Sentences with phrase «atmospheric layer temperature»

Not exact matches

This «would create a persistent layer of black carbon particles in the northern stratosphere that could cause potentially significant changes in the global atmospheric circulation and distributions of ozone and temperature,» they concluded.

Increased atmospheric heat obviously makes temperatures warmer, which leaves less time for ice to form and solidify and create new layers on glaciers and ice sheets.

Black carbon aerosols — particles of carbon that rise into the atmosphere when biomass, agricultural waste, and fossil fuels are burned in an incomplete way — are important for understanding climate change, as they absorb sunlight, leading to higher atmospheric temperatures, and can also coat Arctic snow with a darker layer, reducing its reflectivity and leading to increased melting.

What is more, because Jupiter's microwave emissions vary in wavelength based on the pressure (as well as temperature) of the atmospheric layers where they originate, observations at multiple wavelengths allow researchers to create a cross-section through the atmosphere.

But these cores formed under the weight of their planets» outer layers, under pressures of around 500 gigapascals — 5 million times atmospheric pressure on Earth — and typical temperatures of about 6,000 kelvin.

Regional trends are notoriously problematic for models, and seems more likely to me that the underprediction of European warming has to do with either the modeled ocean temperature pattern, the modelled atmospheric response to this pattern, or some problem related to the local hydrological cycle and boundary layer moisture dynamics.

Titan has a thin atmospheric layer of roughly constant temperature above the troposphere, followed by an extensive stratosphere ranging from 50 to 200 km (30 to 120 miles) in altitude, where temperatures steadily increase with altitude to a maximum of 160 to 180 K (− 172 to − 136 °F, − 113 to − 93 °C).

In the upper atmosphere of this «hot Jupiter» sits a layer of titanium oxide, which has flipped the usual atmospheric temperature structure on its head.

So the mechanism should cause a decline in skin temperature gradients with increased cloud cover (more downward heat radiation), and there should also be a decline in the difference between cool skin layer and ocean bulk temperatures - as less heat escapes the ocean under increased atmospheric warming.

Layer your view of shifting continents with data on atmospheric composition, temperature, biodiversity, day length, and solar luminosity, to get a more complete view of our dynamic planet.

For each channel, the brightness temperature can be thought of as the averaged temperature over a thick atmospheric layer....»

These four channels measure the atmospheric temperature in four thick layers spanning the surface through the stratosphere...... The brightness temperature for each channel corresponds to an average temperature of the atmosphere averaged over that channel's weighting function.

The standard assumption has been that, while heat is transferred rapidly into a relatively thin, well - mixed surface layer of the ocean (averaging about 70 m in depth), the transfer into the deeper waters is so slow that the atmospheric temperature reaches effective equilibrium with the mixed layer in a decade or so.

As the outer atmospheric layers above this point continue to get colder as the column optical depth of the slab is increased, the temperature profile within the slab will appear to «pivot» about the TAU = 1 point.

The radiative transfer problem is best addressed numerically with a sufficient number of vertical layers to resolve the atmospheric temperature and absorber distributions and with a sufficient number of spectral intervals to resolve the spectral dependence of the contributing gases — as is being done in most GCMs.

The advantage of the ocean heat content changes for detecting climate changes is that there is less noise than in the surface temperature record due to the weather that affects the atmospheric measurements, but that has much less impact below the ocean mixed layer.

Accordingly, as the optical depth is cranked up, a temperature gradient will be established within the atmospheric layer as the layer bottom temperature Tb becomes hotter than the layer mean temperature, and the layer top temperature Tt becomes colder than the layer mean.

θ = potential temperature, which is conserved for dry adiabatic processes and is a useful vertical coordinate for examining various fluid mechanical processes (like Rossby waves) when the atmospheric lapse rate is stable (for dry convection)(which is generally true on a large scale away from the boundary layer).

Thus, if the absorption of the infrared emission from atmospheric greenhouse gases reduces the gradient through the skin layer, the flow of heat from the ocean beneath will be reduced, leaving more of the heat introduced into the bulk of the upper oceanic layer by the absorption of sunlight to remain there to increase water temperature.

This simple radiative example (convective transport is not being allowed) shows that any finite surface temperature Ts can be supported in radiative equilibrium with any arbitrarily cold «upper atmosphere» temperature Tt, by prescribing the appropriate LW opacity TAU for the atmospheric layer, with the energy required to maintain a fixed Ts adjusted accordingly.

Ray: «The IR flux from the warmer surface excites much of the CO2 — much more than would be excited at thermal equilibrium at the temperature of the atmospheric layer where the photon is absorbed.»

Starting with zero atmospheric LW absorption, adding any small amount cools the whole atmopshere towards a skin temperature and warms the surface — tending to produce a troposphere (the forcing at any level will be positive, and thus will be positive at the tropopause; it will increase downward toward the surface if the atmosphere were not already as cold as the skin temperature, thus resulting in atmospheric cooling toward the skin temperature; cooling within the troposphere will be balanced by convective heating from the surface at equilibrium, with that surface + troposphere layer responding to tropopause - level forcing.)

(By similar logic, increasing atmospheric optical thickness tends to increase the downward flux at the surface or any other level, and reduce the upward flux at TOA or any other level, but with exceptions due to inversions (layers with increasing temperature with height).

However, there is not a temperature inversion layer between the Stratosphere and the Mesosphere; therefore, there is a clear opportunity for atmospheric turnover or a horizontal rolling mix of the two layers at the boundary levels or the explanation for the «atmospheric waves».

Is it possible that just the atmospheric fronts themselves could result in waves or destabilization of the temperature inversion layer?

One explanation for the seasonal offset is that the large summertime snow / ice change alters ground temperatures, and these ground temperature changes are felt more at ground - level during winter when the surface atmospheric layer is most stable.

In any case; the question seems to me to be moot, since there is general agreement that CO2 and H2O and other GHG molecules DO capture LWIR from the surface or other atmospheric layers; which must increase the net energy (and Temperature) of THAT layer.

Other aspects (temperature, winds, etc.) of the atmospheric environment and chemicals other than halocarbons can also influence the ozone layer.

The global surface is set up as a grid with several dozen vertical layers to resolve the atmospheric temperature structure.

The rise in Arctic temperatures is probably also tied to a sudden warming of the stratosphere, the atmospheric layer about 30,000 feet high - above where most weather happens - that occurred several weeks ago, Moore said.

A National Research Council panel was convened to examine observed trends of temperature near the surface and in the lower to midtroposphere (the atmospheric layer extending from the earth's surface up to about 8 km).

However, I have argued elsewhere, that because of both temperature and density gradients, the escape path to space is favored over the return path to the surface; because of re-absorption in subsequent atmospheric layers.

Each higher and cooler layer in turn emits thermal radiation corresponding to its temperature; and much of that also escapes directly to space around the absorption bands of the higher atmosphere layers; and so on; so that the total LWIR emission from the earth should then be a composite of roughly BB spectra but with source temepratures ranging ove the entire surface Temeprature range, as well as the range of atmospheric emitting Temperatures.

It seems to me that any layer from the surface to the highest limits of the atmosphere is radiating some roughly blackbody looking spectrum corresponding to its own Temperature; and much of that spectrum exits directly to space (assuming cloudless skies for the moment) with a spectrum corresponding to the emission temperature of that surface; but now with holes in it from absorption by GHG molecules or the atmospheric gases Temperature; and much of that spectrum exits directly to space (assuming cloudless skies for the moment) with a spectrum corresponding to the emission temperature of that surface; but now with holes in it from absorption by GHG molecules or the atmospheric gases temperature of that surface; but now with holes in it from absorption by GHG molecules or the atmospheric gases themselves.

Since these two time series represent largely independent mean temperature estimates for the same atmospheric layer, the strong correspondence between them is further proof that the fluctuations are real.

2 The troposphere is the atmospheric layer where the temperature generally decreases with height, extending from the surface up to approximately 10 — 15 km, and the stratosphere is the stable layer above that extending up to approximately 50 km.

Are you saying that because he uses a LTE model with atmospheric layers to explain carbon dioxide IR radiation (and re-radiation), that he is implying that one should find non-smooth temperatures with increasing height in such layers?

For us, one of the most fascinating findings of this analysis is that the atmospheric temperature profiles from the boundary layer to the middle of the stratosphere can be so well described in terms of just two or three distinct regions, each of which has an almost linear relationship between molar density and pressure.

They are assumed to have an additional greenhouse effect causing a further increase of atmospheric temperatures near the ground and a decrease in the layers above approximately 15 km altitude.

Deep in the ice sheets of Greenland are annual layers that record what the atmospheric gases and the air temperature were like over each of the last 250,000 years.

One effect among many is to reduce the temperature gradient within the skin layer of the ocean and hence reduce the rate of cooling of the upper mixed layer (the first few meters of which are warmed by the Sun) to the atmosphere and also, radiatively, through the atmospheric infrared window, directly to space.

Figure 1 shows the different atmospheric layers each defined by temperature changes that reflect different chemistry.

Global average surface air temperatures only reflect the heat present in the atmospheric layer immediately above the land / ocean surface.

The short - term influence of various concentrations of atmospheric carbon dioxide on the temperature profile in the boundary layer.

The satellite temperature weighting function describes the relative contributions that each atmospheric layer makes to the total satellite signal.

Chris's figure (for the change in atmospheric CO2 per degree change in temperature) is within the range calculated for ocean water temperatures in 1999 by J. Ahlbeck, who concluded: ``... a temperature increase of one degree celsius will increase the atmospheric concentration of carbon dioxide in the range of 8 ppm (150 m layer) to 18 ppm (600 m layer).

Even if storms are absent, the cold atmospheric temperatures of winter chill the surface layers of the ocean.

Based on the understanding of both the physical processes that control key climate feedbacks (see Section 8.6.3), and also the origin of inter-model differences in the simulation of feedbacks (see Section 8.6.2), the following climate characteristics appear to be particularly important: (i) for the water vapour and lapse rate feedbacks, the response of upper - tropospheric RH and lapse rate to interannual or decadal changes in climate; (ii) for cloud feedbacks, the response of boundary - layer clouds and anvil clouds to a change in surface or atmospheric conditions and the change in cloud radiative properties associated with a change in extratropical synoptic weather systems; (iii) for snow albedo feedbacks, the relationship between surface air temperature and snow melt over northern land areas during spring and (iv) for sea ice feedbacks, the simulation of sea ice thickness.

They find that the different moisture availability over land and ocean leads to different atmospheric temperature lapse rates (latent heat release), which in combination with a well - mixed free (above boundary layer) atmosphere can explain the land — sea contrast.

«The basic problem of this research is to determine how to merge data from nine instruments to produce a useful time series of deep - layer atmospheric temperatures.