The linked reference by Hughes et al (2015) presents state-of-the-art analysis about the Jakobshavn Effect (Hughes, 1986), focused on progressive ice-bed uncoupling due to such factors as: basal meltwater, buoyancy friction (particularly with changing surface elevation), boundary constraints of the fjord. This work has relevance to multiple marine-terminating, and marine, glaciers in both Greenland and Antarctica (see the extract for concerns about the PIG an the Thwaites Glacier, among other Antarctic marine glaciers):
Hughes, T., Sargent, A., Fastook, J., Purdon, K., Li, J., Yan, J.-B., and Gogineni, S.: Sheet, stream, and shelf flow as progressive ice-bed uncoupling: Byrd Glacier, Antarctica, and Jakobshavn Isbrae, Greenland, The Cryosphere Discuss., 9, 4271-4354, doi:10.5194/tcd-9-4271-2015, 2015.
http://www.the-cryosphere-discuss.net/9/4271/2015/tcd-9-4271-2015.pdfAbstract. The first-order control of ice thickness and height above sea level is linked to the decreasing strength of ice-bed coupling alone flowlines from an interior ice divide to the calving front of an ice shelf. Uncoupling progresses as a frozen bed progressively thaws for sheet flow, as a thawed bed is progressively drowned for stream flow, and as lateral and/or local grounding vanish for shelf flow. This can reduce ice thicknesses by 90 % and ice elevations by 99 % along flowlines. Original work presented here includes (1) replacing flow and sliding laws for sheet flow with upper and lower yield stresses for creep in cold overlying ice and basal ice sliding over deforming till, respectively, (2) replacing integrating the Navier–Stokes equations for stream flow with geometrical solutions to the force balance, and (3) including resistance to shelf flow caused by lateral confinement in a fjord and local grounding at ice rumples and ice rises. A comparison is made between our approach and two approaches based on continuum mechanics. Applications are made to Byrd Glacier in Antarctica and Jakobshavn Isbrae in Greenland.
Extract: "Equation (24), based only on the force balance, is especially useful here because of its robust simplicity that applies to all flowlines and flowbands (ice streams) that end at a specified ice thickness h0. It gives phi variations along x that are usually somewhat higher than when the mass balance is also included, but with the same general trend. Using Eq. (24), Pingree et al. (2011) showed how Eq. (24) produced ice elevations before and after a former surge lifecycle of Lambert Glacier in East Antarctica, and for impending surge lifecycles of Thwaites Glacier and Pine Island Glacier entering the Pine Island Bay polynya in West Antarctica that continue into East Antarctica. Using Eq. (24), Hughes (2011) has tentatively assigned inception, growth, mature, declining, and terminal lifecycle stages shown in Table 2 to all major Antarctic ice streams at the present time."
Edit: See the two attached associated images related to the Jakobshavn Effect; which elsewhere in this fold I have associated with the more dynamic "Thwaites Effect"