensional basin from both sides, with a combination of clastic sediment and in situ carbonate growth (Strobel et al., 1987, 1988; Heiland-Hansen et al., 1988; Scaturo et al., 1988). The simulation program is implemented in 'C' and has been executed on Apollo and Sun workstations using graphical plotting functions based on the 'X' windows system. Sediment geometries are plotted on the graphics terminal as they are computed, so the user can immediately view the results. Then, based on these observations, the parameters can be repeatedly changed and the program rerun till the user is satisfied with the resultant geometry.
SEDPAK models geometries of clastic and carbonate sediments as they evolve through time and respond to depositional processes that include tectonic movement, eustasy, and sedimentation. Clastic modeling includes sedimentary bypass and erosion and sedimentation in alluvial and coastal plains, marine-shelf, basin-slope, and basin-floor settings. Carbonate modeling includes progradation, the development of hard grounds, downslope aprons, keep up, catch up, back step, and drowned reef facies, as well as lagoonal and epeiric facies. Also included is the capability to model extensional vertical faulting of the basin, sediment compaction, and isostatic response to sediment loading.
Subaqueous Gravity Flows in the Rader Member, Capitan Reef Complex (Permian), Delaware Mountains, West Texas
Authors: Lawson Ellen C. 
Published: November 2010

Abstract
The Rader Member contains coarse, allochthonous carbonate debris deposited on low-angle slopes (&lt;10°) basinward of a ~500 m, higher-angle (30°) foreslope (Rigby, 1953; King, 1948). Subaqueous gravity flows fill channels which have up to 40 m of relief. Bed thickness for a single flow ranges from &lt;1 m to as much as 15 m. Some mass flows are traceable &gt;6.5 km parallel to depositional strike and extend &gt;17 km southeast from the toe-of-slope into the Delaware Basin. A previously undocumented, prominent basin-sloping erosion surface occurs at the base of the mass flows and truncates 55 m of section in the toe-of-slope (Fig. 1). The angle of truncation is as high as 7° in the toe-of-slope and diminishes to &lt;1° along the basin slope.
Subaqueous gravity flows in the Rader section exhibit features which suggest deposition from debris flows, turbidity flows, and possibly from density-modified grain flows (or grain flow-debris flow (Hampton, 1979)). Features which imply a debris-flow origin include poorly sorted and graded debris, a wide range of clast sizes, chaotic orientation of clasts, matrix support, and some large rafted clasts near the top of the bed. Atypical features observed are a fine, quartz-rich sand matrix with a small amount of mud (&lt;1%) and appreciable rounding of the clasts. Rader debris flows were competent to carry limestone boulders up to 10 m across in their longest exposed dimension.
Depth Evolution of the Delaware Basin - Castile/Salado Transition
Authors: Hovorka Susan D. 
Published: November 2010

Abstract
Ochoan evaporites of the Castile and Salado formations in the Delaware Basin contain information about the final stages of basin evolution, specifically regarding the nature of the connection to the ocean and stability of local sea level. Core from the Gulf PDB-03 research well, Menton area, Loving County, Texas, was examined from near the base of the Castile Formation to the uppermost preserved halite in the Salado Formation (Figs. 1 and 2) to investigate evaporite depositional environments, especially with respect to paleodepth. A list of criteria for interpretation of paleodepth was developed (Table 1). These criteria are based on (1) comparison of observed evaporite fabrics with similar fabrics in modern and other ancient examples, and (2) interpretation of how observed evaporite processes would effect fabrics in different settings. Comparison of depth criteria with sequences of fabrics observed in the Castile and Salado formations shows systematic textural variation from the base to the top of individual depositional cycles as well as the entire sequence (Figs. 1 and 2).
The Geology of Lechuguilla Cave, New Mexico
Authors: Jagnow David H. 
Published: November 2010

Abstract
Lechuguilla Cave is located 3½ miles WNW of Carlsbad Cavern in the headwaters of Lechuguilla Canyon. The more shelfward position of this cave, combined with its great depth, allows the geologist a rare opportunity to study the very heart of the Permian-age Capitan Reef Complex.
The Evolution of the Delaware Basin - Preliminary Results
Authors: Hill Carol A. 
Published: November 2010

Abstract
This paper summarizes an ongoing research project on the Delaware Basin studying interrelationships between oil-gas, sulfur deposits, Mississippi Valley-type (MVT) ores, and cave genesis. Such an integrated approach was taken by Hill (1987), who suggested that basinal H2S - generated by oil-anhydrite reactions at the Castile-Bell Canyon contact - was the ultimate source for the sulfuric-acid speleogenesis of Guadalupe caves and for MVT ores in carbonate rock along the margins of the basin.
The Role of Hydrogen Sulfide in the Evolution of Caves in the Guadalupe Mountains of Southeastern New Mexico
Authors: DuChene Harvey R. , McLean John S. 
Published: November 2010

Abstract
Part of the Permian Capitan Reef Complex is exposed in the Guadalupe Mountains of southeastern New Mexico and western Texas (Fig. 1). The reef complex includes the Capitan Limestone and the carbonate backreef beds of the Artesia Group that comprise a lithosome called the Capitan aquifer (Hiss, 1976). This lithosome contains well-developed solution openings that range from microscopic to voids the size of Carlsbad Cavern. This solution porosity was once thought to be caused by weak carbonic acid in the phreatic zone within the Capitan aquifer (Bretz, 1949). During the last 15 years, however, workers have obtained evidence indicating that sulfuric acid may be a major cause of carbonate dissolution (Egemeier, 1973; Jagnow, 1977; Palmer et al., 1977; Maslyn, 1979; Davis, 1980; Kirkland, 1982; and Hill, 1987). Sulfuric acid is generated when oxygen (O2) is introduced into solutions containing dissolved hydrogen sulfide (H2S) gas (Hill, 1987).
Hydrogen sulfide is common in subsurface formations in southeastern New Mexico (Bjorklund and Motts, 1959; Hinds and Cunningham, 1970, pp. 4 and 7). In southeastern New Mexico and elsewhere along the subsurface trend of the Capitan reef, H2S is present in accumulations of oil and gas and in associated saline water (Schram, 1956a, p. 103, and 1956b, p. 307; Wilson, 1956, p. 179; and Roswell Geological Society Symposium Committee, 1956a, p. 181, and 1956b, p. 291).
Architectural Controls on the Recovery of Hydrocarbons From Sandstone Reservoers
Authors: Tyler Noel , Finley Robert J. 
Published: November 2010

Abstract
Development of the 330-billion-bairel oil resource remaining in United States reservoirs after conventional primary and secondary recovery will be dependent on the advanced understanding of facies relations and compartmentalization inherent in reservoir depositional systems. Style of deposition, as reflected in internal reservoir architecture, defines flow units that determine how a reservoir drains, where hydrocarbons remain unrecovered at the interwell (macroscopic) scale, and what approaches will be effective in accessing unrecovered oil. A substantial part of the unrecovered oil resource is nonresidual oil that, although mobile in the reservoir, remains unrecovered owing to poor contact by existing wells and vertical or areal bypassing by the waterflood front.
Because heterogeneity style is a product of depositional system, it is predictable and can be characterized in terms from low to high in a lateral and vertical sense. For sandstones, the wave-dominated deltas, barrier cores, and sand-rich strand plains show a low degree of heterogeneity in both dimensions, whereas the highly aggradational backbarrier fans, fluvially dominated deltas, and fine-grained meander belts show a higher intensity of heterogeneity. Other systems can be similarly classified. The resulting matrix leads to delineation of targeted approaches to incremental oil recovery specifically tailored to the distribution of remaining oil saturation. Such approaches, optimized to the character of the depositional system, may include geologically targeted infill drilling, selective recompletion, horizontal drilling, and strategic cross-reservoir flooding involving flood redesign and profile modification. Such techniques are herein termed Advanced Secondary Recovery (ASR) and represent advancements in technology that will lead to near- and mid-term improvements in efficiency that set the stage for later approaches to Enhanced Oil Recovery (EOR).
Hierarchies of Architectural Units in Terrigenous Clastic Rocks, and Their Relationship to Sedimentation Rate
Authors: Miall Andrew D. 
Published: November 2010

Abstract
Sedimentation rates vary by eleven Orders of magnitude and the physical scale of depositional units varies by fourteen orders of magnitude. These variations suggest a hierarchical ordering of depositional units in clastic sedimentary deposits.
A tentative grouping of architectural units has been constructed, based primaril on the recurrence interval of the depositional events: Group 1 deposits are the product of events taking tens of seconds to a few minutes, such as the burst-and-sweep activitiy of a fluid boundary layer. Group 2 deposits are those formed in a few minutes to a few hours, and include ripples and dune depositional increaments. Group 3 deposits are those forming in a few hours to a day or two, including diurnal tidal bundles. Group 4 deposits form in days to a few months, and include such processes as neap-spring tidal cycles:group 4 deposits also encompasse the spacing of many storm events. Group 5 deposits represent one to a few years, such as seasonal events (spring runoff, glacial varves), and occasional violent storrms. Group 6 is for sedimentary processes of a hundred to thousands of years duration, including the evolution of fluvial macroforms, eolian dunes and tidal sand-wave fields. Group 7 represents longterm geomorphic processes, over thousands to tens of thousands of years, such as channel and draa migration. Group 8 processes extend over tens to hundreds of thousands of years, and represent such depositional elements as channel belts, ergs and sand-ridge fields. Fifth-order stratigraphic sequences, many generated by Milankovitch causes, are also of this rank. Group 9 processes are of hundreds of thousands to a few million years duration, such as fourth-order stratigraphic cycles (e.g., major cyclothems, shelf coarsening-upward cycles driven by thrust-loading events, etc). Deposits assigned to group 10 are those taking a few millions to tens of millions of years, including third-order stratigraphic cycles.
Instantaneous sedimentation rates are of a similar order of magnitude within each group, ranging from 105 m/ka for the smallest scale of deposit, to 10-1 m/ka for groups 9 and 10. Deposits of each group may be defined, in some cases, by enclosing bounding surfaces. Hierarchiesof such surfaces have been erected for fluvial and eolian deposits and for some suites of estuarine and shelf bedforms.
Investigations of each group require different techniques. Deposits up to group 7 and possibly 8 may be documented in expectionalyy good outcrop. Studies of moderm deposits of groups 6 to 8 may be carried out using high-resolution geophysical techniques. Groups 7 to 10 require investigation and reconstructio using basin-mapping techniques based on careful correlation. Subsurface well and seimic data may be employed.
Photomosaics of Outcrops
Authors: Wizevich Michael C. 
Published: November 2010

Abstract
Photomosaics can be useful tools for understanding and communicating geologic features expressed on outcrop faces. In order to utilize photomosaics properly, maximum resolution and minimum geometric distortion of the features is necessary. Maximum resolution is best obtained by using quality equipment and by attending to proper technique. In some cases increasing contrast will improve resolution; various methods can be utilized.
Sufficient overlap of photographs in the construction of photomosaics will remove distortion in most situations. A common problem is perspective distortion, the convergence of vertical lines. This occurs when the film plane and outcrop face are not parallel and results in curved or "smiling" mosaics. When it is not feasible to obtain parallelism, several methods can be used to help correct this problem. In many situations fitting a 35-mm camera with a perspective control lens is the simplest and most economical strategy for reducing or eliminating the problem.
The Large-Scale Architecture of The Fluvial Westwater Canyon Member, Morrison Formation (Upper Jurassic), San Juan Basin, New Mexico
Authors: Cowan E. Jun 
Published: November 2010

Abstract
The Westwater Canyon Member of the Morrison Formation (Upper Jurassic) has previously been interpreted as consisting of fluvial “channel systems” tens of kilometers wide and tens of meters thick. Reinvestigation of the member indicates that these “channel systems” actually represent post-depositional aquifer conduits, defined instead by differing sandstone colors, rather than primary depositional features. The member is composed of amalgamated, individual fining-up sandstone sheets each about 5-10 m thick. The absolute widths of these sheet sandstone bodies are at least 1 km and possibly exceed several kilometers. The width.thickness range of the sandstone sheets are well within the typical values of sandstone body dimensions reported from other fluvial sandstones, and are interpreted to represent aggradational channel-belts. Sandstone bodies thicker than about 12 m are the result of amalgamation of these individual unit sandstone bodies, and do not represent individual channel belts as interpreted previously.
Internally, the sheets contain abundant concave-up troughs typically 30 m wide and 5 m thick, filled both laterally and vertically with inclined parallel- to low-angle cross-stratified sandstone, in places exhibiting parting lineation. The laterally-limited extent of these large troughs and nature of their internal fills suggest that they represent short-lived scour fills rather than confined elongated channels. The concave-up erosional base, a negative feature, was most likely formed due to large-scale flow separation within a wider and shallower channel. Physical conditions similar to stream-flow convergence at channel confluences may be responsible for their formation. The abundant preservation of these troughs in the Westwater Canyon Member is consistent with the expected poor preservation of positive barforms in a sweeping, sandy-braided channel belt.
Review of the literature indicates that inferred channelbelt sandstone bodies mostly fall within the thickness range of 1 to 12 m, irrespective of their interpreted fluvial style. Post-depositional large-scale reservoir conduits are also expected to fall within this range for sandy fluvial systems-. Deviations from this range are due to amalgamation of the sandstone bodies or increased grain-size heterogeneity, resulting in an increase and decrease, respectively, of the conduit size.
Architectural-Facies Analysis of Nonmarine Depositional Systems in The Upper Triassic Chinle Formation, Southeastern Utah
Authors: Dubiel Russell F. 
Published: November 2010

Abstract
The Upper Triassic Chinle Formation in southeastern Utah is a sequence of continental strata deposited in a back-arc cratonic basin. Archi tectural-faries analysis of exposures in sub-parallel canyons and in cliffs surrounding structural uplifts reveals an intricately interbedded fluvial-deltaic-lacustrine system characterized by: 1. mobile fluvial-channel belts consisting of stacked, high- and low-sinuosity channel complexes; 2. overbank deposits, including levees, paleosols, marshes, and small floodplain lakes interiingered with crevasse splays and lacustrine deltas; and 3. extensive lacustrine-basin, lacustrine-mudflat, and eolian sandsheet strata deposited throughout the entire study area. Stratigraphic panels of closely-spaced measured sections oriented both perpendicular and parallel to depositional dip depict the facies architecture both within the extra-channel strata and the relations of the extra-channel deposits to adjacent channel complexes.
In the Shinarump and Monitor Butte Members in the lower part of the Chinle Formation, fluvial-channel complexes interfinger with extra-channel facies. These extra-channel facies include levees, crevasse splays, and wetland complexes consisting of lacustrine deltas, lakes, and marshes. In the Moss Back and Petrified Forest Members in the middle part of the Chinle, fluvial-channel complexes interfinger with floodplain strata characterized by paleosols and crevasse splays. Locally, paleosol horizons and lake and marsh deposits serve as marker beds in three dimensions. The Owl Rock and Church Rock Members in the upper part of the Chinle are dominated by laterally extensive lacustrine-basin, lacustrine-mudflat, and minor eolian sandsheet strata that extended throughout the study area.
Variations in Alluvial Architecture Across The Oligo-Miocene Huesca Fluvial System, Ebro Basin, Spain
Authors: Hirst J.P.P. 
Published: November 2010

Abstract
The Huesca System is interpreted as a terminal, distributive fluvial system. Flow across this ‘fluvial fan’ was largely through a network of well-defined channels and the deposits typically consist of channel-sandstone bodies enclosed within floodplain fines. Amalgamation of the sandstone units varies depending on the location within the system. Lateral profiles are used to show that there are systematic and broadly quantifiable variations in the alluvial architecture across the system.
A precise apex for this distributive system cannot be determined, and thus a datum line has been constructed within the proximal region. This datum has enabled plots to be constructed showing medial to distal variations. The results indicate 1. the proportion of in-channel sediment decreased distally; 2. the sandstone bodies thin distally and thus the paleochannels were becoming shallower, and 3. sheet sandstones deposited by laterally unstable channels are prevalent medially, whereas more stable channels, indicated by ribbon sandstones, were more common distally. The decrease in channel depth and in-channel component are probably the result of evaporative water loss, channel bifurcation and gradient decrease. The increased channel stability distally is interpreted to be the result of reduced ability to erode the banks, more frequent avulsion and ephemeral flow.
The alluvial architecture of the ‘peripheral areas’ of the system, adjacent to the thrust front that defines the northern margin of the basin, differs slightly from the main part of the system. The main difference is the higher frequency of ribbon sandstones in the peripheral areas. This may be due to the tectonic instability of the area near the thrust front and periodic inundation by the marginal alluvial fans. Also, these marginal fans would have increased the flow paths of streams into the peripheral parts of the main system.
The study has applications to hydrocarbon exploration in analogous sequences. Radial variations in reservoir potential are indicated and the extents of sandstone bodies in the subsurface may be estimated from the width-thickness relationship determined from the medial part of the system.
Three-Dimensional Reservoir Architecture of a Valley-Fell Sequence and a Deltaic Aggradational Sequence
Authors: Eschard R. , Ravenne C. , Houel P. , Knox R. 
Published: November 2010

Abstract
In the Middle Jurassic series of the Cleveland basin (Northeastern England), the Scalby Formation comprises two main members, interpreted as a valley-fill complex overlain by a deltaic aggradational series. The valley was incised during a relative sea-level drop and infilled during a stepped relative sea-level rise by a retrogradational fluvial to estuarine complex. The valley fill is composed of three superposed sandsheet prisms showing, respectively, 1. fluvially dominated straight channels, 2. tidally influenced meander belts, and 3. a mixed fluvial-tidal meander belt The deltaic aggradational member corresponds to highstand deposits. Small ribbons or meandering channels are isolated in shaly floodplain and lacustrine facies.
A precise three-dimensional reservoir reconstruction has been carried out on a 1-km2 area using cliff sections, drill cores, wireline logs and petrophysical measurements. Accurate reservoir reconstructions are presented here as large cross sections in terms of lithology, porosity and permeability. At Cloughton, the valley-fill member consists of a lower and upper prism. Each corresponds to a channel-fill stage with a basal aggradational fluvial unit overlain by an estuarine or paralic transgressive unit The basal prism displays a fluvial stacked-chaanel unit with side bars and sand or clay plugs, the tops of which are truncated by a transgressive surface. The unit is overlain by an estuarine sand-flat complex. The upper prism corresponds to tidally-influenced meander belts with hectometric point bars composed of argillaceous sandstone and siltstone. It is capped by shaly marsh deposits, corresponding to the period of maximum flooding of the valley fill. The aggradational deltaic member consists mainly of delta-plain shales with multistory ribbon channels and wide meander belts.
The best potential reservoirs are located in the basal fluvial sucked channels of the valley fill. Reservoir qualities decrease in the estuarine sand-flat complex and are very poor in the mixed fluvial-tidal meander belts. The small ribbon channels generally constitute good but small disconnected reservoirs. The sequence stratigraphy of the Scalby Formation shows that reservoir geometry and architecture could be controlled by minor relative sea-level variations.
Constructing a Three-Dimensional Rock-Property Model of Fluvial Sandstones in The Peoria Field, Colorado
Authors: Chapin Mark A. , Mayer David F. 
Published: November 2010

Abstract
Fluid-flow units and fluid-flow barriers are distinguished through mapping distributions of facies and bounding surfaces of coalesced channel belts within the Lower Cretaceous J Sandstone in the Peoria field, Colorado. Measured rock properties (porosity, permeability, relative permeability, and capillary pressure) were calibrated to facies, which were distinguished by common associations of grain sizes, clay content, and sedimentary structures. The three-dimensional distribution of rock properties in the J sandstone reservoir was obtained through facies mapping. Within a meander belt, trough cross-stratified and clean, ripple-laminated point-bar sandstones act as flow units, and clay-rich abandonment fills act as flow barriers. Hydraulic communication between vertically stacked channel belts depends on the thickness and continuity of muddy sandstones having abundant clay inclusions that commonly overlie basal scour surfaces. The effect of smaller scale sedimentary bounding surfaces on fluid flow was not measurable at the scale of the well spacing and engineering data available. Compartmentalization of the reservoir is indicated by two elevations of oil-water contacts along the downdip, west flank of the field. This is explained by a concentration of abandonment-fill facies and a lack of hydraulic communication between coalesced channel belts in the center of the field. Pre- and post-injection production patterns are explained by the geologic model.