Henry’s and non-Henry’s law behavior of Br in simple marine systems

Siemann, Michael G.; Schramm, Michael

doi:10.1016/s0016-7037(01)00857-2

Cited by 31 publications

(17 citation statements)

References 15 publications

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“…These K D mineral-melt values for marialite and sodalite, resulting in no significant Cl/Br fractionation, are distinct from those for halides (Stoessell & Carpenter 1986, Berndt & Seyfried 1997, Siemann & Schramm 2002 and apatite-group minerals (Dong & Pan 2002), all of which have marked preference for Cl over Br. This approximately equal uptake of Cl and Br by scapolitegroup minerals and sodalite is probably attributable to their accommodation in the large structural cages of these framework aluminosilicates (Papike & Zoltai 1965, Fleet 1989.…”

Section: Results Of Exchange Experiments and Factors Controlling The mentioning

confidence: 75%

“…Knowledge of the halogens in geological samples is important in our understanding of magmatic, metamorphic and sedimentary processes (e.g., Sigiura et al 1963, Böhlke & Irwin 1992, Carroll & Webster 1994, You et al 1994, McCaig et al 2000, in the formulation of genetic models for mineral deposits (e.g., Kesler et al 1995, Markl & Piazolo 1998 and in the reconstruction of paleoenvironments (e.g., Channer et al 1997, Siemann & Schramm 2002. There is a considerable body of data on F and Cl in rocks, minerals, melts and fluids (Böhkle & Irwin 1992, Carroll & Webster 1994, and references therein).…”

Section: Introductionmentioning

confidence: 99%

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Bromine in Scapolite-Group Minerals and Sodalite: XRF Microprobe Analysis, Exchange Experiments, and Application to Skarn Deposits

Pan¹,

Dong²

2003

The Canadian Mineralogist

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Application of an X-ray fluorescence (XRF) microprobe for the analysis of single grains (80 to 1,000 m in diameter) of Clrich minerals for Br has been evaluated for fluorapatite, chlorapatite, scapolite-group minerals (marialite and meonite) and sodalite. A calibration curve based on the Br contents in four international reference materials has been confirmed by measurements on Brbearing standard solutions and by agreement with the results of Cl-rich minerals from instrumental neutron-activation analyses. Absolute errors associated with individual XRF microprobe analyses (i.e., counting statistics alone) are less than 5%, and the calculated limit of detection in the analysis of single mineral grains is ~1 ppm Br. Matrix and grain-size effects are shown to be negligible. Experiments at 1 atmosphere and 800 to 1000°C yield the following distribution coefficients for Br-Cl exchanges between marialite or sodalite and hydrous NaCl-NaBr melts: K D marialite-melt = 0.97 ± 0.08 and K D sodalite-melt = 0.9 ± 0.1. Therefore, the Cl/Br values in marialite and sodalite closely reflect the halogen proportions of their coexisting melts or fluids. The diffusivity of Br in sodalite follows an Arrhenius relation: D Br = 6.5 ϫ 10 -7 exp(-270 ± 10kJ/mol/RT) m 2 /s, over the temperature range from 800 to 1000°C. D Br in marialite is 1.7 ± 0.3 ϫ 10 -19 m 2 /s at 800°C. The Cl/Br weight ratios of marialite in the Tieshan Fe skarn deposit, China, cluster around 650 ± 40, supporting an origin involving hydrothermal brines from associated evaporites. Scapolitegroup minerals in the exoskarns of the Nickel Plate Au skarn deposit, British Columbia, have Cl/Br from 560 to 570, higher than those (130 to 180) of their counterparts in the endoskarns and vuggy cavities. This variation is attributable to an increased involvement of magmatic water from distal to proximal zones. Similarly, scapolite-group minerals in the Grenville U-Th-Mo-REE pegmatite-skarn-vein deposits vary widely in Cl/Br, from 80 to 380, indicative of mixed sources of hydrothermal fluids. This study shows the potential of Br analysis of Cl-rich silicate minerals for constraining the sources and evolution of hydrothermal fluids.Keywords: XRF microprobe, Br, scapolite-group minerals, sodalite, exchange experiments, distribution coefficient, diffusion coefficient, skarn deposits. SOMMAIRENous évaluons l'application d'une microsonde à fluorescence X pour l'analyse de grains isolés (de 80 à 1,000 m de diamètre) pour le Br dans les minéraux porteurs de Cl comme la fluorapatite, la chlorapatite, les minéraux du groupe de la scapolite tels marialite et méionite, et sodalite. Le calibrage a été fait au moyen des teneurs en brome de quatre étalons internationaux, et a été confirmé avec des résultats obtenus pour des solutions standards contenant du Br et des minéraux riches en Cl analysés par activation neutronique instrumentale. Les erreurs absolues associées à une seule analyse par microsonde à fluorescence X, dues aux seules erreurs de comptage, sont inférieures à 5%, et le ...

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Section: Results Of Exchange Experiments and Factors Controlling The mentioning

confidence: 75%

Section: Introductionmentioning

confidence: 99%

Bromine in Scapolite-Group Minerals and Sodalite: XRF Microprobe Analysis, Exchange Experiments, and Application to Skarn Deposits

Pan¹,

Dong²

2003

The Canadian Mineralogist

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“…The relationship between the partition coefficient and the actual concentration ratios of Sr:Ca for each treatment did not result in a linear relationship, which would be expected if the degree of elemental discrimination was constant at each Sr:Ca concentration (Siemann & Schramm 2002). A non-linear relationship also indicates that the relationship between the elemental concentration of otoliths and water cannot be extrapolated beyond these data points.…”

Section: Effect Of Strontiummentioning

confidence: 82%

Relationship between water and otolith elemental concentrations in juvenile black bream Acanthopagrus butcheri

Elsdon¹,

Gillanders²

2003

Mar. Ecol. Prog. Ser.

196

164

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“…Concentration measurements of Br in rocksalt proved to be a very effective method in characterizing the primary/ secondary origin of rocksalt (Kühn 1957;Fischbeck and Bornemman 1988;Siemann and Schramm 2002). Similarly, extensive studies on the fluid chemistry gave important constraints on the possible sources of fluids in rocksalt (e.g., Herrmann 1981;Herrmann and Knipping 1989;Siemann and Ellendorff 2001).…”

Section: Studies Ofmentioning

confidence: 99%

Solution-precipitation creep and fluid flow in halite: a case study of Zechstein (Z1) rocksalt from Neuhof salt mine (Germany)

Schléder

Urai

Nollet

et al. 2008

Int J Earth Sci (Geol Rundsch)

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Zechstein (Z1) rocksalt from the Fulda basin, from the immediate vicinity of the Hessen potash bed is folded into tight to isoclinal folds which are cut by an undeformed, 1 cm thick, coarse-grained halite vein. Microstructures were investigated in etched, gamma-irradiated thin sections from both the wall rock and the vein. The lack of synsedimentary dissolution structures and the widespread occurrence of plate-shaped and hopper grains in the wall-rock suggests that the sedimentary environment was perennial lake. Deformation microstructures are in good agreement with solution-precipitation creep process, and salt flow under very low differential stress. Strength contrast between anhydrite-rich and anhydrite-poor layers caused the small scale folding in the halite beds. The vein is completely sealed and composed mainly of euhedral to subhedral halite grains, which often overgrow the wall-rock grains. Those microstructures, together with the presence of occasional fluid inclusion bands, suggest that the crystals grew into a solution-filled open space. Based on considerations on the maximum value of in-situ differential stress, the dilatancy criteria, the amount of released fluids from the potash bed during metamorphism and the volume change, it is proposed that the crack was generated by hydrofracturing of the rocksalt due to the presence of the salt-metamorphic fluid at near-lithostatic pressure.Keywords Halite Á Potash salt Á Deformation mechanism Á Hydrofracture Fluid transport in rocksaltStudies of Casas and Lowenstein (1989) and Lowenstein and Spencer (1990) on Quaternary halite deposition showed that the effective porosity and permeability decrease drastically in the shallow subsurface. After about 50 m of burial the halite is nearly completely cemented, and is without any visible porosity. At depth of 100 m, the halite is tight, entirely cemented and has no measurable permeability. The very low permeability of halite is demonstrated by laboratory measurements and its ability to seal large hydrocarbon columns and fluid pressure cells. This very low permeability is maintained during halokinesis, although there are some processes which can lead to the increase in permeability.For example, Fokker (1995) considered the long term evolution of salt permeability after abandonment of solution mining caverns. He showed that when fluid pressure in the cavern approaches lithostatic due to creep convergence, diffuse dilatancy of the roof occurs and the permeability of the salt increases to allow the slow escape of the fluid. Similar high-pressure fluid pockets (porous salt) occur also in nature and these are presumably slowly moving upwards by similar processes. This process might operate in other rock types, as suggested by the mobile hydrofracture model in Bons (2001). The detailed nature of the relation between the effective stress, differential stress and permeability was

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Henry’s and non-Henry’s law behavior of Br in simple marine systems

Cited by 31 publications

References 15 publications

Bromine in Scapolite-Group Minerals and Sodalite: XRF Microprobe Analysis, Exchange Experiments, and Application to Skarn Deposits

Bromine in Scapolite-Group Minerals and Sodalite: XRF Microprobe Analysis, Exchange Experiments, and Application to Skarn Deposits

Relationship between water and otolith elemental concentrations in juvenile black bream Acanthopagrus butcheri

Solution-precipitation creep and fluid flow in halite: a case study of Zechstein (Z1) rocksalt from Neuhof salt mine (Germany)

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