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convection over open ocean to drive convection and deep convective clouds, the longwave (LW) radiative effect of which suppresses sea ice growth. Interestingly, we find here that downward LW radiation plays a significant role in affecting the abruptness of winter sea ice loss, but that while wintertime Arctic atmospheric convection indeed occurs in all models examined at high enough CO 2 , the LW cloud radiative effect does not seem to be a major player. Bathiany et al. (2016) looked closely at the
convection over open ocean to drive convection and deep convective clouds, the longwave (LW) radiative effect of which suppresses sea ice growth. Interestingly, we find here that downward LW radiation plays a significant role in affecting the abruptness of winter sea ice loss, but that while wintertime Arctic atmospheric convection indeed occurs in all models examined at high enough CO 2 , the LW cloud radiative effect does not seem to be a major player. Bathiany et al. (2016) looked closely at the
paper presents a verification study of the skill and potential economic value of deterministic forecasts of ice growth (also, active icing ; Bredesen et al. 2017b ). The phase of active ice accumulation on blades has been associated with the strongest production losses (e.g., Bernstein et al. 2012 ; Bergström et al. 2013 ); it is also the sensitive phase during which preventive anti-icing can make a difference. Icing forecasts for the range up to day 3 are produced from global and limited
paper presents a verification study of the skill and potential economic value of deterministic forecasts of ice growth (also, active icing ; Bredesen et al. 2017b ). The phase of active ice accumulation on blades has been associated with the strongest production losses (e.g., Bernstein et al. 2012 ; Bergström et al. 2013 ); it is also the sensitive phase during which preventive anti-icing can make a difference. Icing forecasts for the range up to day 3 are produced from global and limited
ice volume in all seasons. The 〈 ω io 〉 and 〈 θ io 〉 terms peak in late autumn and early winter, because during this period the sea ice growth rate stays at a high level leaving dense (saline) surface water behind. The dense surface water leads to increased vertical convection and upward oceanic turbulent heat flux yielding more basal ice melt. Note that the enhanced sea ice area and volume losses during 6–10 August are caused by the so-called Great Arctic Cyclone of August 2012, which enhanced
ice volume in all seasons. The 〈 ω io 〉 and 〈 θ io 〉 terms peak in late autumn and early winter, because during this period the sea ice growth rate stays at a high level leaving dense (saline) surface water behind. The dense surface water leads to increased vertical convection and upward oceanic turbulent heat flux yielding more basal ice melt. Note that the enhanced sea ice area and volume losses during 6–10 August are caused by the so-called Great Arctic Cyclone of August 2012, which enhanced
1. Introduction The process of aggregation, or the collection of one or more ice crystals, deemed snow in this study, is a critical component in ice-microphysical parameterizations within cloud-resolving models due to the inherent size and mass of aggregates. A diverse range of sizes and shapes (habits) form in nature based on environmental growth conditions and advective transport strength, which leads to varied sedimentation velocities and easily attained precipitation-sized particles
1. Introduction The process of aggregation, or the collection of one or more ice crystals, deemed snow in this study, is a critical component in ice-microphysical parameterizations within cloud-resolving models due to the inherent size and mass of aggregates. A diverse range of sizes and shapes (habits) form in nature based on environmental growth conditions and advective transport strength, which leads to varied sedimentation velocities and easily attained precipitation-sized particles
highlights the relationship between RH w and RH ice as a function of temperature. As air temperature decreases, the RH w needed to sustain an ice cloud shrinks as well. This is in contrast to the requirement that RH w ≥ 100% for liquid-phase and mixed-phase clouds. Ice supersaturation directly relates to ice growth through deposition, which can only occur above saturation with respect to ice, and ice loss through sublimation, which occurs when conditions are subsaturated with respect to ice
highlights the relationship between RH w and RH ice as a function of temperature. As air temperature decreases, the RH w needed to sustain an ice cloud shrinks as well. This is in contrast to the requirement that RH w ≥ 100% for liquid-phase and mixed-phase clouds. Ice supersaturation directly relates to ice growth through deposition, which can only occur above saturation with respect to ice, and ice loss through sublimation, which occurs when conditions are subsaturated with respect to ice
1. Introduction Vapor depositional growth is largely responsible for the variety of shapes (or habits) of ice crystals found in atmospheric cold clouds. The crystal sizes, shapes, and surface properties that result from vapor growth can have strong impacts on numerical cloud model simulations of ice-containing clouds ( Gierens et al. 2003 ; Woods et al. 2007 ; Avramov and Harrington 2010 ), on the optical properties of cloud systems ( Mitchell et al. 1996 ; Järvinen et al. 2018 ; van
1. Introduction Vapor depositional growth is largely responsible for the variety of shapes (or habits) of ice crystals found in atmospheric cold clouds. The crystal sizes, shapes, and surface properties that result from vapor growth can have strong impacts on numerical cloud model simulations of ice-containing clouds ( Gierens et al. 2003 ; Woods et al. 2007 ; Avramov and Harrington 2010 ), on the optical properties of cloud systems ( Mitchell et al. 1996 ; Järvinen et al. 2018 ; van
( D. S. Park et al. 2015 ; Woods and Caballero 2016 ). Below, we will indicate that changes in the moisture flux convergence, total column water (TCW; liquid water plus ice), and associated downward IR over the BKS depend strongly on the evolution (growth and decay) of the UB pattern from a daily perspective. In particular, it is demonstrated that the intensified UB occurs together with enhanced positive SAT anomaly, downward IR, TCW, and moisture flux convergence over the BKS and its adjacent
( D. S. Park et al. 2015 ; Woods and Caballero 2016 ). Below, we will indicate that changes in the moisture flux convergence, total column water (TCW; liquid water plus ice), and associated downward IR over the BKS depend strongly on the evolution (growth and decay) of the UB pattern from a daily perspective. In particular, it is demonstrated that the intensified UB occurs together with enhanced positive SAT anomaly, downward IR, TCW, and moisture flux convergence over the BKS and its adjacent
the Arctic sea ice is still active from autumn to early winter, so the sea ice could be another potential factor affecting the subseasonal variation of the WACE and CAWE pattern. A recent observational study by Jiang et al. (2021) suggested that air–ice interaction in the Barents–Kara Sea is dominated by the sea ice driving effect when the anomalous turbulent heat flux is upward following the sea ice loss. In this study, we aim to 1) quantify the contributions of different dynamical and thermal
the Arctic sea ice is still active from autumn to early winter, so the sea ice could be another potential factor affecting the subseasonal variation of the WACE and CAWE pattern. A recent observational study by Jiang et al. (2021) suggested that air–ice interaction in the Barents–Kara Sea is dominated by the sea ice driving effect when the anomalous turbulent heat flux is upward following the sea ice loss. In this study, we aim to 1) quantify the contributions of different dynamical and thermal
be enhanced somehow by high positive supersaturations with respect to water (e.g., Fukuta and Schaller 1982 ). Such supersaturations can occur transiently in the vicinity or wakes of falling freezing drops or graupel/hail in wet growth, the surfaces of which remain close to 0°C, much warmer than the ambient air, enhancing ice production (e.g., Gagin 1972 ; Gagin and Nozyce 1984 ; Prabhakaran et al. 2020 ). However, it is unclear whether orders of magnitude of enhancement could be produced by
be enhanced somehow by high positive supersaturations with respect to water (e.g., Fukuta and Schaller 1982 ). Such supersaturations can occur transiently in the vicinity or wakes of falling freezing drops or graupel/hail in wet growth, the surfaces of which remain close to 0°C, much warmer than the ambient air, enhancing ice production (e.g., Gagin 1972 ; Gagin and Nozyce 1984 ; Prabhakaran et al. 2020 ). However, it is unclear whether orders of magnitude of enhancement could be produced by
). Here, iceberg calving and underwater melting processes are combined into a single parameter termed marine ice loss ( L M ). A semiempirical parameterization of L M as a function of runoff ( R ) enables total ice sheet mass budget closure. Rignot et al. (2008) parameterized L M in terms of a linear function of surface mass balance (SMB). Here, that relation is revisited using updated L M data beginning in 1992 ( Rignot et al. 2011 ). Surface mass balance and runoff data are after Box et al
). Here, iceberg calving and underwater melting processes are combined into a single parameter termed marine ice loss ( L M ). A semiempirical parameterization of L M as a function of runoff ( R ) enables total ice sheet mass budget closure. Rignot et al. (2008) parameterized L M in terms of a linear function of surface mass balance (SMB). Here, that relation is revisited using updated L M data beginning in 1992 ( Rignot et al. 2011 ). Surface mass balance and runoff data are after Box et al
