Lidar detection of leads in Arctic sea ice

Schnell, R. C.; Barry, Roger G.; Miles, Martin W.; Andreas, Edgar L.; Radke, Lawrence F.; Brock, C. A.; McCormick, M. P.; Moore, John L.

doi:10.1038/339530a0

Cited by 93 publications

(52 citation statements)

References 12 publications

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“…Nevertheless, the effective surface heat transfer coefficient over the lead is 7.9 x 10 -3, close to the 2.4 x 10 -3 value predicted by the observational fit of Andreas and Murphy (1986). We also note that the depth of the IBL at the downwind edge of the lead is around 20 m. in rough agreement with the 15 m value predicted for a lead by the formula of Schnell et al (1989). At the surface.…”

Section: G Mean Turbulent Temperature Fluxsupporting

confidence: 70%

Turbulent transport from an arctic lead: A large-eddy simulation

Glendening

Burk

1992

Boundary-Layer Meteorol

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Section: G Mean Turbulent Temperature Fluxsupporting

confidence: 70%

Turbulent transport from an arctic lead: A large-eddy simulation

Glendening

Burk

1992

Boundary-Layer Meteorol

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“…Large heat fluxes for individual leads were observed in the lowest 30 m [54]. The vertical extent of plumes above leads depends on the thermal structure of the atmosphere, with stable stratifications prohibiting the development of large plumes above leads, and neutral stratification, e.g., after a front, allowing deeper plume penetration [22,47].…”

Section: Meteorologymentioning

confidence: 99%

The Spring-Time Boundary Layer in the Central Arctic Observed during PAMARCMiP 2009

et al. 2012

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Abstract:The Arctic atmospheric boundary layer (AABL) in the central Arctic was characterized by dropsonde, lidar, ice thickness and airborne in situ measurements during Above sea ice, a low AABL top, low near-surface temperatures, strong surface-based temperature inversions and an increase of moisture with altitude were observed. AABL properties and particle concentrations were modified by a frontal system, allowing vertical mixing with the free atmosphere. Above areas with many leads, the potential temperature decreased with height in the lowest 50 m and was nearly constant above, up to an altitude of 100-200 m, indicating vertical mixing. The increase of the backscatter coefficient towards the surface was high. Above sea ice with few refrozen leads, the stably stratified boundary layer extended up to 200-300 m altitude. It was characterized by low specific humidity and a smaller increase of the backscatter coefficient towards the surface.

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“…The evolution downstream of the boundary layer and clouds associated with wide leads and polynyas is, however, fundamentally different from the cold air outbreak schematized by Agee [1987]. In contrast to the cold air outbreaks, there is only a limited fetch over the open water associated with leads and polynyas, so downwind the boundary layer becomes stable, although a cloud plume is often evident downwind for more than 100 km of wide leads and polynyas [e.g., Schnell et al, 1989;Curry et al, 1997Curry et al, , 2000.…”

Section: Introductionmentioning

confidence: 99%

A springtime cloud over the Beaufort Sea polynya: Three‐dimensional simulation with explicit spectral microphysics and comparison with observations

Khvorostyanov

Curry

Gültepe³

et al. 2003

J. Geophys. Res.

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[1] This paper addresses the formation of a cloud system associated with an arctic polynya in Beaufort Sea during springtime. Data were obtained as a part of the First International Satellite Cloud Climatology Project (ISCCP) Regional Experiment (FIRE) Arctic Clouds Experiment from the Canadian Convair 580 aircraft during 25 April 1998. These data include in situ observations of cloud microphysics and meteorological variables and remote measurements from satellite and airborne lidar. A three-dimensional cloud-resolving model with explicit bin-resolving cloud microphysics is used to simulate the atmospheric boundary layer and cloud evolution associated with the polynya. After initialization with the aircraft sounding profiles, a quasi-steady polynya-induced atmospheric boundary layer (ABL) and a cloud system form. Strong turbulence in the ABL occurs above the polynya, the internal thermal boundary layer (ITBL) develops and grows upward in the downwind direction, and the ABL downwind of the polynya is separated into two decoupled layers. The cloud forms in the middle of the polynya, and its upper boundary lifts downwind while the lower boundary lowers and reaches the surface beyond the polynya southern boundary as a light fog. Farther to the south, the fog evaporates and transforms into an elevated cloud plume that extends for several tens of kilometers downwind. This cloud morphology is in good agreement with the lidar observations, which showed a cloud layer extending for more than 100 km downwind, and with the numerous previous observations. The simulated microphysical properties of a mixed cloud are similar to those observed. A new ice nucleation scheme resulted in cloud plume gradual crystallization along the wind and eventual transformation into diamond dust. Detailed evaluation of the water budget, supersaturation, and crystal size spectra showed that the ice crystal supersaturation relaxation times are 10-60 min; thus deposition on the crystals is rather slow, and only 1-5% of the available vapor is deposited on the crystals. The large ice crystal supersaturation relaxation time explains the relatively slow growth and gravitational fallout of the ice crystals, as well as the extensive propagation downwind of the plume.

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Lidar detection of leads in Arctic sea ice

Cited by 93 publications

References 12 publications

Turbulent transport from an arctic lead: A large-eddy simulation

Turbulent transport from an arctic lead: A large-eddy simulation

The Spring-Time Boundary Layer in the Central Arctic Observed during PAMARCMiP 2009

A springtime cloud over the Beaufort Sea polynya: Three‐dimensional simulation with explicit spectral microphysics and comparison with observations

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