Propagation of surface waves on irregular bed topography

A. S. Warke; S. K. Das; L. Debnath

doi:10.1007/bf02831933

Propagation of surface waves on irregular bed topography

Journal of Applied Mathematics and Computing ◽

10.1007/bf02831933 ◽

2006 ◽

Vol 20 (1-2) ◽

pp. 197-208 ◽

Cited By ~ 2

Author(s):

A. S. Warke ◽

S. K. Das ◽

L. Debnath

Keyword(s):

Surface Waves ◽

Bed Topography ◽

Irregular Bed Topography

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A well-balanced upstream flux-splitting finite-volume scheme for shallow-water flow simulations with irregular bed topography

International Journal for Numerical Methods in Fluids ◽

10.1002/fld.2048 ◽

2009 ◽

pp. n/a-n/a ◽

Cited By ~ 3

Author(s):

Jihn-Sung Lai ◽

Wen-Dar Guo ◽

Gwo-Fong Lin ◽

Yih-Chi Tan

Keyword(s):

Shallow Water ◽

Water Flow ◽

Finite Volume ◽

Finite Volume Scheme ◽

Shallow Water Flow ◽

Flow Simulations ◽

Volume Scheme ◽

Bed Topography ◽

Flux Splitting ◽

Irregular Bed Topography

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Surface “waves” on Byrd Glacier, Antarctica

Antarctic Science ◽

10.1017/s0954102003001664 ◽

2003 ◽

Vol 15 (4) ◽

pp. 547-555 ◽

Cited By ~ 15

Author(s):

D. REUSCH ◽

T. HUGHES

Keyword(s):

Surface Waves ◽

Wave Train ◽

Water Pressure ◽

Force Balance ◽

Surface Slope ◽

Ice Shelf ◽

Overburden Pressure ◽

Ross Ice Shelf ◽

Bed Topography ◽

Catchment Areas

Byrd Glacier has one of the largest ice catchment areas in Antarctica, delivers more ice to the Ross Ice Shelf than any other ice stream, and is the fastest of these ice streams. A force balance, combined with a mass balance, demonstrates that stream flow in Byrd Glacier is transitional from sheet flow in East Antarctica to shelf flow in the Ross Ice Shelf. The longitudinal pulling stress, calculated along an ice flowband from the force balance, is linked to variations of ice thickness, to the ratio of the basal water pressure to the ice overburden pressure where Byrd Glacier is grounded, and is reduced by an ice-shelf buttressing stress where Byrd Glacier is floating. Longitudinal tension peaks at pressure-ratio maxima in grounded ice and close to minima in the ratio of the pulling stress to the buttressing stress in floating ice. The longitudinal spacing of these tension peaks is rather uniform and, for grounded ice, the peaks occur at maxima in surface slope that have no clear relation to the bed slope. This implies that the maxima in surface slope constitute a “wave train” that is related to regular variations in ice-bed coupling, not primarily to bed topography. It is unclear whether these surface “waves” are “standing waves” or are migrating either upslope or downslope, possibly causing the grounding line to either retreat or advance. Deciding which is the case will require obtaining bed topography in the map plane, a new map of surface topography, and more sophisticated modeling that includes ice flow linked to subglacial hydrology in the map plane.

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