bluuebunny/crossref_metadata_2025_split huggingface dataset:
Geology of the Main Pass Cap Rock Sulphur Deposit
Authors: Danielson1 D. A. , Spera2 S. J. , Edwards3 A. F. 
Published: August 2024

Abstract
This paper discusses the geology of the Main Pass 299 sulphur and oil deposit as a part of a field conference examining the mineral resources of the Gulf Coast salt dome province. A complementary core workshop provides an opportunity to examine cap rock core from the Main Pass deposit. Interpretations of the geology of the Main Pass deposit presented in this paper are based on data from twenty exploration wells plus the data acquired from sulphur production wells and from oil and gas development wells.
Main Pass 299 is located in the federal offshore Gulf of Mexico about 90 miles southeast of New Orleans and about 30 miles east of Venice, Louisiana (Fig. 1). Water depths average 210 ft. Oil and gas rights on the dome were acquired by Chevron in 1962, who produced in excess of 57 million barrels of oil and 38 billion cubic feet of gas from sandstone reservoirs on the flanks of the salt dome. At the time sulphur was discovered, Chevron had not drilled on top of the dome.
The Main Pass 299 salt dome sulphur deposit was discovered by a joint venture partnership composed of Freeport-McMoRan Resource Partners - FMRP (58.33%); IMC Fertilizer, Inc. (25%); and Homestake Mining Company (16.67%). Main Pass 299 is one of six salt domes drilled in 1988-1989 by FMRP from a total of eleven offshore salt domes acquired in the February 1988 Federal Offshore Sulphur Lease Sale by FMRP and joint venture partners.
In late 1988, FMRP as operator
Successful Exploration Techniques for Haile-Ridgeway type Gold Deposits in South Carolina
Authors: Lapoint Dennis J. 
Published: August 2024

Abstract
Renewed gold exploration in the Carolina slate belt of North and South Carolina that led to the discovery of the Ridgeway gold mine (#5 on Figure 1) by Amselco (now Kennecott) began at about the same time as the last Geological Society of America field trip to focus on southeastern metal deposits. That trip occurred in the fall of 1980 as part of the national GSA meeting in Atlanta, Georgia (Bell, Carpenter, and Feiss, 1980). On that trip at stop 8, Henry Bell described abundant hydrothermal alteration similar to the Haile and Brewer mines in an area with no known gold mines. He noted that auger cuttings from a hole drilled by the South Carolina Geological Survey in the 1960’s near stop 8 at Mount Rehovah church contained 0.06 ppm gold and 220 ppm copper in the upper 9 feet of rock and 10 ppm molybdenum from 30-40 feet. Because the values decreased with depth, the gold was attributed to surface enrichment (Bell, 1976). Samples collected by Bell (1976) of small drainage basins in the region contained up to 1000 ppm tin in heavy mineral concentrates that were also anomalous in gold, boron, lanthanum, niobium, beryllium, and copper (Figure 16 of Bell, Carpenter, and Feiss, 1980). Bell et al. (1980) stated “Geochemical data suggest that this region is on the periphery of an area having many of the ore-bearing characteristics of the Haile and Brewer mines”
Stop 8 was only hundred’s of feet west of the present site of the
Newly Discovered Devonian Sedex-type Base and Precious Metal Mineralization, Northern Carlin Trend, Nevada
Authors: Emsbo Poul , Hutchinson Richard W. , Hofstra Albert H. , Volk Jeffrey A. , Bettles Keith H. , Baschuk Gary J. , Collins Terry M. , Lauha Eric A. , Borhauer Jeffrey L. 
Published: August 2024

Abstract
This report presents evidence for a previously unrecognized type of Au mineralization on the Barrick Goldstrike property that is geochemically, mineralogically, and temporally distinct from classic Carlin-type mineralization (Table 1). This newly recognized mineralization is characterized by a mineral assemblage that includes barite, sphalerite, minor boulangerite, pyrite, galena, minor tetrahedrite, tennantite, chalcopyrite and native gold. Gold occurs as native inclusions in pyrite, chalcopyrite, tetrahedrite, bitumen, dolomite, and barite. In contrast, features recognized in Carlin-type deposits include a mineral asemblage of As-rich pyrite, realgar, orpiment, and arsenopyrite, with a distinct absence of base metal sulfides. Gold occurs as sub-micron inclusions in As-rich pyrite and alteration consists of decalcification, silicification, and argillization. Carlin-type mineralization is younger than a 39 Ma dike (Emsbo et al., 1996).
Recognition of the base metal mineralization resulted from a broad study of the breccia-hosted Carlin-type deposit in the Meikle Mine. Examination of the stratigraphic section adjacent to Meikle revealed that these base metal sulfides and barite are stratiform and occur in unaltered rocks of the Popovich Formation. In Meikle, the base metal-rich assemblage also occurs as discordant veins which were brecciated and cut by Carlin-type mineralization (Lamb, 1995). The association of low but significant gold content with this base metal mineralization outside Meikle prompted a study of its geological and spatial characteristics, its age and significance within the geologic evolution of the Goldstrike property, and the relationship of its gold to its other sulfides.
In this abstract we describes textural, stratigraphic/spatial, and geochemical evidence that this base
Age of Mineralization at the Twin Creeks SHMG Deposit, Nevada
Authors: Hall Chris M. , Simon Grigore , Kesler Stephen E. 
Published: August 2024

Abstract
This paper will explore the significance of thermochemical sulfate reduction (TSR) to the origin of sedimenthosted disseminated gold (SHDG) deposits. TSR provides a means of generating abnormally high concentrations of H2S at moderate temperatures (e.g., 100 to 200°C). A high H2S content is a prerequisite for mobilizing gold and other metals associated with SHDG deposits (Ag, Hg, Sb, As), and is also necessary to form ore bodies with a high Au/Ag ratio. Field and sulfur-isotopic evidence supporting the TSR hypothesis will be reviewed. The discussion will focus on SHDG deposits in the Carlin Trend and similar deposits in China, as well as the Hemlo gold deposit, Ontario, a possible Archean analog of this deposit type. If valid, the TSR hypothesis has significance to the minerals exploration industry as a means to discriminate between favorable vs. unfavorable source rocks.
Mineralization at Twin Creeks mine is hosted by rocks of the Ordovician Comus Formation, which consists of dolomitic to calcareous black shales with tuffaceous interbeds and interlayered basalt flows and sills. These rocks have been deformed into a northwest-trending fold system with a known length of about 4.5 km (3 miles). Gold mineralization post -dates this folding, and is concentrated in the nose of this fold and in favorable stratigraphic horizons in the limbs of the fold. In the most intensely mineralized part of the deposit, the Megapit, the fold is cut into three sections by right-lateral the TC (northern) and DZ (southern) faults trending NE-SW (Fig. 1) and dipping steeply to
Clay Alteration and Age of Sediment-Hosted Disseminated Gold Deposits in the Fold and Thrust Belt, Utah
Authors: Parry W. T. , Wilson Paula N. , Presnell Ricardo 
Published: August 2024

Abstract
Sediment-hosted, disseminated gold deposits in the Mercur district and Bameys Canyon in the Bingham district are infolded and thrust-faulted Paleozoic sediments of the Oquirrh Mountains, Utah. Folding and thrust faulting occurred in a Jurassic event and the Cretaceous Sevier Orogeny (Armstrong, 1968; Almendinger and Jordan, 1981; Almendinger et al.,1984; Snoke and Miller, 1988). The Oquirrh Mountain range is allocthonous and is underlain by the east-vergent Oquirrh thrust (Presnell, 1992; Presnell and Parry, 1995) not te Charleston thrust. Mercur is located . in the southern Oquirrh Mountains dominated by a series of northwest trending anticline-syncline pairs. Barneys Canyon and Bingham are in the central Oquirrh mountains where structural complexity results from the east -vergent thrust belt interacting with the Uinta arch.
An Amagmatic Origin for Carlin-Type Gold Deposits
Authors: Ilchik Robert P. , Barton Mark D. 
Published: August 2024

Abstract
Suggested genetic models for Carlin-type deposits make connections to magmatism, regional metamorphism or regional extension (Sillitoe and Bonham, 1990; Seedorff, 1991; Ilchik and Barton, in press). Depositional mechanisms are uncertain with mixing, wall-rock reaction, and cooling each consistent with at least some of the available evidence (e.g. Hofstra et al., 1991; Kuehn and Rose, 1995). Based on geological, physical, and chemical reasoning, we propose a genetic model in which meteoric fluids were circulated by heat released during crustal extension during the mid-Tertiary. These deeply circulated fluids interacted with the sedimentaryrock pile and scavenged gold under chemically favorable conditions. Upon upwelling, these fluids interacted with various lithologies and/or other fluids and produce the characteristic alteration and metal suites of these deposits. To test the viability of this amagmatic model, we have investigated certain physical and chemical constraints implicit to the model.
Heat balance and thermal convection calculations indicate that ample surface waters could be heated to appropriate temperatures and circulated during rapid crustal extension (Figure 1). Additional heat from magmatism or elevated subcrustal heat flow could have contributed to the overall energy balance but is not necessary. The critical feature needed to generate major hydrothermal systems is a rapid increase in permeability. Such an increase likely accompanied the time-transgressive crustal extension across the northern Great Basin in the late Eocene and early Oligocene. Mass balance calculations indicate that solution transport efficiencies of &lt;10% can account for several times the amount oflmown alteration and mineralization. In contrast, magma-driven or metamorphic fluids appear
Day One Road Log
Authors: John David A. 
Published: August 2024

Abstract
Today's field trip examines late Eocene and Oligocene granitoid intrusions, cogenetic volcanic rocks (Keetley Volcanics), and associated hydrothermally altered and mineralized rocks in the central Wasatch Mountains. Because of late Cenozoic tilting related to Basin and Range extension, a continuum of mid-Tertiary paleodepths is exposed that ranges from about 11 km on the west side of the Little Cottonwood stock to the actual paleosurface on the east side of the range (Fig. 1; John, 1989a). Consequently, we will see a wide variety of textures and styles of emplacement in the intrusive rocks, and a correspondingly wide variety of hydrothermal alteration types and mineral deposits (Lawton et al., 1980; John, 1989a).
Mid-Tertiary igneous rocks in the central Wasatch Mountains consist of three phaneritic stocks exposed in the western and central parts of the range (Little Cottonwood, Alta, and Clayton Peak stocks); six porphyry to fine-grained phaneritic stocks exposed in the middle and eastern parts of the range, primarily in the Park City mining district (Flagstaff, Glencoe, Mayflower, Ontario, Pine Creek, and Valeo stocks); a subvolcanic porphyry complex (Park Premier stock) exposed near the Park Premier mine which is now partly covered by water filling the Jordanelle Reservoir; and coeval volcanic rocks (Keetley Volcanics), subvolcanic intrusions, and a volcanic neck (Indian Hollow plug) are exposed on the east side of the range (Figs. 2 and 3). The intrusive rocks range from coarse-grained, coarsely porphyritic on the west to fine-grained, porphyroaphanitic on the east (John, 1989a). They form a high-K, calc-alkaline series (Vogel
Paleomagnetism of the Oquirrh Mountains and Implications for the Cenozoic Structural History of the Easternmost Great Basin
Authors: Melker Marc D. , Geissman John W. 
Published: August 2024

Abstract
Tertiary intrusive and extrusive igneous rocks and Upper Paleozoic sedimentary rocks were sampled at 47 sites in the Oquirrh Mountains. Paleomagnetic data from over 350 samples provide a grand mean direction for the Oquirrh Mountains derived from site means determined by averaging best-fit lines. The grand mean for the Oquirrh Mountains (D/I = 332.1/55.4, α95 = 4.1) compared with a late Eocene reference direction (D/I = 351.2/58.3, α95 = 2.4) provides a quantitative assessment of the magnitude of deformation related to extension. The discrepancy between the observed and expected late Eocene directions is interpreted to indicate that the Oquirrh Mountains have been tilted some 10.8 ± 4.0 degrees, down to the east, since late Eocene time. This contrasts with previous estimates of about 15 to 25 degrees of tilting based on orientations of volcaniclastic strata and the apparent asymmetry of the Bingham Canyon porphyry copper ore shell. A modest amount of tilt is consistent with a subhorizontal decoupling or anastomosing shear zone model for extension in the eastern Great Basin. Seismic reflection profiles, two-dimensional basin modeling using residual gravity profiles, and earthquake focal mechanisms corroborate this conclusion.
Preliminary Re-Os Dating on Molybdenite Mineralization from the Bingham Canyon Porphyry Copper Deposit, Utah
Authors: Chesley John T. , Ruiz Joaquin 
Published: August 2024

Abstract
Four molybdenite samples from veins in the Bingham Canyon porphyry copper deposit yield a weighted average Re-Os age of 37.0 ± 0.27 Ma. The molybdenite ages all overlap at the 2σ level. Previous investigations have suggested that mineralization at Bingham Canyon is coincident with and genetically related to the emplacement of the Bingham stock within the Bingham intrusive complex. However, the molybdenite ages are younger than all reported ages for magmatism in the Bingham porphyry deposit (~39.8 to 37.6 Ma). This suggests either that all the reported ages of the Bingham intrusions are disturbed and the actual ages of the intrusive rocks are younger or that molybdenite mineralization is not directly related to emplacement and cooling of any dated intrusion exposed at Bingham. The latter scenario would suggest the Bingham stock is just the focal point for the superposition of exsolved fluids from deeper in the system.
History and Production of the West Mountain (Bingham) Mining District, Utah
Authors: Krahulec Kenneth A. 
Published: August 2024

Abstract
Erastus Bingham and his two sons, Thomas and Sanford, began ranching in a wooded canyon in the Oquirrh Mountains in 1848. This was a year after the Latter-day Saint (LDS) pioneers entered the Great Salt Lake Valley, then a part of Mexico (Arrington and Hansen, 1963). They were probably the first Caucasians to recognize mineralized rock in the Oquirrh Mountains and brought their discovery to LDS President Brigham Young.1 Young, however, wisely counseled the Saints to settle and farm Utah to provide the necessities of life and avoid the pursuit of precious metals:
Instead of hunting gold let every man go to work at raising wheat, oats, barley, corn, and vegetables and fruit in abundance that there may be plenty in the land (Robertson and Harris, 1962).
Young did, however, encourage the utilitarian production of coal and iron from the Iron Springs area in southwestern Utah, near Cedar City, in 1851. The Mormon (LDS) pioneers also began a lead mine, discovered by Henry Rollins, and furnace for bullets near Minersville in 1858 (Salt Lake Mining Review, 9/15/1902). They also began producing salt from the Great Salt Lake as early as 1847 (Arrington, 1963). In 1864, Young persuaded a wagon train of pioneers headed for Idaho to set up their saw mill in Bingham Canyon (Boutwell, 1905). Logging flourished in the canyon for the next several years (Spendlove, 1937).
In 1848, gold was discovered at Sutter's Mill in California. The eager Forty-Niners rushed through Utah en route to California, but were
Geology of the Melco Gold Deposit, Oquirrh Mountains, Utah
Authors: Gunter William L. , Austin Gerry W. 
Published: August 2024

Abstract
The Melco deposit is the largest of five gold mines that constitute the 1.5 million ounces Barneys Canyon project. The deposits form an arc along the nose of the north-trending Copperton anticline. Gold mineralization formed in structurally prepared zones near Theologically contrasting formational contacts. Bedding plane slip during Mesozoic folding caused some deformation. The Melco deposit, located on the NW flank of the Copperton anticline, was localized in a structurally complex zone at the intersection of a N 55° E-trending strain corridor and N 30° E-striking high-angle faults. The latter faults provided conduits for Tertiary-age gold-bearing fluids and late stage carbon-pyrite-orpiment-realgar introduction. In cross section, gold distributions resemble an upright goblet with a stem but no base.
These sediment-hosted deposits contain micron-sized gold as native metal and as inclusions within the arsenic-rich rims of zoned pyrite grains. The deposits are anomalous in As-Sb-Tl-Hg, and contain low silver and base metal values. Bleaching and decalcification are the most pronounced alteration effects. Silicification is present but subtle. The deposits lie at the outer edge of an asymmetrical pyrite-Au-As halo developed around the Bingham Canyon porphyry system. There is a growing body of evidence that these sediment-hosted gold deposits represent a distal precious metal event genetically related to late stage mineralization at Bingham Canyon, which lies 5 miles to the south.
Day Three Road Log
Authors: Austin Gerry W. , Gunter William L. 
Published: August 2024

Abstract
Today's field trip examines “Carlin-style” gold deposits hosted within Permian-aged sediments of the Copperton anticline. We will visit two gold mines: the now exhausted Barneys Canyon deposit and the active Melco mine. Representative core will be available at the respective sites. The excursion will focus on the structural controls and alteration related to gold mineralization in this group of deposits. Weather permitting, a traverse will be made along the axis of the Copperton anticline from the Melco haul road south to Bingham Canyon. The traverse will pass down section through a sequence of unmineralized Permian to Pennsylvanian siliceous clastic rocks and end in the Bingham pyrite halo.
This road log begins at the intersection of the new Bingham Highway with Highway U-111, approximately two miles east of the town of Copperton. The route from downtown Salt Lake City to this junction may be followed on the Day Two Road Log for the Bingham Canyon field trip.
The route heads southwest toward Copperton, northwest on a private road toward the Kennecott Utah Copper concentrator, and then continues northwest to the Barneys Canyon and Melco gold mines.
0.0 Begin at the junction of the new Bingham Highway and U-111. Head southwest, toward Copperton, on the new Bingham Highway.
0.5 Dead ahead are the waste-rock piles from the Bingham Canyon mine.
1.5 Turn right, onto a private road, through the entrance gate to the Copperton concentrator.
2.6 Turn right at the fork in the road. Bingham's Copperton concentrator is to the left. The
Road log
Authors: Molnár F. , Lexa J. , Gatter I. 
Published: August 2024

Abstract
km 0 The first Shell gas station on the M3 motorway after the end of Budapest sign. From here, the M3 motorway crosses the Gödöllő Hills during the next 35–40 kilometers. This area consists of a 2 km thick Tertiary-Quaternary sedimentary sequence underlain by Mesosoic carbonate rocks. On the present surface, loess from the Pleistocene glaciation and drift sand deposits are the most common sediments.
60 On the left side ahead the first view of the Western Mátra Mtns. appears. They are the highest mountains of Hungary with 1014 m elevation at the Kékes summit. The visible part of the Western Mátra Mts. is composed of Miocene andesitic-rhyolitic rocks forming a caldera structure with approximately 15 km diameter. The Mátra Mtns. is the object of the field programme on the fourth day and details of regional geology can be found in the guidebook. In front of the mountains the town of Gyöngyős can also be seen.
69 The M3 motorway crosses one of the traditional wine-producing area of Hungary. The vineyards covering 28 000 acres on the southern foreland of the Mátra Mts. are famous for various white vines. The center of the wine region is Gyöngyős.
Behind the vineyards to the left (north) the Eastern Mátra Mtns. can be seen. This part of the Matra Mtns. is built up by andesitic rocks of Miocene age. In contrast to the Western Matra Mts., large caldera structures cannot be found here and the area is very poor in hydrothermal mineralisation.
High- and Low-Sulfidation Epithermal Mineralization of the Mátra Mountains, Northeast Hungary
Authors: Gatter István , Molnár Ferenc , Földessy János , Zelenka Tibor , Kiss János , Szebényi Géza 
Published: August 2024

Abstract
The Mátra Mtns. cover an area of 570 km2 in the western part of the Tertiary-Quaternary volcanic belt of the Carpathians. The average elevation of this region varies between 600 to 700 m; however, the highest peaks in Hungary, Galyatetõ (965 m) and Kékestetõ (1015 m), are found here. The Mátra Mountains consist of two major volcanic units (Fig. 1).
The Paleogene Unit covers an area of about 25 km2 in the northeastern part of the Màtra Mtns. in the vicinity of Recsk village. The Paleogene Unit consists of an Upper Eocene calc-alkaline volcanic sequence intercalated with sedimentary rocks. It formed along the internal island arc part of asubduction zone that was located between the Northern and Southern Alps during the Laramian-Pyrenean orogeny (50–70 Ma). The emplacement of the Paleogene Unit into its present position in the Western Carpathians was caused by a large-scale (ca. 300 km) northeastward movement of crustal units along the re-activated Periadriatic-Darnó strike-slip fault during the lower Miocene (Zelenka, 1973, 1975; Csontos et al, 1992).
The ore complex containing high- and low-sulfidation type epithermal, porphyry copper, skarn and metasomatic replacement deposits and is genetically related to this Paleogene Unit. Mining activities around Recsk go back presumably as far as prehistoric time. However, documentation of prospecting is available only since the 18th century. In the early times copper ores and silver-bearing galena and fahlore were exploited, whereas the alunitized and pyritized wallrock was used for alum production. The enargite-luzonite-grey-ore-Au-pyrite massive/stockwork mineralization was discovered in the middle of the
Post-Caldera Epithermal Veins of the Štiavnica Stratovolcano
Authors: Lexa Jaroslav 
Published: August 2024

Abstract
The post-caldera system of epithermal veins that extends over an area of 100 km2 in the central zone of the Štiavnica stratovolcano includes 120 veins, with the major veins reaching a length of 8 km. Their position in the evolution of the stratovolcano, mineralogy, alteration zoning and genetic aspects are discussed by Lexa et al. (1999) — reprinted in this volume. Here we concentrate on the aspects of the system which are not covered in that paper, including structural aspects, subdivision into mineralization types and a detailed description of the two epithermal veins to be visited.
The system of epithermal veins formed on faults of the Hodruša-Štiavnica resurgent horst in the central part of the caldera. Thus, their evolution was controlled by the structural evolution of the horst. According to structural relationships, radiometric dating of associating rhyolites and radiometric dating of the epithermal veins itself, the uplift of the horst lasted almost 2 Myr, during the Middle Sarmatian to Early Pannonian (roughly 12.5 to 10.7 Ma; Lexa et al., 1999). The regional stress field during this time was dominated by strong NW-SE extension, with the maximum stress axis mostly in a subvertical position, but occasionally also in a sub-horizontal NE-SW orientation (Nemcok et al., in press). This configuration of the stress field is reflected in dip-slip as well as oblique movements on the veins. While the strong extension led eventually to the formation of low-angle and lystric vein structures with a decreasing dip with the increasing depth, the dextral lateral