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Nathan Magee, Kayla Spector, Yi-Hsuan Lin, Corey Tong, and John Beatty

is essentially impossible to follow the growth or sublimation of individual particles in real cirrus as a balloon or aircraft probe is necessarily capturing a single snapshot of a particle at some undefined point in its lifetime. Because of these challenges, some of the most fundamental thermodynamic parameters and physical characteristics of ice particle surfaces are still highly uncertain at cirrus-relevant temperatures and pressures. Specifically, the equilibrium vapor pressure with respect to

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Atsushi Kudo

, sublimation of ice crystals in precipitation falling beneath a cloud, or cloud-base detrainment instability ( Emanuel 1981 ), may have caused convective instability (rather than dynamical shear instability) that created the vertical wind oscillations. Using high-resolution numerical simulations, Lane et al. (2003) and Lane and Sharman (2008) investigated turbulence caused by the breaking of convectively induced internal gravity waves or KH waves, above and near cumulonimbus clouds. According to Knox

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Jon Nelson

1. Background The lack of measurements of ice single crystal sublimation in air has resulted in a glaring gap in our knowledge of ice crystal response to nonequilibrium conditions. An early study of solid prismatic ice crystals sublimating in air was by Shaw and Mason (1955) . They measured the sublimation rates of the basal and prism faces of single crystals of ice attached to a substrate. Some of their crystals did not sublimate until a certain undersaturation was reached, a result probably

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Glen E. Liston and Kelly Elder

downstream water supply ( Wahl 1992 ). At each point in a landscape, the snow evolution can be described by a snow/water mass balance. Given the energies associated with melt and sublimation processes, the mass balance is intimately coupled to the energy balance. Changes in mass and energy balances govern the snow-cover distribution and evolution at each point in space and time, and include precipitation (solid and liquid), snowmelt, snow metamorphism (affecting factors such as density, thermal

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B. Kochtubajda and E. P. Lozowski

JUNE 1985 B. KOCHTUBAJDA AND E. P. LOZOWSKI 597The Sublimation of Dry Ice Pellets Used for Cloud Seeding B. KOCHTUBAJDAAlberta Research Council, Atmospheric Sciences Department, Edmonton, Alberta, Canada T6H 5R7 E. P. LOZOWSKIUniversity of Alberta, Meteorology Division, Edmonton, Alberta, Canada(Manuscript received 13 January 1984, in final form 15 December 1984

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L. C. Bowling, J. W. Pomeroy, and D. P. Lettenmaier

Colorado alpine region ( Berg 1986 ; Groisman et al. 1997 ). Déry and Yau (1999) estimate that between 10 and 60 blowing-snow events occur per year on the Alaskan North Slope. Blowing-snow events involve erosion, horizontal transport, deposition, and in-transit snow sublimation and play an important role in the spatial and temporal distribution of water and energy fluxes in many high-latitude regions. Tabler (1975a) estimated that over half of wind-transported snowfall sublimates in the high

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Richard Essery, John Pomeroy, Jason Parviainen, and Pascal Storck

atmosphere. The presence of snowcover for much of the year has a major influence on the surface energy balance and hydrology of boreal forests. Intercepted snow on a forest canopy has a large exposed surface area, and a large fraction of the annual snowfall over boreal forests in dry continental climates sublimates from the canopy without ever reaching the ground ( Schmidt and Troendle 1992 ; Pomeroy and Gray 1995 ; Lundberg and Halldin 2001 ). Snow on the ground below the canopy, however, is sheltered

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Richard Bintanja

particle in an undersaturated environment is likely to be subject to significant sublimation (e.g., Schmidt 1972 ). In fact, there is a close balance between the sensible heat flux directed toward and a latent heat flux directed away from the particle. Because the suspended particles have been eroded originally from the surface, snowdrift sublimation essentially represents a flux of moisture from the surface to the atmosphere and thereby affects the surface mass balance of snow surfaces. Snowdrift

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A. N. Gelfan, J. W. Pomeroy, and L. S. Kuchment

differences in snow characteristics for various meteorological and canopy conditions. Hedstrom and Pomeroy (1998) , Lundberg et al. (1998) , Pomeroy et al. (1998) , Nakai et al. (1999) , Ohta et al. (1999) , Suzuki et al. (1999) , Parviainen and Pomeroy (2000) , Storck et al. (2002) , and Essery et al. (2003) described how snow interception and sublimation processes influence mass and energy exchange in the canopy and reduce net precipitation under forest canopies. Snow redistribution by wind in

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James Montesi, Kelly Elder, R. A. Schmidt, and Robert E. Davis

1. Introduction Sublimation from snow occurs when water vapor gradients form near ice crystal surfaces, usually at subfreezing temperatures ( Schmidt 1972 ). Vapor pressure gradients form when the water vapor pressure of the atmosphere is different from that near the ice surface. Snow sublimation rate can be defined as the amount of mass lost per unit time. Sublimation rates depend on particle surface area to mass ratio, vapor pressure gradients, and rate of air exchange around the snow crystal

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