Heat transfer in the top millimeter of the ocean

McAlister, E. D.; McLeish, William

doi:10.1029/jc074i013p03408

Cited by 75 publications

(29 citation statements)

References 10 publications

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“…Heat transfer in the top millimeter of the ocean occurs as a combined result of turbulence, conduction, and radiation; differences in water temperature between 2-and 20-mm depth may exist ( McAlister and McLeish 1969), but are generally small ( < 1 "C ) in magnitude (Woodcock 1941) . In Jakles Lagoon the salinity of the surface microlayer may be slightly greater in summer (due to evaporation) and considerably less in winter (due to freshwater precipitation) than the subsurface water.…”

Section: Discussionmentioning

confidence: 99%

Phytoneuston Ecology of a Temperate Marine Lagoon1

Hardy

1973

Limnology & Oceanography

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Comparison of neuston (upper 0.4 cm ) and plankton ( 10 cm deep ) water samples from a temperate marine lagoon and an adjacent, less sheltered bay indicates that: 1) the surface microlayer exhibits greater and more rapid environmental fluctuations than the subsurface water; 2 ) no abundant phytoneuston populations develop outside the lagoon; 3 ) in the main lagoon fairly abundant phytoneuston populations develop; 4) phytoneuston population are most devclopcd in the shallow sheltered pond area of the lagoon, particularly in summer; 5) taxonomic diversity is generally lower and dominance greater in well-developed phytoneuston populations than in underlying phytoplankton populations; 6) photosynthetic assimilation ratios are greater in phytoneuston than in phytoplankton populations.

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Section: Discussionmentioning

confidence: 99%

Phytoneuston Ecology of a Temperate Marine Lagoon1

Hardy

1973

Limnology & Oceanography

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“…Occasionally a stable boundary layer develops where the insolation is strong and the winds are weak, but this is the exception. Since radiative and conductive transfer processes dominate over convection next to the boundary, the strongest temperature gradients are expected to occur there (e.g., McAlister and McLeish, 1969). In order to simplify discussion, we define at the outset a scaling depth, 6, for the boundary layer across which the whole temperature difference, AT, between the surface temperature, To, and the interior temperature, Tb, occurs such that molecular conduction along a linear gradient through this layer accounts for the net heat flux, QN, at the surface (see Figure 1).…”

Section: Introductionmentioning

confidence: 99%

The aqueous thermal boundary layer

Katsaros

1980

Boundary-Layer Meteorol

113

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This article reviews the available data, measurement techniques, and present understanding of the millimeter thick aqueous thermal boundary layer. A temperature difference between the surface and lower strata, AT, of the order of a few tenths to -1 "C have been observed. Techniques ranging from miniature mercury thermometers and electrical point sensors to optical interferometry and infrared radiometry have been employed. Many processes influence the temperature structure in this thin boundary layer. Among them are: the net upward heat flux due to evaporation and sensible heat transfer; infrared and solar radiation; and the turbulence near the interface due to wind mixing, wave breaking and current shear. Presence of solute and surface-active materials stimulate or dampen these mixing processes thereby influencing boundary-layer thickness and temperature structure.

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“…Because of evaporation, the temperature at the water surface, or skin, is typically less than the bulk temperature immediately below by several tenths of a degree Celsius [Donlon and Robinson, 1997;Schlüssel et al, 1990;Wick et al, 1996]. This thin, gravitationally unstable TBL is of O(10 À3 m) thick or less [Hill, 1972;McAlister and McLeish, 1969;Wu, 1971], and exists for a variety of forcing, including sheardriven [Saunders, 1967] and buoyancy-driven [Katsaros, 1977;Katsaros et al, 1977] turbulent processes. Depending on the relative amount of shear and buoyancy, vertical and horizontal structure can be complex due to the variability of the near-surface turbulence mechanisms and due to the supporting heat flux [Zappa et al, 1998].…”

Section: Passive Thermal Infrared Imagery Measurementsmentioning

confidence: 99%

Influence of rain on air‐sea gas exchange: Lessons from a model ocean

Zappa

McGillis

et al. 2004

J. Geophys. Res.

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[1] Rain has been shown to significantly enhance the rate of air-water gas exchange in fresh water environments, and the mechanism behind this enhancement has been studied in laboratory experiments. In the ocean, the effects of rain are complicated by the potential influence of density stratification at the water surface. Since it is difficult to perform controlled rain-induced gas exchange experiments in the open ocean, an SF 6 evasion experiment was conducted in the artificial ocean at Biosphere 2. The measurements show a rapid depletion of SF 6 in the surface layer due to rain enhancement of air-sea gas exchange, and the gas transfer velocity was similar to that predicted from the relationship established from freshwater laboratory experiments. However, because vertical mixing is reduced by stratification, the overall gas flux is lower than that found during freshwater experiments. Physical measurements of various properties of the ocean during the rain events further elucidate the mechanisms behind the observed response. The findings suggest that short, intense rain events accelerate gas exchange in oceanic environments.

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Heat transfer in the top millimeter of the ocean

Cited by 75 publications

References 10 publications

Phytoneuston Ecology of a Temperate Marine Lagoon1

Phytoneuston Ecology of a Temperate Marine Lagoon1

The aqueous thermal boundary layer

Influence of rain on air‐sea gas exchange: Lessons from a model ocean

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