Forecasting the structure and strength of ice on solid surfaces

Voytkovskiy, K. F.; Golubev, V. N.

doi:10.3189/s0022143000215736

Cited by 1 publication

(2 citation statements)

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“…Solute concentrations tend to be uniform within the brine pocket and, thus, with a uniform freezing point, results in supercooling and freezing at the cooler end of the pocket, and superwarming and ice melting at the warmer extreme. More explicitly, some researchers [e.g., Penner , ; Voytkovskiy and Golubev , ] determined that freezing rates of pure water and solutions are minimal when temperature is held close to the freezing point, at which the ice‐water interface is close to equilibrium, but the rates will increase, many fold, at higher extents of supercooling. Voytkovskiy and Golubev [] even suggest that the freezing rate of water is proportional to the cubic root of the extent of supercooling, which means that the freezing rate is technically zero when the ice‐water interface reaches equilibrium.…”

Section: Introductionmentioning

confidence: 99%

“…More explicitly, some researchers [e.g., Penner , ; Voytkovskiy and Golubev , ] determined that freezing rates of pure water and solutions are minimal when temperature is held close to the freezing point, at which the ice‐water interface is close to equilibrium, but the rates will increase, many fold, at higher extents of supercooling. Voytkovskiy and Golubev [] even suggest that the freezing rate of water is proportional to the cubic root of the extent of supercooling, which means that the freezing rate is technically zero when the ice‐water interface reaches equilibrium. Therefore, Spaans and Baker [] suggested that the thermodynamic equilibrium assumption of the Clapeyron equation may never be reached, or may take a very long time to establish.…”

Section: Introductionmentioning

confidence: 99%

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A numerical model for water and heat transport in freezing soils with nonequilibrium ice‐water interfaces

Peng

Huang

et al. 2016

Water Resources Research

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A one‐dimensional numerical model of heat and water transport in freezing soils is developed by assuming that ice‐water interfaces are not necessarily in equilibrium. The Clapeyron equation, which is derived from a static ice‐water interface using the thermal equilibrium theory, cannot be readily applied to a dynamic system, such as freezing soils. Therefore, we handled the redistribution of liquid water with the Richard's equation. In this application, the sink term is replaced by the freezing rate of pore water, which is proportional to the extent of supercooling and available water content for freezing by a coefficient, β. Three short‐term laboratory column simulations show reasonable agreement with observations, with standard error of simulation on water content ranging between 0.007 and 0.011 cm3 cm−3, showing improved accuracy over other models that assume equilibrium ice‐water interfaces. Simulation results suggest that when the freezing front is fixed at a specific depth, deviation of the ice‐water interface from equilibrium, at this location, will increase with time. However, this deviation tends to weaken when the freezing front slowly penetrates to a greater depth, accompanied with thinner soils of significant deviation. The coefficient, β, plays an important role in the simulation of heat and water transport. A smaller β results in a larger deviation in the ice‐water interface from equilibrium, and backward estimation of the freezing front. It also leads to an underestimation of water content in soils that were previously frozen by a rapid freezing rate, and an overestimation of water content in the rest of the soils.

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Section: Introductionmentioning

confidence: 99%