A study of sea ice dynamic events in a small bay

Wang, Keguang; Leppäranta, Matti; Kõuts, Tarmo

doi:10.1016/j.coldregions.2006.02.002

Cited by 14 publications

(12 citation statements)

References 9 publications

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“…For the compacted pack ice of uniform thickness, theoretical and laboratory studies show that P * c is basically controlled by the buckling strength [ Coon , 1974; Hopkins , 1994, 1998], while for those of various thicknesses, P * c is highly dependent on the available thin ice [e.g., Thorndike et al , 1975; Hibler , 1979, 1980; Flato and Hibler , 1995; Haapala et al , 2005]. Although there is no direct field measurement of P * c on the geophysical scale, numerically calibrated values from the dynamic simulations in the polar oceans and subpolar seas [e.g., Hibler and Walsh , 1982; Hibler and Ackley , 1983; Zhang and Leppäranta , 1995; Leppäranta et al , 1998; Zhang , 2000; Wang et al , 2003, 2006] are consistent with the in situ stress measurements [e.g., Coon et al , 1989; Tucker and Perovich , 1992; Richter‐Menge and Elder , 1998; Richter‐Menge et al , 2002], with a range of 10 to 100 kPa. The field measurement of P * t is usually more difficult, because tensile stress is often one or two orders of magnitude smaller than the thermal‐, motion‐ and tide‐induced stresses [ Tucker and Perovich , 1992; Richter‐Menge and Elder , 1998; Richter‐Menge et al , 2002].…”

Section: Resultsmentioning

confidence: 99%

Observing the yield curve of compacted pack ice

Wang

2007

J. Geophys. Res.

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[1] A method for observing the yield curve of compacted pack ice is developed based on the characteristic analysis of the stress field within the pack ice. The analysis shows that the slope of the yield curve is associated with the angle between intersecting linear kinematic features; thus by measuring the intersection angles we can inversely estimate the yield curve. Applying this method to the observed angles generates a curved diamond yield curve, which possesses almost all the advantages identified by the other methods. However, due to the limited data available, more observations are favored to refine this yield curve.

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Section: Resultsmentioning

confidence: 99%

Observing the yield curve of compacted pack ice

Wang

2007

J. Geophys. Res.

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“…This mechanism introduces an anisotropy in high-resolution simulations that is similar to observations with comparable spatial resolution. Lead characteristics, including intersection angles between LKFs, were studied a number of times (Lindsay and Rothrock, 1995;Hutchings et al, 2005;Wilchinsky et al, 2010;Bröhan and Kaleschke, 2014;Wang et al, 2016;Hutter et al, 2019). These studies show that VP models produce LKFs with various confinements, scales, resolutions, and forcings.…”

Section: Introductionmentioning

confidence: 99%

Simulating intersection angles between conjugate faults in sea ice with different viscous–plastic rheologies

et al. 2019

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Abstract. Recent high-resolution pan-Arctic sea ice simulations show fracture patterns (linear kinematic features or LKFs) that are typical of granular materials but with wider fracture angles than those observed in high-resolution satellite images. Motivated by this, ice fracture is investigated in a simple uni-axial loading test using two different viscous–plastic (VP) rheologies: one with an elliptical yield curve and a normal flow rule and one with a Coulombic yield curve and a normal flow rule that applies only to the elliptical cap. With the standard VP rheology, it is not possible to simulate fracture angles smaller than 30∘. Further, the standard VP model is not consistent with the behavior of granular material such as sea ice because (1) the fracture angle increases with ice shear strength; (2) the divergence along the fracture lines (or LKFs) is uniquely defined by the shear strength of the material with divergence for high shear strength and convergent with low shear strength; (3) the angle of fracture depends on the confining pressure with more convergence as the confining pressure increases. This behavior of the VP model is connected to the convexity of the yield curve together with use of a normal flow rule. In the Coulombic model, the angle of fracture is smaller (θ=23∘) and grossly consistent with observations. The solution, however, is unstable when the compressive stress is too large because of non-differentiable corners between the straight limbs of the Coulombic yield curve and the elliptical cap. The results suggest that, although at first sight the large-scale patterns of LKFs simulated with a VP sea ice model appear to be realistic, the elliptical yield curve with a normal flow rule is not consistent with the notion of sea ice as a pressure-sensitive and dilatant granular material.

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“…During the past 25 years there have been several developments in sea ice modelling (see Leppäranta, 2004). The models have shown good results from polar oceans down to 100 km size basins (Wang et al, 1994(Wang et al, , 2003(Wang et al, , 2006b, so it is natural to utilize this knowledge of sea ice for modelling large lakes. Here, a modern viscousplastic lake ice model is presented.…”

Section: Introductionmentioning

confidence: 98%

The ice cover on small and large lakes: scaling analysis and mathematical modelling

Leppäranta

Wang

2008

Hydrobiologia

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Lake ice cover is described by its thickness, temperature, stratigraphy and overlying snow layer. When the ratio of ice thickness to lake size is above *10 -5 , the ice cover is stable; otherwise, mechanical forcing breaks the ice cover, and ice drifting takes place with lead-opening and ridging. This transition enables a convenient distinction to be made between small and large lakes. The evolution of the ice cover on small lakes is solved by a wholly thermodynamic model, but a coupled mechanical-thermodynamic model is needed for large lakes. The latter indicates a wide distribution of ice thickness, and frazil ice may be formed in openings. Ecological conditions in large lakes differ markedly from those in small lakes because vertical mixing and oxygen renewal may take place during the ice season, and the euphotic zone penetrates well into the water column in thin ice regions. Mesoscale sea ice models are applicable to large lakes with only minor tuning of the key parameters. These model systems are presented and analysed using Lake Peipsi as an example. As the climate changes, the transition size between small and large lake ice cover will change.

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A study of sea ice dynamic events in a small bay

Cited by 14 publications

References 9 publications

Observing the yield curve of compacted pack ice

Observing the yield curve of compacted pack ice

Simulating intersection angles between conjugate faults in sea ice with different viscous–plastic rheologies

The ice cover on small and large lakes: scaling analysis and mathematical modelling

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