Thus, for every 1 % increase in local sea level, there is a ~ 5 % increase
in ice flux through the grounding line (though this may be higher if the bed is slippery near the grounding line, see Tsai et al. 2015).
InSAR observations from 1992 to 2006 mapped the ice flow for most of the Antarctic coastline, and detected different patterns
of ice flux into the ocean in East and West Antarctica.
Kwok, R., and D.A. Rothrock, 1999: Variability of Fram
Strait ice flux and North Atlantic Oscillation.
Stable grounding lines can not be established on these reverse bed slopes1, because ice thickness is a key factor in
controlling ice flux across the grounding line.
If I may add one more speculative question: are the portions of glacial sheets formed during periods of
high ice flux less stable, and more prone to calving, than those formed during slow flux?
However, the use of a physically based lightning parameterization — incorporating
cloud ice fluxes — reveals global flash rates in 2100 may decrease by 15 % under RCP8.5.
We can observe the gyre in the Beaufort Sea, offshore of the Canadian and Alaskan coasts as well as
the ice flux leaving the Arctic Ocean through the Fram Straight, between Greenland and the Svalbard archipelago.
The mass balance at the calving front is the sum of
the ice flux from upglacier, the rate of melting above and below the waterline and the iceberg - calving rate.