Carbon-13 Isotope Effects in Systems Containing Carbon Dioxide, Bicarbonate, Carbonate, and Metal Ions

Thode, H. G.; Shima, Masako; Rees, C. E.; Krishnamurty, Kotra V.

doi:10.1139/v65-076

Cited by 111 publications

(30 citation statements)

References 11 publications

(9 reference statements)

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“…Isotope exchange reactions are described by equilibrium constants, defined in the standard thermodynamic form as the quotient of the activities of the products and reactant. The equilibrium constants for the abundant species K 1 , K 2 , and K 3 are maintained from the existing TOUGHREACT database, while the equilibrium constant for the much less abundant, heavier isotopic species (K 1 ', K 2 ', K 3 ') are determined using the appropriate equilibrium isotopic fractionation factor α eq as follows: 13 These equilibrium fractionation factors are calculated by Thode et al (1965) at 50 o C. Johnson et al (2009) reported field data of carbon isotope ratios in two carbon sequestration projects, one at Weyburn and the other at Pembina, Canada. They used the so-called gas mixture model to interpret measured isotope ratios and mole fraction of CO 2 in the gas phase.…”

Section: Model Developmentmentioning

confidence: 99%

Mineralization of carbon dioxide sequestered in volcanogenic sandstone reservoir rocks

Zhang

DePaolo

et al. 2013

International Journal of Greenhouse Gas Control

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Section: Model Developmentmentioning

confidence: 99%

Mineralization of carbon dioxide sequestered in volcanogenic sandstone reservoir rocks

Zhang

DePaolo

et al. 2013

International Journal of Greenhouse Gas Control

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“…Note that fractionation factors for freshwater are hardly comparable with those in seawater since the equilibrium constants are salinity dependent. Moreover, the high concentrations of Mg 2+ and Na + affect the speciation within the carbonate system as well as the isotopic composition of DIC by the presence of sodium and magnesium complexes of bicarbonate and carbonate (Thode et al 1965;Garrels et al 1961).…”

Section: Discussionmentioning

confidence: 99%

Using cavity ringdown spectroscopy for continuous monitoring of δ¹³C(CO₂) and ƒCO₂ in the surface ocean

Becker

Andersen

Fiedler

et al. 2012

Limnology & Ocean Methods

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The role of the global surface ocean as a source and sink for atmospheric carbon dioxide and the flux strengths between the ocean and the atmosphere can be quantified by measuring the fugacity of CO 2 (ƒCO 2 ) as well as the dissolved inorganic carbon (DIC) concentration and its isotopic composition in surface seawater. In this work, the potential of continuous wave cavity ringdown spectroscopy (cw-CRDS) for autonomous underway measurements of ƒCO 2 and the stable carbon isotope ratio of DIC [d 13 C(DIC)] is explored. For the first time, by using a conventional air-sea equilibrator setup, both quantities were continuously and simultaneously recorded during a field deployment on two research cruises following meridional transects across the Atlantic Ocean (Bremerhaven, Germany-Punta Arenas, Chile). Data are compared against reference measurements by an established underway CO 2 monitoring system and isotope ratio mass spectrometric analysis of individual water samples. Agreement within DƒCO 2 = 0.35 µatm for atmospheric and DƒCO 2 = 2.5 µatm and Dd 13 C(DIC) = 0.33‰ for seawater measurements have been achieved. Whereas "calibration-free" ƒCO 2 monitoring is feasible, the measurement of accurate isotope ratios relies on running reference standards on a daily basis. Overall, the installed CRDS/equilibrator system was shown to be capable of reliable online monitoring of ƒCO 2 , equilibrium d 13 C(CO 2 ), d 13 C(DIC), and pO 2 aboard moving research vessels, thus making possible corresponding measurements with high spatial and temporal resolution.

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“…This bias The lowest and highest estimated values of δ d , ε p are indicated assuming (1) ;SST in the Onnagawa basin was in the range of 10-20 • C; and (2) δ c value approximately 1‰ higher than the modern value (Kennett, 1986;Savin, 1989, 1991;Hodell and Vayavananda, 1994). [653.627/(T -233.45) 2 ] + 0.22) + (24.12-9866/T ) (‰); after Thode et al (1965) and Mook et al (1974).…”

Section: Origins Of 3-nor-and 8-nor-dpepmentioning

confidence: 98%

Reconstruction of the biogeochemistry and ecology of photoautotrophs based on the nitrogen and carbon isotopic compositions of vanadyl porphyrins from Miocene siliceous sediments

et al. 2008

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Abstract. We determined both the nitrogen and carbon isotopic compositions of various vanadyl alkylporphyrins isolated from siliceous marine sediments of the Onnagawa Formation (middle Miocene, northeastern Japan) to investigate the biogeochemistry and ecology of photoautotrophs living in the paleo-ocean. The distinctive isotopic signals support the interpretations of previous works that the origin of 17-nor-deoxophylloerythroetioporphyrin (DPEP) is chlorophylls-c 1−3 , whereas 8-nor-DPEP may have originated from chlorophylls-a 2 or b 2 or bacteriochlorophylla. Although DPEP and cycloheptanoDPEP are presumably derived from common precursory pigments, their isotopic compositions differed in the present study, suggesting that the latter represents a specific population within the photoautotrophic community. The average δ 15 N value for the entire photoautotrophic community is estimated to be -2 to +1‰ from the δ 15 N values of DPEP (-6.9 to -3.6‰; n=7), considering that the empirical isotopic relationships that the tetrapyrrole nuclei of chloropigments are depleted in 15 N by ∼4.8‰ and enriched in 13 C by ∼1.8‰ relative to the whole cells. This finding suggests that nitrogen utilized in the primary production was supplied mainly through N 2 -fixation by diazotrophic cyanobacteria. Based on the δ 13 C values of DPEP (-17.9 to -15.6‰; n=7), we estimated isotopic fractionation associated with photosynthetic carbon fixation to be 8-14‰. This range suggests the importance of β-carboxylation and/or active transport of Correspondence to: Y. Kashiyama (chiro@jamstec.go.jp) the carbon substrate, indicating in turn the substantial contribution of diazotrophic cyanobacteria to primary production. Based on the δ 15 N values of 17-nor-DPEP (-7.4 to -2.4‰; n=7), the δ 15 N range of chlorophylls-c-producing algae was estimated to be -3 to +3‰. This relative depletion in 15 N suggests that these algae mainly utilized nitrogen regenerated from diazotrophic cyanobacteria. Given that diatoms are likely to have constituted the chlorophylls-cproducing algae within the biogenic-silica-rich Onnagawa Formation, cyanobacteria-hosting diatoms may have been important contributors to primary production.

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Carbon-13 Isotope Effects in Systems Containing Carbon Dioxide, Bicarbonate, Carbonate, and Metal Ions

Cited by 111 publications

References 11 publications

Mineralization of carbon dioxide sequestered in volcanogenic sandstone reservoir rocks

Mineralization of carbon dioxide sequestered in volcanogenic sandstone reservoir rocks

Using cavity ringdown spectroscopy for continuous monitoring of δ¹³C(CO₂) and ƒCO₂ in the surface ocean

Reconstruction of the biogeochemistry and ecology of photoautotrophs based on the nitrogen and carbon isotopic compositions of vanadyl porphyrins from Miocene siliceous sediments

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Carbon-13 Isotope Effects in Systems Containing Carbon Dioxide, Bicarbonate, Carbonate, and Metal Ions

Cited by 111 publications

References 11 publications

Mineralization of carbon dioxide sequestered in volcanogenic sandstone reservoir rocks

Mineralization of carbon dioxide sequestered in volcanogenic sandstone reservoir rocks

Using cavity ringdown spectroscopy for continuous monitoring of δ13C(CO2) and ƒCO2 in the surface ocean

Reconstruction of the biogeochemistry and ecology of photoautotrophs based on the nitrogen and carbon isotopic compositions of vanadyl porphyrins from Miocene siliceous sediments

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Using cavity ringdown spectroscopy for continuous monitoring of δ¹³C(CO₂) and ƒCO₂ in the surface ocean