Sentences with phrase «equilibrium response times»

The typical equilibrium response times of the climate system's various components range from a single day to millenia.

It's also possible that a lower TCR would simply indicate a longer equilibrium response time.

Not exact matches

And is the current large scale ablation seen on these glaciers due to these glaciers coming to some equilibrium with a warmer world due to coming out of the LIA and response times associated with the large masses involved?

Furthermore, you also need to distinguish the equilibrium response from the response at any point in time when following a particular scenario.

They conclude, based on study of CMIP5 model output, that equilibrium climate sensitivity (ECS) is not a fixed quantity — as temperatures increase, the response is nonlinear, with a smaller effective ECS in the first decades of the experiments, increasing over time.

These transient models show that not enough time has elapsed for the equilibrium response to be achieved.

The functional response for cat trapping (the offtake with constant effort per unit time) overlaid against the curve of cat productivity suggested a stable equilibrium point at low cat densities (0.07 — 0.13 cats km — 2).

Because latent heat release in the course of precipitation must be balanced in the global mean by infrared radiative cooling of the troposphere (over time scales at which the atmosphere is approximately in equilibrium), it is sometimes argued that radiative constraints limit the rate at which precipitation can increase in response to increasing CO2.

(57k) When I state that the equilibrium climatic response must balance imposed RF (and feedbacks that occur), I am referring to a global time average RF and global time average response (in terms of radiative and convective fluxes), on a time scale sufficient to characterize the climatic state (including cycles driven by externally - forced cycles (diurnal, annual) and internal variability.

The disequilibrium referred to comes from the fact that the ocean has a lot of thermal inertia and takes a long time to warm up, whereas the atmosphere has a short response time and quickly comes into equilibrium with any given ocean temperature, corresponding to the current amount of greenhouse gases.

The instantaneous RF difference between the tropopause and TOA is the instantaneous forcing on the stratosphere RFs1; if the TOA forcing is smaller than the tropopause forcing, then the forcing on the stratosphere is negative, which means that the stratosphere will cool (this doesn't necessarily mean it will cool everywhere, but the equilibrium response to negative stratospheric RF requires a negative PR+CR response — being the stratosphere, at least in the global time average, CR can be approximated as zero).

Starting from an old equilbrium, a change in radiative forcing results in a radiative imbalance, which results in energy accumulation or depletion, which causes a temperature response that approahes equilibrium when the remaining imbalance approaches zero — thus the equilibrium climatic response, in the global - time average (for a time period long enough to characterize the climatic state, including externally imposed cycles (day, year) and internal variability), causes an opposite change in radiative fluxes (via Planck function)(plus convective fluxes, etc, where they occur) equal in magnitude to the sum of the (externally) imposed forcing plus any «forcings» caused by non-Planck feedbacks (in particular, climate - dependent changes in optical properties, + etc.).)

[Response: Questions 3 and 4 only specify a certain time point, and thus appear (to me) to be asking for the transient, not equilibrium, temperature changes.

One can consider net PR+CR as a response to externally - imposed RF (external forcing) plus feedback «RF», or one can consider PR + CR — feedback «RF» as the response to the externally imposed RF; the later is perhaps more helpful in picturing the time evolution toward equilibrium (and illustrates why the time it takes for an imbalance, equal to: externally imposed RF — climate dependent terms (PR + CR — feedback «RF»), to decay is proportional to both heat capacity and climate sensitivity (defined per unit externally imposed RF).

The equilibrium response to an addition of RF at a level is an increase in net upward flux consisting of LW radiation (the Planck response, PR) plus a convective flux response CR; CR is approximately zero at and above the tropopause in the global time average.

part of the utility is that Charney sensitivity, using only relatively rapid feedbacks, describes the climate response to an externally imposed forcing change on a particular timescale related to the heat capacity of the system (if the feedbacks were sufficiniently rapid and the heat capacity independent of time scale (it's not largely because of oceanic circulation), an imbalance would exponentially decay on the time scale of heat capacity * Charney equilibrium climate sensitivity.

You state in the response to # 10, ``... There is no surprise that the CO2 in the atmosphere winds up partially in the oceans, nor that the amount of CO2 going into or coming out of the oceans varies in time and space — that's simple equilibrium chemistry between the liquid (that is, dissolved) and gaseous phases...» Are the buffers a part of simple equilibrium chemistry, and where can I go to read up on this and how it pertains to the Models.

This Nature Climate Change paper concluded, based purely on simulations by the GISS - E2 - R climate model, that estimates of the transient climate response (TCR) and equilibrium climate sensitivity (ECS) based on observations over the historical period (~ 1850 to recent times) were biased low.

The equilibrium climate sensitivity quantifies the response of the climate system to constant radiative forcing on multi-century time scales.

Some moderate uncertainty begins to arise when we go beyond the radiative forcings and start looking at the climate response time as to how quickly the climate system approaches equilibrium.

«Their study shows that the time - dependent response of zonal mean surface temperature differs significantly from its equilibrium response particularly in those latitude belts, where the fraction of ocean - covered area is relatively large.

«The equilibrium climate sensitivity quantifies the response of the climate system to constant radiative forcing on multicentury time scales.

So it seems to me that the simple way of communicating a complex problem has led to several fallacies becoming fixed in the discussions of the real problem; (1) the Earth is a black body, (2) with no materials either surrounding the systems or in the systems, (3) in radiative energy transport equilibrium, (4) response is chaotic solely based on extremely rough appeal to temporal - based chaotic response, (5) but at the same time exhibits trends, (6) but at the same time averages of chaotic response are not chaotic, (7) the mathematical model is a boundary value problem yet it is solved in the time domain, (8) absolutely all that matters is the incoming radiative energy at the TOA and the outgoing radiative energy at the Earth's surface, (9) all the physical phenomena and processes that are occurring between the TOA and the surface along with all the materials within the subsystems can be ignored, (10) including all other activities of human kind save for our contributions of CO2 to the atmosphere, (11) neglecting to mention that if these were true there would be no problem yet we continue to expend time and money working on the problem.

And the gut feeling by IPCC is everything from a walk in the park to catastrophe: «The equilibrium climate sensitivity quantifies the response of the climate system to constant radiative forcing on multi - century time scales.

Each of these components, C1, C2 and C3, is then associated with some fraction of the emissions into the atmosphere, E, and a particular removal mechanism: where b3 (= 0.1) is a fixed constant representing the Revelle buffer factor, and b1 is a fixed constant such that b1 + b3 = 0.3 [11]; b1 represents the fraction of atmospheric CO2 that would remain in the atmosphere following an injection of carbon in the absence of the equilibrium response and ocean advection; b0 represents an adjustable time constant, the inverse of which is of order 200 years.

Physically, C1 can be thought of as representing the concentration of CO2 in long - term stores such as the deep ocean; C1 + C2 as representing the CO2 concentration in medium - term stores such as the thermocline and the long - term soil - carbon storage; and C = C1 + C2 + C3 as the concentration of CO2 in those sinks that are also in equilibrium with the atmosphere on time scales of a year or less, including the mixed layer, the atmosphere itself and rapid - response biospheric stores.

The response time of the troposphere is relatively short, from days to weeks, whereas the stratosphere reaches equilibrium on a time scale of typically a few months.

4) If WV stayed the same on a planet entirely covered by land and all else being equal the equilibrium temperature of that planet would be much less than that of Earth because the faster response time in warming up from solar energy would be matched by an equally fast loss of energy at night and in winter.

Energy budget estimates of equilibrium climate sensitivity (ECS) and transient climate response (TCR) are derived using the comprehensive 1750 — 2011 time series and the uncertainty ranges for forcing components provided in the Intergovernmental Panel on Climate Change Fifth Assessment Working Group I Report, along with its estimates of heat accumulation in the climate system.

In the case of this glacier, its response time to approach a new equilibrium is in excess of 100 years (Pelto and Hedlund, 2001).

Because of the slow response time of the climate system, the equilibrium climate consistent with current levels of greenhouse gases will not be reached for many centuries.

They conclude, based on study of CMIP5 model output, that equilibrium climate sensitivity (ECS) is not a fixed quantity — as temperatures increase, the response is nonlinear, with a smaller effective ECS in the first decades of the experiments, increasing over time.

If the sea level response to a change in temperature is an exponential decay to equilibrium then given that the 0.8 C temperature increase since pre-industrial times occurred over a relatively short time period relative to time scale of the ice - albedo feedback, the expected rate of sea level rise should be approximately 3 m / C * 0.8 C / 560 y = 43 cm per century.

From AR5: «The resulting equilibrium temperature response to a doubling of CO2 on millennial time scales or Earth system sensitivity is less well constrained but likely to be larger than ECS...» See also ``... medium confidence that Earth - system sensitivity may be up to two times the model equilibrium climate sensitivity (ECS).»