Diffusion of Dissolved Gases in Liquids

Himmelblau, D. M.

doi:10.1021/cr60231a002

Cited by 461 publications

(217 citation statements)

References 52 publications

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“…These diffusivities were computed from data of Davidson and Cullen (1957) at 15", 20", and 25°C by extrapolation of the linear log D vs. l/T plots using the Arrhenius equation. The ratio of exchange constants is equal to the ratio of cliffusivities within the limits of error in either quantity ( Himmelblau 1964). In correspondence to a trough-to-crest variation in pH from 7.8 to 8.6 total carbonate changed from 1.571 to 1.492 x 10-3, or a change of 7.9 x 1O-S M, while dissolved oxygen changed by about 2.7 mg liter-l or 8.4 x lo-" M 02 during the same day.…”

Section: Ph C02 and Photosynthesismentioning

confidence: 99%

Dynamics of O₂ and CO₂ exchange, photosynthesis, and respiration in rivers from time‐delayed correlations with ideal sunlight

Schurr

Ruchti

1977

Limnology & Oceanography

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The oxygen exchange constant, photosynthetic rate, and respiration rate for several Swiss rivers have been determined using only the continuous data record of a single oxygen electrode, the measured tcmpcrature, and an assumed ideal light intensity curve in conjunction with a simple model rate equation and a novel cross-correlation computational technique. The method can, in favorable circumstances, be extended to determine also total carbonate dynamics from continuous pH measurements.For the Aare at Bern in March 1974, the oxygen exchange constant was 0.38 h-l, the respiration rate was 0.6 mg liter-' h-l, and mean photosynthetic rate was 0.28 mg liter-l h-l. The exchange rate for dissolved (but not hydrated or ionized) COti was 0.91 times that for dissolved oxygen. and the ratio of 02 molecules released to COP molecules consumed during photosynthesis was about 1.2.

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Section: Ph C02 and Photosynthesismentioning

confidence: 99%

Dynamics of O₂ and CO₂ exchange, photosynthesis, and respiration in rivers from time‐delayed correlations with ideal sunlight

Schurr

Ruchti

1977

Limnology & Oceanography

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“…The difisivity of gases in liquids decreases with increasing salinity as demonstrated by the results quoted by Himmelblau (1964). Thus for CO*, diffusivity decreases from 1.92 x 1O-5 cm2 s-l in freshwater to 1.30 x 1O-5 cm* s-' at a NaCl concentration of 3.78 mol liter-'.…”

Section: Gas Exchange With Saline Watersmentioning

confidence: 68%

Gas exchange with saline waters

Gat

Shatkay

1991

Limnology & Oceanography

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The salt effect on the gas exchange rate is a combination of an effect on solubility, which is considerably lower in the saline solution, and on piston velocity. These effects reinforce each other to reduce gas influx rates by as much as one order of magnitude in the case of a brine as salty as the Dead Sea, whereas the effect on the rate of escape of gas is smaller. At high wind‐speeds, when bubble entrainment becomes the dominant mode of gas transport, several opposing salt effects come into play that depend not only on the salt concentration but also on the nature of the salt. Even though gas exchange is more sluggish in the saline solution, the higher persistence of bubbles and foams under saline conditions may result in a higher degree of aeration of a brine as a result of a storm surge, when compared to a similar event in a freshwater system.

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“…The values used for D W,CO2 were those corresponding to the closest 5° incremental temperature to the in situ water temperature at the time the sample was taken (Himmelblau 1964;Jahne et al 1987;Oelkers 1991;Schwarzenbach et al 2003) (S4). Values used for Sc W,CO2 were those corresponding to saltwater at the closest 1° incremental temperature to the in situ water temperature (Matson and Harriss 1995).…”

Section: Calculating Voc Fluxmentioning

confidence: 99%

Improved method for quantifying the air‐sea flux of volatile and semi‐volatile organic carbon

Hauser

Dickhut

Falconer

et al. 2013

Limnology & Ocean Methods

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Understanding the global cycling of bioelements, such as carbon, requires linking their transport vectors and pools in atmospheric, aquatic, and terrestrial systems. Quantifying carbon movement through the oceanic system is critical for a complete picture of the global carbon budget. Given the variability in metabolic balance within and between marine and coastal aquatic ecosystems (Caffrey et al. 1998;del Giorgio and Duarte 2002;Gupta et al. 2009;Kemp et al. 1997;Raymond et al. 2000), lateral transport of carbon could be the key to reconciling gaps in carbon budgets. One possible transport vector that has not been thoroughly investigated is organic carbon transfer between surface waters and the atmosphere.There is currently no universally accepted method for quantifying the diffusive air-sea flux of OC. Previous studies have mainly measured only a few compounds and have used atmospheric gas phase OC (GOC) quantification techniques such as direct trapping followed by chromatographic analysis Chuck et al. 2005;Singh et al. 2003 AbstractA method for quantifying the diffusive air-sea exchange of gaseous organic carbon (OC) was developed. OC compounds were separated into two operational pools-those that were kinetically air limited in diffusion across the air-sea interface and those that were water limited-during simultaneous air/water sampling. The method separates OC compounds into low Henry's law constant (low-H) semivolatile OC (SOC) and high Henry's law constant (high-H) volatile OC (VOC) pools that can be categorized by relating diffusion kinetic parameters to Henry's Law constant. Air limited (low-H; H << ~0.1 L atm mol -1 ) compounds were collected in pure water traps and were quantified as dissolved OC, whereas water limited (high-H; H >> ~0.1 L atm mol -1 ) compounds were collected on solid sorbent tubes downstream from the water traps and were analyzed by gas chromatography-flame ionization detection (GC-FID). Separating OC based on H, rather than measuring OC as one bulk pool, allows improved estimates of OC concentration gradients and fluxes. A 10-month field study in the York River Estuary in Gloucester Point, VA revealed an average VOC flux of 138 µg C m -2 d -1 and an average SOC flux of 832 mg C m -2 d -1 (positive fluxes denote sea to air transfer).

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Diffusion of Dissolved Gases in Liquids

Cited by 461 publications

References 52 publications

Dynamics of O₂ and CO₂ exchange, photosynthesis, and respiration in rivers from time‐delayed correlations with ideal sunlight

Dynamics of O₂ and CO₂ exchange, photosynthesis, and respiration in rivers from time‐delayed correlations with ideal sunlight

Gas exchange with saline waters

Improved method for quantifying the air‐sea flux of volatile and semi‐volatile organic carbon

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Diffusion of Dissolved Gases in Liquids

Cited by 461 publications

References 52 publications

Dynamics of O2 and CO2 exchange, photosynthesis, and respiration in rivers from time‐delayed correlations with ideal sunlight

Dynamics of O2 and CO2 exchange, photosynthesis, and respiration in rivers from time‐delayed correlations with ideal sunlight

Gas exchange with saline waters

Improved method for quantifying the air‐sea flux of volatile and semi‐volatile organic carbon

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Dynamics of O₂ and CO₂ exchange, photosynthesis, and respiration in rivers from time‐delayed correlations with ideal sunlight

Dynamics of O₂ and CO₂ exchange, photosynthesis, and respiration in rivers from time‐delayed correlations with ideal sunlight