Miller, G.H., Bradley, R.S. and Andrews, J.T., 1975: The glaciation level and
lowest equilibrium line altitude in the High Canadian Arctic: maps and climatic interpretation.
Not exact matches
How about this brutally simplified calculation for a
lower bound of
equilibrium temperature sensitivity: — there seems to be a consensus that transient t.s. <
equilibrium t.s. — today, the trend
line is a + 1 C (see Columbia graph)-- CO2 is at 410, which is 1.46 * 280 — rise is logarithmic, log (base2) of 1.46 = 0.55 — 1/0.55 = 1.8 — therefore, a
lower bound for ETS is 1.8 C
Depending on meridional heat transport, when freezing temperatures reach deep enough towards
low - latitudes, the ice - albedo feedback can become so effective that climate sensitivity becomes infinite and even negative (implying unstable
equilibrium for any «ice -
line» (latitude marking the edge of ice) between the equator and some other latitude).
A glacier that is approaching
equilibrium during retreat will thin mostly near the terminus, and at some elevation above the terminus, usually near the
equilibrium line or in the
lower accumulation zone, there will be comparatively little thinning (Schwitter and Raymond, 1993).
That is, there is still a fair chance that we can «hold the 2 °C
line», if strong mitigation of greenhouse gases is combined with the following three actions: (i) a slow, rather than instant, elimination of aerosol cooling, (ii) a directed effort to first remove warming aerosols like black carbon, and (iii) a concerted and sustained programme, over this century, to draw - down excessive CO2 (geo - and bio-engineering) and simultaneously reduce non-CO2 forcings, such that the final
equilibrium temperature rise will be
lower than would otherwise be expected on the basis of current concentrations.