Thermodynamic Properties of Water to 1,000° C and 10,000 Bars

Burnham, Charles W.; Holloway, John; Davis, Nicholas F.

doi:10.1130/spe132-p1

Cited by 305 publications

(146 citation statements)

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“…Lowering P(H 2 0) to 0.5P(Total) results in lowering the reaction temperatures 60° to 75 °C (depending on total pressure). Both the temperature and pressure changes can be calculated using data in Helgeson et al (1978) and Burnham et al (1969). Consequently, the temperatures in Table 4 and Figure 4 are maximum reaction temperatures.…”

Section: Alteration Temperaturesmentioning

confidence: 99%

Hydrothermal Alteration of Peridotite from the Galicia Margin, Iberian Peninsula

Kimball¹,

Evans²

1988

Proceedings of the Ocean Drilling Program

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The Galicia margin lies northwest of the Iberian Peninsula and is a passive ocean margin with thin sedimentary cover. Altered peridotite was recovered from ODP Site 637, on the north-trending ridge at the western edge of the margin, near the oceanic/continental crust boundary.The altered ultramafics were originally clinopyroxene-rich upper mantle harzburgites and are now extensively serpentinized (>85%) and cut by very late-stage carbonate veins. Despite pervasive late, low-temperature alteration, evidence of early, high-temperature alteration remains. Alteration is apparent as (1) amphibole rims on clinopyroxene (>800°C), (2) hornblende + tremolite (450° to 800°C), (3) breakdown of hornblende to form tremolite + chlorite (<450°C), (4) zoned Cr-spinels, (5) hydration of orthopyroxene and olivine to serpentine, (6) serpentine veins, (7) replacement of pyroxene and olivine by calcite, and (8) calcite veins and vugs.Both the relict igneous and the high-temperature alteration minerals (amphiboles) show evidence of brittle deformation. Subsequent low-temperature alteration veins and minerals are deformed only in faulted and brecciated zones. This textural evidence suggests that the low-temperature alteration occurred after emplacement of the ultramafics at the surface. Serpentine fills tension fractures in orthopyroxene, and both serpentine and calcite fill tension cracks in olivine.The high-temperature alterations in these samples are similar to those found in oceanic fracture zone and ophiolite ultramafics. This widespread occurrence of high-temperature alteration suggests that hot fluids were pervasive in these ultramafic blocks.Localization of high-temperature alteration close to large carbonate veins suggests channelization of the late, lowtemperature fluids. Earlier hydrations (e.g., high-temperature alterations and serpentinization) were pervasive.

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Section: Alteration Temperaturesmentioning

confidence: 99%

Hydrothermal Alteration of Peridotite from the Galicia Margin, Iberian Peninsula

Kimball¹,

Evans²

1988

Proceedings of the Ocean Drilling Program

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“…As water occupies 110 cc/mol at 0.5 kbar and 48 cc/mol at 1 kb, 600°C (Burnham et al, 1969), 167 cc volume change for the reaction (19) suggests that at least 2 water molecules are supposed to be released through the reaction (19). The increase of the formation con stant of tri-chloro complexes with decreasing pressure can also be ascribed to the positive vol ume change for the reaction (19).…”

Section: Nac1mentioning

confidence: 99%

Aqueous speciation of zinc chloride in supercritical hydrothermal solutions from 500 to 700.DEG.C. and 0.5 to 1.0 kb.

1998

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“…The model assumes isothermal fluid flow at 370°C, corresponding to a Á calcite-water of 3.8% ; initial fluid and rock compositions of 12.2% (%16.0% (calcite) at 370°C) and 21.0%, respectively; permeable porosity of 0.05; and a molar H 2 O volume of 22 cm [Burnham et al, 1969]. Varying the porosity to as high as 10% had no discernable effect on the geometry of the profile.…”

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confidence: 99%

New evidence for syntectonic fluid migration across the hinterland‐foreland transition of the Canadian Cordillera

2002

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[1] Oxygen isotope data from syntectonic veins, thrust faults, and wall rocks suggest that fluids infiltrated the Western Ranges of the Rocky Mountain foreland from deeper rocks of the Dogtooth Range during Mesozoic contraction. This signifies the first such evidence for kilometerscale fluid migration at the hinterland-foreland transition of the Canadian Cordillera. Fluid infiltration resulted in isotopic depletion in wall rocks and isotopic disequilibrium between veins (fluid) and their host rocks downstream of a lithologic, structural, and isotopic shift between predominantly siliciclastic (Dogtooth Range) and calcareous (Western Ranges) sequences. The shift corresponds with an average d 18 O that is 3.0% higher in the Western Ranges. In the Dogtooth Range, atypically low carbonate values (15.6% ± 0.8% (VSMOW)), and the consistency with which vein signatures approach the average bulk rock d18 O of individual outcrops indicate fluid buffering by a siliciclastic reservoir and outcrop-scale (10 -100 m) fluid circulation. In contrast, rocks and veins in the Western Ranges exhibit a gradational increase in d18 O that extends !14 km eastward and up section from the isotopic shift and possess values that are below or at the low end of typical carbonate compositions (16.2 -20.9% (VSMOW)). Furthermore, veins systematically exhibit lower oxygen values than their host rocks; this implies that the fluids that entered the Western Ranges were in modest disequilibrium with the rocks through which they flowed. We use a one-dimensional reactive transport model to infer that rocks in the Western Ranges experienced a time-integrated fluid flux of 1.1 Â 10 5 mol H 2 O cm À2 (%2.4 Â 10 6 cm 3 cm À2 ) and sluggish reaction kinetics during the flow event.

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Thermodynamic Properties of Water to 1,000° C and 10,000 Bars

Cited by 305 publications

References 0 publications

Hydrothermal Alteration of Peridotite from the Galicia Margin, Iberian Peninsula

Hydrothermal Alteration of Peridotite from the Galicia Margin, Iberian Peninsula

Aqueous speciation of zinc chloride in supercritical hydrothermal solutions from 500 to 700.DEG.C. and 0.5 to 1.0 kb.

New evidence for syntectonic fluid migration across the hinterland‐foreland transition of the Canadian Cordillera

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