Measurements of bubble plumes and turbulence from a submarine

Osborn, Thomas R.; Farmer, David M.; Vagle, Svein; Thorpe, S. A.; Cure, M.

doi:10.1080/07055900.1992.9649447

Cited by 90 publications

(37 citation statements)

References 16 publications

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“…Huang and Qiao (2010) compared Eq. (6) with observations by Anis and Moum (1995), Osborn et al (1992) and Wüest et al (2000) with an order of magnitude agreement for values of β between 0.15 and 1. Studies are ongoing in this field (Stevens and Smith, 2004;Gerbi et al, 2009) and it is still unclear on the role surface waves play in dissipation (Babanin and Haus, 2009;Huang and Qiao, 2010;Teixeira, 2012).…”

Section: Introductionsupporting

confidence: 81%

Wave-turbulence scaling in the ocean mixed layer

2013

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Abstract. Microstructure measurements were collected using an autonomous freely rising profiler under a variety of different atmospheric forcing and sea states in the open ocean. Here, profiles of turbulent kinetic energy dissipation rate, , are compared with various proposed scalings. In the oceanic boundary layer, the depth dependence of was found to be largely consistent with that expected for a shear-driven wall layer. This is in contrast with many recent studies which suggest higher rates of turbulent kinetic energy dissipation in the near surface of the ocean. However, some dissipation profiles appeared to scale with the sum of the wind and swell generated Stokes shear with this scaling extending beyond the mixed layer depth. Integrating in the mixed layer yielded results that 1 % of the wind power referenced to 10 m is being dissipated here.

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Section: Introductionsupporting

confidence: 81%

Wave-turbulence scaling in the ocean mixed layer

2013

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“…Therefore, this question must be addressed as a function of scale, whether it be body size, volume of the flow field generated by the swimming and feeding organism, or a characteristic length scale determined by the swimming pattern. Turbulent energy dissipation at the ocean surface ranges from 10 -5 to 10 -4 W kg -1 , decreasing with increasing depth to about 10 -6 W kg -1 within 10 m (Yamazaki & Kamykowski 1991, Osborn et al 1992) and to about 10 -7 to 10 -10 W kg -1 in the stratified depths of the ocean (Gargett 1989). Yamazaki & Squires (1996) used the Ozmidov scale to relate the turbulence energy spectrum to the root mean square (rms) turbulence velocity.…”

mentioning

confidence: 99%

Contribution of fine-scale vertical structure and swimming behavior to formation of plankton layers on Georges Bank

Gallager¹,

Yamazaki²,

Davis³

2004

Mar. Ecol. Prog. Ser.

104

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The roles of plankton behavior, stratification, and microstructure in the formation of fine-scale plankton layers were examined using a 3-dimensional video plankton recorder mounted on a remotely operated vehicle. Vertically compressed plankton patches were observed in association with a cold pool over the Southern Flank of Georges Bank, extending from the tidal mixing front to the shelf-slope break during the months of May and June, 1994, 1995, 1997. In June 1995, 3 major plankton layers were present: a 10 m thick layer above the thermocline, a 1 m thick layer within the thermocline, and a third, 2 to 5 m thick layer immediately below the thermocline. Energy dissipation rate was lowest in the central layer and increased in both top and bottom layers. Some passive organisms and particles, e.g. the colonial diatom Chaetoceros socialis and rod-shaped diatoms, were concentrated in all 3 layers, while marine snow particles were found only in transitional regions. All stages of Calanus spp. were present in high numbers on the fringes of all 3 layers, while Oithona sp. was found only in the thin, central layer. Plankton were significantly aggregated only when the motility number, Mn (i.e. ratio of plankton swimming speed/rms turbulent velocity) was greater than 3, suggesting dominance of plankton behavior over physical structure. Under both quiescent and turbulent conditions, the Lagrangian frequency spectra (f ) for swimming plankton and passive particles decreased with a slope of f -2 . However, in quiescent conditions, the magnitude of the spectrum for swimming plankton was 10-fold greater than for passive particles, illustrating a decoupling of plankton swimming from turbulent eddies. The air/water interface, the pycnocline, and multiple shear interfaces at density discontinuities act as boundaries to vertical zones where plankton behavior may succumb to or dominate background microstructure, thus providing a mechanism for formation of plankton and particulate layers.KEY WORDS: Fine-scale vertical structure · Thin layers · Plankton behavior · Turbulence Resale or republication not permitted without written consent of the publisherMar Ecol Prog Ser 267: [27][28][29][30][31][32][33][34][35][36][37][38][39][40][41][42][43] 2004 communities, species-specific patterns in abundance can form as a function of fine-scale physical structure (Owen 1989, Davis et al. 1992, Gallager et al. 1996b and may persist for many days (Donaghay et al. 1992, Cowles & Desiderio 1993, reviewed in Cowles et al. 1998. If this scale is undersampled or, worse, ignored, the result of persistent fine-scale structure will be gross underestimates of production (Cowles et al. 1998).Vertical fine-structure has been observed since the study of Eckart (1948), and is usually described in terms of mixing, such as the interaction between density stratification and horizontal shear (Gargett et al. 1984). One of the net results of shear is to redistribute horizontal variance onto vertical variance, producing the typical multiple-layer effect,...

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“…The experimental data needed in these studies are not easy to obtain (see Terray et al (1996) and Soloviev et al (2007) for a review), but the limited data shows that in the presence of breaking waves the dissipation values are higher than given by the sheardriven wall layer approach (e.g. Agrawal et al 1992;Osborne et al 1992;Anis and Moum 1995;Drennan et al 1996;Terray et al 1996;Phillips et al 2001;Zappa et al 2007). Anis and Moum (1995) measured high dissipation rates at depths greater than the height of the breaking waves and suggested that the orbital motions of swell could be one possible mechanism that transports the wave induced turbulence to deeper depths.…”

Section: Wind-generated Wavesmentioning

confidence: 99%

Transfer Across the Air-Sea Interface

Garbe

Rutgersson

Boutin

et al. 2013

Springer Earth System Sciences

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The efficiency of transfer of gases and particles across the air-sea interface is controlled by several physical, biological and chemical processes in the atmosphere and water which are described here (including waves, large-and small-scale turbulence, bubbles, sea spray, rain and surface films). For a deeper understanding of relevant transport mechanisms, several models have been developed, ranging from conceptual models to numerical models. Most frequently the transfer is described by various functional dependencies of the wind speed, but more detailed descriptions need additional information. The study of gas transfer mechanisms uses a variety of experimental methods ranging from laboratory studies to carbon budgets, mass balance methods, micrometeorological techniques and thermographic techniques. Different methods resolve the transfer at different scales of time and space; this is important to take into account when comparing different results. Air-sea transfer is relevant in a wide range of applications, for example, local and regional fluxes, global models, remote sensing and computations of global inventories. The sensitivity of global models to the description of transfer velocity is limited; it is however likely that the formulations are more important when the resolution increases and other processes in models are improved. For global flux estimates using inventories or remote sensing products the accuracy of the transfer formulation as well as the accuracy of the wind field is crucial. IntroductionThe transfer of gases and particles across the air-sea interface depends not only on the concentration difference between the water and the air, but also on the efficiency of the transfer process. The efficiency of the transfer is controlled by complex interaction of a variety of processes in the air and in the water near the interface. Here we treat both gases and particles since the transfer, to some extent, is governed by similar mechanisms. Studies of transfer across the air-sea interface include a variety of methods and techniques ranging from laboratory studies, modeling and large-scale field studies. Various methods reach somewhat different conclusions, due to representation of different

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Measurements of bubble plumes and turbulence from a submarine

Cited by 90 publications

References 16 publications

Wave-turbulence scaling in the ocean mixed layer

Wave-turbulence scaling in the ocean mixed layer

Contribution of fine-scale vertical structure and swimming behavior to formation of plankton layers on Georges Bank

Transfer Across the Air-Sea Interface

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