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Eddy County New Mexico
Lost bones: In search of Wesley Hurt’s Mammoth, Salinas Pueblo Missions National Monument’s Quarai Unit, central New Mexico
Lithology and reservoir properties of the Delaware Mountain Group of the Delaware Basin and implications for saltwater disposal and induced seismicity
Hypogenic karst of the Great Basin
ABSTRACT Discoveries in the 1980s greatly expanded speleologists’ understanding of the role that hypogenic groundwater flow can play in developing caves at depth. Ascending groundwater charged with carbon dioxide and, especially, hydrogen sulfide can readily dissolve carbonate bedrock just below and above the water table. Sulfuric acid speleogenesis, in which anoxic, rising, sulfidic groundwater mixes with oxygenated cave atmosphere to form aggressive sulfuric acid (H 2 SO 4 ) formed spectacular caves in Carlsbad Caverns National Park, USA. Cueva de Villa Luz in Mexico provides an aggressively active example of sulfuric acid speleogenesis processes, and the Frasassi Caves in Italy preserve the results of sulfuric acid speleogenesis in its upper levels while sulfidic groundwater currently enlarges cave passages in the lower levels. Many caves in east-central Nevada and western Utah (USA) are products of hypogenic speleogenesis and formed before the current topography fully developed. Wet climate during the late Neogene and Pleistocene brought extensive meteoric infiltration into the caves, and calcite speleothems (e.g., stalactites, stalagmites, shields) coat the walls and floors of the caves, concealing evidence of the earlier hypogenic stage. However, by studying the speleogenetic features in well-established sulfuric acid speleogenesis caves, evidence of hypogenic, probably sulfidic, speleogenesis in many Great Basin caves can be teased out. Compelling evidence of hypogenic speleogenesis in these caves include folia, mammillaries, bubble trails, cupolas, and metatyuyamunite. Sulfuric acid speleogenesis signs include hollow coralloid stalagmites, trays, gypsum crust, pseudoscallops, rills, and acid pool notches. Lehman Caves in Great Basin National Park is particularly informative because a low-permeability capstone protected about half of the cave from significant meteoric infiltration, preserving early speleogenetic features.
Paleokarst reservoirs: Efficient and flexible characterization using point-spread-function-based convolution modeling
Applications of quantitative prestack seismic analysis to unconventional resource play characterization in the Permian/Delaware Basin
A New Unified Model For Cave Pearls: Insights from Cave Pearls in Carlsbad Cavern, New Mexico, U.s.a.
Guadalupe Mountains, West Texas and New Mexico: Key excursions
PRESERVATION OF FOSSIL MICROBES AND BIOFILM IN CAVE POOL CARBONATES AND COMPARISON TO OTHER MICROBIAL CARBONATE ENVIRONMENTS
7. Depth and timing of calcite spar and “spar cave” genesis: Implications for landscape evolution studies
Calcite spar (crystals >1 cm in diameter) are common in limestone and dolostone terrains. In the Guadalupe Mountains, New Mexico and west Texas, calcite spar is abundant and lines small geode-like caves. Determining the depth and timing of formation of these large scalenohedral calcite crystals is critical in linking the growth of spar with landscape evolution. In this study, we show that large euhedral calcite crystals precipitate deep in the phreatic zone (400–800 m) in these small geode-like caves (spar caves), and we propose both are the result of properties of supercritical CO 2 at that depth. U-Pb dating of spar crystals shows that they formed primarily between 36 and 28 Ma. The 87 Sr/ 86 Sr values of the euhedral calcite spar show that the spar has a significantly higher 87 Sr/ 86 Sr (0.710–0.716) than the host Permian limestone (0.706–0.709). This indicates the spar formed from waters that are mixed with, or formed entirely from, a source other than the surrounding bedrock aquifer, and this is consistent with hypogene speleogenesis at significant depth. In addition, we conducted highly precise measurements of the variation in nonradiogenic isotopes of strontium, 88 Sr/ 86 Sr, expressed as δ 88 Sr, the variation of which has previously been shown to depend on temperature of precipitation. Our preliminary δ 88 Sr results from the spar calcite are consistent with formation at 50–70 °C. Our first U-Pb results show that the spar was precipitated during the beginning of Basin and Range tectonism in a late Eocene to early Oligocene episode, which was coeval with two major magmatic periods at 36–33 Ma and 32–28 Ma. A novel speleogenetic process that includes both the dissolution of the spar caves and precipitation of the spar by the same speleogenetic event is proposed and supports the formation of the spar at 400–800 m depth, where the transition from supercritical to subcritical CO 2 drives both dissolution of limestone during the main speleogenetic event and precipitation of calcite at the terminal phase of speleogenesis. We suggest that CO 2 is derived from contemporaneous igneous activity. This proposed model suggests that calcite spar can be used for reconstruction of landscape evolution.
Delineating the Rattlesnake Springs, New Mexico Watershed using Near-Surface Geophysical Techniques
Berino Paleosol, Late Pleistocene Argillic Soil Development on the Mescalero Sand Sheet in New Mexico
Synsedimentary dissolution pipes and the isolation of ancient bacteria and cellulose
Stratigraphic Response Across a Structurally Dynamic Shelf: The Latest Guadalupian Composite Sequence at Walnut Canyon, New Mexico, U.S.A.
Flow simulations for carbon sequestration at a coal-seam pilot site
Hydrocarbon potential of the Barnett Shale (Mississippian), Delaware Basin, west Texas and southeastern New Mexico
Abstract Site-specific investigations of bedded evaporites began at the Waste Isolation Pilot Plant site in New Mexico (USA) in 1976, and the first waste was accepted in 1999. Here, we describe and discuss some lessons learned from personal experience. “Fatal flaws” may not be fatal. Features, events, or processes are sometimes useful exclusionary factors, especially during site selection. Solution chimneys discovered northwest of the site in 1975 were possible vertical pathways for radionuclide transport. Intensive field studies since then have indicated no solution chimneys at the Waste Isolation Pilot Plant site. Known chimneys are related to a geologic unit not found at the Waste Isolation Pilot Plant, and chimney fill is not very permeable. Normal fluid flow should be downward if subevaporite formations are connected to near-surface units. If a solution chimney had been found early at the pilot plant, there might have been pressure to relocate it. Timing is important. Potash resources were assessed in 1976 by drilling 21 boreholes; four were completed as shallow hydrology observation wells. Data from all boreholes would have provided a comprehensive picture of the hydrology early in the project history. Resource conflicts were considered more important at the time than hydraulic parameters. Critics will always be with you. the Waste Isolation Pilot Plant is recertified every five years, offering multiple opportunities for outside review and comment. Repeated comments about dissolution of some halite beds, for example, rely on conclusions reached before site-specific studies. Intensive studies since 1984 of shafts, cores, and geophysical logs have shown that halite is distributed mainly by depositional processes. Some critics remain well behind the curve of technical work; we still must respond.