Aqua de Ney, California, a spring of unique chemical character

Feth, J. H.; Rogers, Suzanne; Roberson, C. E.

doi:10.1016/0016-7037(61)90107-7

Cited by 30 publications

(32 citation statements)

References 3 publications

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“…To our knowledge, trithiolane has not 639 previously been reported to occur in deep-sea hydrothermal systems. However, we have 640 observed trithiolane and several other cyclic carbon-sulfur compounds in strongly alkaline (pH > 641 11) fluids discharged from serpentinite-hosted springs at Aqua de Ney in northern California 642 (Feth et al, 1961;Barnes et al, 1972), suggesting these compounds may be common in fluids 643 discharged from serpentinites (Fig. 5g).…”

Section: Amino Acid Analyses 524mentioning

confidence: 99%

Investigation of extractable organic compounds in deep-sea hydrothermal vent fluids along the Mid-Atlantic Ridge

McCollom

Seewald

German

2015

Geochimica et Cosmochimica Acta

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Section: Amino Acid Analyses 524mentioning

confidence: 99%

Investigation of extractable organic compounds in deep-sea hydrothermal vent fluids along the Mid-Atlantic Ridge

McCollom

Seewald

German

2015

Geochimica et Cosmochimica Acta

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“…Serpentinization reactions generate alkaline, Ca-rich, and Si-poor fluids (Barnes and O'Neil 1969;Seyfried and Dibble 1980;Janecky and Seyfried 1986;Seyfried et al 2007;Klein et al 2009). Fluids influenced by serpentinization reactions are known from mid-ocean ridge settings (Kelley et al 2001(Kelley et al , 2005Charlou et al 2002;Schmidt et al 2007), ophiolites (Feth et al 1961;Barnes et al 1967;Neal and Stanger 1983;Abrajano et al 1988), and forearc regions of subduction zones (Mottl et al 2003(Mottl et al , 2004. Rodingites have been found in a range of tectonic settings, including seafloor spreading centers (Aumento and Loubat 1971;Honnorez and Kirst 1975;Bideau et al 1991;Hekinian et al 1993), rifted continental margins (Beard et al 2002), and ophiolites (Barriga and Fyfe 1983;Hatzipanagiotou and Tsikouras 2001;Austrheim and Prestvik 2008;Iyer et al 2008).…”

Section: Rodingitization Of Gabbro During Serpentinization Of Abyssalmentioning

confidence: 98%

Metasomatism Within the Ocean Crust

Bach

Jöns

Klein

2012

Lecture Notes in Earth System Sciences

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From ridge to trench, the ocean crust undergoes extensive chemical exchange with seawater, which is critical in setting the chemical and isotopic composition of the oceans and their rocky foundation. Although the overall exchange fluxes are great, the first-order metasomatic changes of crustal rocks are generally minor (usually <10% relative change in major element concentrations). Drastic fluid-induced metasomatic mass transfers are limited to areas of very high fluid flux such as hydrothermal upflow zones. Epidotization, chloritization, and serizitization are common in these upflow zones, and they often feature replacive sulfide mineralization, forming significant metal accumulations below hydrothermal vent areas. Diffusional metasomatism is subordinate in layered (gabbroicdoleritic-basaltic) crust, because the chemical potential differences between the different lithologies are minor. In heterogeneous crust (mixed mafic-ultramafic lithologies), however, diffusional mass transfers between basaltic lithologies and peridotite are very common. These processes include rodingitization of gabbroic dikes in the lithospheric mantle and steatitization of serpentinites in contact to gabbroic intrusions. Drivers of these metasomatic changes are strong across-contact differences in the activities of major solutes in the intergranular fluids. Most of these processes take place under greenschist-facies conditions, where the differences in silica and proton activities in the fluids are most pronounced. Simple geochemical reaction path models provide a powerful tool for investigating these processes. Because the oceanic crust is hydrologically active throughout much of its lifetime, the diffusional metasomatic zones are commonly also affected by fluid flow, so that a clear distinction between fluid-induced and lithology-driven

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“…A solubilidade da sílica é constante na faixa de pH 2-9, onde o pH ideal para a precipitação da sílica como coloide é próximo de 4,5; em pH 8, existe a tendência de ocorrer como molécula dispersa (SJOBERG, 1996). Quando em meios de pH extremos, ácido ou principalmente básico, seu potencial de dissolução sofre aumento significativo, por exemplo na nascente de água fria de Aqua de Ney/California/ EUA, que contém ~1870 mg/L de Si (pH=11,6) (FETH et al, 1961).…”

Section: Hidrogeoquímica Da Sílicaunclassified