Sentences with phrase «radiative heating rate»

Turner D. D., M. D. Shupe and A. B. Zwink (April 2018): Characteristic Atmospheric Radiative Heating Rate Profiles in Arctic Clouds as Observed at Barrow, Alaska.

Stratospheric heating by potential geoengineering aerosols Geoengineering aerosols change stratospheric radiative heating rates Heating rates depend on aerosol species and size

Not exact matches

If the atmosphere consisted of Oxygen / Nitrogen only, its thermal conductivity would be very low, solar heating would be much the same, and the insulation effect (and the gravitational lapse rate) would produce a substantial temperature differential from the surface to the top of the atmosphere without any radiative absorption.

Since OHC uptake efficiency associated with surface warming is low compared with the rate of radiative restoring (increase in energy loss to space as specified by the climate feedback parameter), an important internal contribution must lead to a loss rather than a gain of ocean heat; thus the observation of OHC increase requires a dominant role for external forcing.

(The difference between zero and non-zero heat capacity responses is proportional to a radiative imbalance, which is proportional to the rate of change in enthalpy and thus temperature, barring a change in where the heat is going, etc..)

radiative forcing = RF «=» V0 feedback (including planck response) «=» voltage across resistor = i * R «=» F * T (negative for stable climate) radiative disequilibrium «=» v0 + i * R = voltage across inductor = L * di / dt «=» heating rate = C * dT / dt okay...

This, and the radiative emission rate allows you to calculate the radiative heat loss from a packet of atmosphere.

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.

For simplicity, assume all solar heating at the surface (so that the lapse rate is (1 - dimensional climate model, radiative convective equilibrium) positive or approaching zero but never negative) unless otherwise stated:

The lapse rate within the troposphere is largely determined by convection, which redistributes any changes in radiative heating or cooling within the troposphere + surface so that all levels tend to shift temperature similarly (with some regional / latitudinal, diurnal, and seasonal exceptions, and some exceptions for various transient weather events).

Re my 441 — competing bands — To clarify, the absorption of each band adds to a warming effect of the surface + troposphere; given those temperatures, there are different equilibrium profiles of the stratosphere (and different radiative heating and cooling rates in the troposphere, etc.) for different amounts of absorption at different wavelengths; the bands with absorption «pull» on the temperature profile toward their equilibria; disequilibrium at individual bands is balanced over the whole spectrum (with zero net LW cooling, or net LW cooling that balances convective and solar heating).

It's because both land and ocean surfaces are heated by shortwave solar radiation and where aerosols reflect SWR equally well over land or water and where greenhouse gases work by retarding the rate of radiative cooling which is not equal over land and water.

That equation is derived from the ratio of the Nusselt and the radiative heat transfer (RHT) rates.

Heat melts Rock like ice and this thuderhead of magma rises high in the geo - sky to bring heat to sea level, thus balancing the core «s heat output when it's radiative rate is slowed by the R - value of the gas atmosphHeat melts Rock like ice and this thuderhead of magma rises high in the geo - sky to bring heat to sea level, thus balancing the core «s heat output when it's radiative rate is slowed by the R - value of the gas atmosphheat to sea level, thus balancing the core «s heat output when it's radiative rate is slowed by the R - value of the gas atmosphheat output when it's radiative rate is slowed by the R - value of the gas atmosphere.

Given the vast pool of very cold water in the deep ocean, even modest changes in the rate it exchanges heat with the surface can produce large changes in temperature without any change in the planetary radiative balance.

In brief, the temperature profile of the atmosphere is set by convection & latent - heat considerations (= > adiabatic lapse rate); based upon that temperature profile, the radiative transfer processes give rise to the radiative forcing which is the GHE.

The dynamics of the system are governed by the lapse rate which is «anchored» to the ground and whose variations are dependent not only on convection, latent heat changes and conduction but also radiative transfer.

The atmospheric heating and cooling rates are then passed back to the atmosphere structure module that calculates how much the surface and atmospheric temperatures would change during the 30 - minute times step given the radiative heating and cooling rates.

This supports the hypothesis that cirrus radiative heating contributes substantially to the average tropical TST rates.

Irrespective of what one thinks about aerosol forcing, it would be hard to argue that the rate of net forcing increase and / or over-all radiative imbalance has actually dropped markedly in recent years, so any change in net heat uptake can only be reasonably attributed to a bit of natural variability or observational uncertainty.

The closest empirical data for a non radiative atmosphere would be the reversed lapse rate and super heating in the stratosphere.

The analysis uses a global energy budget model that links ECS and TCR to changes in global mean surface temperature (GMST), radiative forcing and the rate of ocean heat uptake between a base and a final period.

This is achieved through the study of three independent records, the net heat flux into the oceans over 5 decades, the sea - level change rate based on tide gauge records over the 20th century, and the sea - surface temperature variations... We find that the total radiative forcing associated with solar cycles variations is about 5 to 7 times larger than just those associated with the TSI variations, thus implying the necessary existence of an amplification mechanism, although without pointing to which one.

The tropospheric lapse rate is maintained mostly by convective transports of heat upwards, in thunderstorms and thunderstorm complexes, including mesoscale disturbances, various waves and tropical storms, while radiative processes serve to cool the troposphere.

The probabilistic analyses of DAI reported in this section draw substantially on (subjective) Bayesian probabilities to describe key uncertainties in the climate system, such as climate sensitivity, the rate of oceanic heat uptake, current radiative forcing, and indirect aerosol forcing.

Vincentrj # 28 you are unclear re the division of your opinions / inferences between the 3 basic sub-topics (1) heat is entering the oceans due to radiative imbalance due to humans burning carbon fuels (2) the heat rate coupled with its estimated duration (based on its cause) will make it within a few decades become unprecedented during the last several thousand years and same for the surface temperature rise that will be required to stop it (3) the effects on flora & fauna will be highly negative even within this century and more so for centuries and millenia thereafter, in particular the human species which has softened much and expects much more since the days when a mammoth tusk through the groin was met with «well Og's had it, press on».

Steve I will ask you to show the radiative heat transfer equation in which you input an emission from another body, gas / solid or fluid and show where it lowers the rate of cooling.

If you have good measurements of upper ocean and atmospheric temperatures, then if you had a good decade - long satellite record of the Earth's total radiative energy balance from space — say, if Triana has been launched to in the late 1990s — then you could use conservation of energy to calculate the rate of heat uptake by the deep ocean over the past ten years.

By contrast, here are the heating / cooling rates from a comprehensive (= «standard») radiative - convective model, plotted against height instead of optical thickness.

It has been demonstrated in small - scale experimental fires that the amount of radiant heat energy liberated per unit time (the fire radiative power; FRP) is related to the rate at which fuel is being consumed.

If there is, concurrently to this process, a reduction in the rate of cooling of the mixed layer to the atmosphere and to space (radiative + latent + sensible), then this will offset upwelling cooling of the mixed layers while the deeper layers will still gain heat unabated (or even at an increased rate).

Figure S1: (a-g): Ensemble - average instantaneous radiative forcings and ocean heat uptake rates (thick lines) and individual ensemble members (thin) for GISS - E2 - R single - forcing experiments.

Looking at the last decade, it is clear that the observed rate of change of upper ocean heat content is a little slower than previously (and below linear extrapolations of the pre-2003 model output), and it remains unclear to what extent that is related to a reduction in net radiative forcing growth (due to the solar cycle, or perhaps larger than expected aerosol forcing growth), or internal variability, model errors, or data processing — arguments have been made for all four, singly and together.

But the radiative cooling is time dependent, and a steeper lapse rate will increase convection and decrease the time over which a rising parcel can radiate heat away, increasing the relative amount of adiabatic versus radiative cooling.

When discussing radiative thermal energy exchange between two objects, it may very well be more appropriate to talk about the heat between objects and not mention the rate thermal energy leaves each object in the direction of the other object.