Polyak, V. J. (1998) Age and Origin of Carlsbad Cavern and Related Caves from 40Ar/39Ar of Alunite. Science, 279 (5358). 1919-1922 doi:10.1126/science.279.5358.1919

References Listed

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	Spongework mazes (sometimes referred to as boneyard) which exhibit passages resembling the interior of sponge or bone and ramiform (branching away) passages types well represented by Carlsbad Cavern and Lechuguilla Cave are characteristic of hypogene caves (6 7). Sulfuric acid indicator minerals found in caves of the Guadalupe Mountains include elemental sulfur gypsum hydrated halloysite alunite natroalunite jarosite hydrobasaluminite and uranyl vanadates; most of these are direct products of cave genesis (2 4 10). Light isotopic ratios of sulfur in the cave minerals (δ 34 S = −30 to 0 per mil relative to troilite in the meteorite Canyon Diablo) indicate that the sulfuric acid responsible for cave genesis was derived from biogenic hydrogen sulfide (4 9 10) most likely produced at the base of the Castile Formation in the Delaware Basin immediately south of the Guadalupe Mountains (9). The caves were formed when the hydrogen sulfide was oxidized to sulfuric acid as it migrated upward and approached the water table in the Capitan reef and forereef facies (Capitan Limestone) (9); massive amounts of limestone and dolostone were subsequently dissolved or replaced by gypsum.
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	Supplementary details of 40 Ar/ 39 Ar analytical procedures irradiation parameters and tables of results for individual analyses are available at . In summary samples were irradiated in vacuo with interlaboratory standard Fish Canyon Tuff sanidine as a neutron fluence monitor: FCT-1 with an age of 27.84 Ma [
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	] relative to a Mmhb-1 flux monitor at 520.4 Ma [S. D. Samson and E. C. Alexander Chem. Geol. (Isotope Geosci. Sect.). 66 27 (1987)]. J factors were determined by CO 2 laser-fusion analyses to a precision of ±0.15 to 0.25% (±2 sigma). Alunite aliquots (15 to 50 mg) were incrementally heated in a double-vacuum molybdenum resistance furnace in 7 to 10 steps at temperatures of 500° to 750°C. Isotopic compositions of argon were measured with a Mass Analyzer Products model 215-50 mass spectrometer. Decay constants and isotopic abundances used in calculations are those suggested by R. H. Steiger and E. Jäger [ Earth Planet. Sci. Lett. 36 359 (1977)]. Plateau ages and associated uncertainties for samples with flat age spectra defined by two or more contiguous incremental steps that comprised >50% of total 39 Ar released and agreed in age within 2 standard deviations were calculated by using the error formula of S. D. Samson and E. C. Alexander [ Chem. Geol. ( Isotope Geosci. Sect. ) 66 27 (1987)].
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	We thank C. E. Chapin of the New Mexico Bureau of Mines and Mineral Resources Socorro New Mexico; D. C. Ford of McMaster University Hamilton Ontario Canada; and C. A. Hill consulting geologist Albuquerque NM for their prereview of this paper. We thank D. Pate J. Richards and the Carlsbad Caverns National Park Service; J. Goodbar and the Carlsbad District Bureau of Land Management; and R. Turner and the Lincoln National Forest Service for the necessary permits and field assistance. Funding for the 40 Ar/ 39 Ar geochronology work was provided by the New Mexico Bureau of Mines and Mineral Resources.

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