atmosphere

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The extremely tenuous, outermost layer of Earth's atmosphere; it lies above the ionosphere and extends from the so-called exobase, at a height of about 500 km, to the edge of interplanetary space. At or below the exobase, the atmosphere is sufficiently dense that collisions dominate the motion of gas molecules and atoms. Above the exobase, on the other hand, collisions are so infrequent that atoms moving with sufficient velocity have a high probability of escaping from Earth's gravitational field into interplanetary space. Escaping atoms make up only a portion of the exospheric hydrogen, however. There is also a gravitationally bound component that consists both of atoms following ballistic trajectories and of satellite atoms that orbit the Earth for some time before returning to the denser atmosphere. The density and structure of the exosphere are influenced by a number of factors, including variations in the temperature and density of the atmosphere below the exobase, photoionization and ionization by impact with solar wind particles, charge exchange with the plasma of the plasmasphere, and radiation pressure exerted by solar far-ultraviolet photons.

For more information on atmosphere, visit Britannica.com.

A gaseous layer that envelops the Earth and most other planets in the solar system. Earth, Venus, Mars, Jupiter, Saturn, Uranus, Neptune, and Titan (Saturn's largest satellite) are all known to possess substantial atmospheres that are held by the force of gravity. The structure and properties of the various atmospheres are determined by the interplay of physical and chemical processes. Structural features of Earth's atmosphere detailed below can often be identified in the atmospheres of other planetary bodies. See also Planetary physics.

The composition of the Earth's atmosphere is primarily nitrogen (N₂), oxygen (O₂), and argon (Ar) [see table]. The concentration of water vapor (H₂O) is highly variable, especially near the surface, where volume fractions can vary from nearly 0% to as high as 4% in the tropics. There are many minor constituents or trace gases, such as neon (Ne), helium (He), krypton (Kr), and xenon (Xe), that are inert, and active species such as carbon dioxide (CO₂), methane (CH₄), hydrogen (H₂), nitrous oxide (NO), carbon monoxide (CO), ozone (O₃), and sulfur dioxide (SO₂), that play an important role in radiative and biological processes.

Composition of the atmosphere*

Molecule	Fraction volume near surface	Vertical distribution
Major constituents
N2	7.8084 × 10−1	Mixed in homosphere; photochemical dissociation high in thermosphere
O2	2.0946 × 10−1	Mixed in homosphere; photochemically dissociated in thermosphere, with some dissociation in mesosphere and stratosphere
Ar	9.34 × 10−3	Mixed in homosphere with diffusive separation increasing above
Important radiative constituents
CO2	3.5 × 10−4	Mixed in homosphere; photochemical dissociation in thermosphere
H2O	Highly variable	Forms clouds in troposphere; little in stratosphere; photochemical dissociation above mesosphere
O3	Variable	Small amounts, 10−8, in troposphere; important layer, 10−6 to 10−5, in stratosphere; dissociated above
Other constituents
Ne	1.82 × 10−5
He	5.24 × 10−6	Mixed in homosphere with diffusive separation increasing above
Kr	1.14 × 10−6
CH4	1.15 × 10−6	Mixed in troposphere; dissociated in upper stratosphere and above
H2	5 × 10−7	Mixed in homosphere; product of H2O photochemical reactions in lower thermosphere, and dissociated above
NO	∼10−8	Photochemically produced in stratosphere and mesosphere

*Other gases, for example, CO, N₂O, NO₂, and many by-products of atmospheric pollution also exist in small amounts.

In addition to the gaseous component, the atmosphere suspends many solid and liquid particles. Aerosols are particulates usually less than 1 micrometer in diameter that are created by gas-to-particle reactions or are lifted from the surface by the wind. A portion of these aerosols can become centers of condensation or deposition in the growth of water and ice clouds. Cloud droplets and ice crystals are made primarily of water with some trace amounts of particles and dissolved gases. Their diameters range from a few micrometers to about 100 μm. Water or ice particles larger than about 100 μm begin to fall because of gravity and may result in precipitation at the surface. See also Aerosol; Cloud physics; Precipitation (meteorology).

One of the remarkable properties of the Earth's atmosphere is the large amount of free molecular oxygen in the presence of gases such as nitrogen, methane, water vapor, hydrogen, and others that are capable of being oxidized. The atmosphere is in a highly oxidizing state that is far from chemical equilibrium. This is in sharp contrast to the atmospheres of Venus and Mars, the planets closest to the Earth, which are composed almost entirely of the more oxidized state, carbon dioxide. The chemical disequilibrium on the Earth is maintained by a continuous source of reactive gases derived from biological processes. Life plays a vital role in maintaining the present atmospheric composition. See also Atmospheric chemistry; Mars; Venus.

The total mass of the Earth's atmosphere is about 5.8 × 10¹⁵ tons (5.3 × 10¹⁵ metric tons). The vertical distribution of gaseous mass is maintained by a balance between the downward force of gravity and the upward pressure gradient force. The balance is known as the hydrostatic balance or the barometric law. Hence, the declining atmospheric pressure that is measured while ascending in the atmosphere is a result of gravity. The globally averaged pressure at mean sea level is 1013.25 millibars (101,325 pascals).

Below about 60 mi (100 km) in altitude, the atmosphere's composition of major constituents is very uniform. This region is known as the homosphere to distinguish it from the heterosphere above 60 mi (100 km), where the relative amounts of the major constituents change with height. In the homosphere there are sufficient atmospheric motions and a short enough molecular free path to maintain uniformity in composition. Above the boundary between the homosphere and the heterosphere, known as the homopause or turbopause, the mean free path of the individual molecules becomes long enough that gravity is able to partially separate the lighter molecules from the heavier ones. The mean free path is the average distance that a particle will travel before encountering a collision. Hence the average molecular weight of the heterosphere decreases with height as the lighter atoms dominate the composition.

The vertical structure of the atmosphere is in large part determined by the transfer properties of the solar and terrestrial radiation streams. The energy of the smallest unit of radiation, the photon, is directly proportional to its frequency. The type of interaction that occurs between photons and the atmosphere depends on the energy of the photons. See also Photon.

The most energetic of the photons are x-rays and extreme ultraviolet radiation of the eletromagnetic spectrum, which are capable of dissociating and ionizing the gaseous molecules. The less energetic near-ultraviolet photons are able to excite molecules and atoms into higher electronic levels. As a result, most of the ultraviolet and x-ray radiation is attenuated by the upper atmosphere. A cloudless atmosphere, however, is relatively transparent to visible light, where most of the solar energy resides. At the opposite end of the spectrum toward the lower frequencies of radiation is the infrared part, which is capable of inducing various vibrational and rotational motions in triatomic and polyatomic molecules.

In order to maintain an energy balance, the Earth must emit about the same amount of radiation as it absorbs from the Sun. The terrestrial radiation occurs in the infrared part of the spectrum and hence is strongly affected by water vapor, clouds, carbon dioxide, and ozone and other trace gases. The ability of these gases to absorb and emit in the infrared allows them to effectively trap some of the outgoing radiation that is emitted by the surface, creating the so-called greenhouse effect. See also Insolation.

The atmospheric layer that extends from the surface to about 7 mi (11 km) is called the troposphere. The tropopause, which is the top of the troposphere, has an average altitude that varies from about 11 mi (18 km) near the Equator to about 5 mi (8 km) near the Poles. The actual tropopause height varies considerably on time scales from a few days to an entire year. The troposphere contains about 80% of the atmospheric mass and exhibits most of the day-to-day weather fluctuations that are observed from the ground. Temperatures generally decrease with increasing altitude at an average lapse rate of about 17°F/mi (6°C/km), although this rate varies considerably, depending on time and location. See also Tropopause; Troposphere.

The stratosphere is the atmospheric layer that extends from the tropopause up to the stratopause at about 30 mi (50 km) above the surface. It is characterized by a nearly isothermal layer in the first 6 mi (10 km) overlaid by a layer in which the temperature increases with height to a maximum of about 32°F (0°C) at the stratopause. The reversal in the temperature lapse rate is a result of direct absorption of solar radiation, mainly by ozone and oxygen at the ultraviolet frequencies. See also Stratosphere.

The reversal of the temperature lapse rate makes the stratosphere vertically stable. This stability limits the amount of vertical mixing and results in molecular residence times of many months to years. Another consequence of a stable stratosphere is that it acts as a lid on the troposphere, confining the strong vertical overturning and hence most of the surface-based weather phenomena. See also Weather.

The mesosphere is the atmospheric layer extending from the stratopause up to the mesopause at an altitude of about 53 mi (85 km). The mesosphere is characterized by temperatures decreasing with height at a rate of about 12°F/mi (4°C/km). Although the mesosphere has less vertical stability than the stratosphere, it is still more stable than the troposphere and does not experience rapid overturning. The coldest temperatures of the entire atmosphere are encountered at the mesopause, with values as low as −150°F (−100°C). The temperature lapse rate found in the mesosphere is a result of the gradual weakening with height of the direct absorption of solar radiation by ozone. The radiative infrared cooling to space by the carbon dioxide molecules is responsible for the low temperatures near the mesopause. See also Mesosphere.

The thermosphere is found above the mesopause. The thermosphere is characterized by rising temperatures with height up to an altitude of about 190 mi (300 km) and then is nearly isothermal above that. Although there is no clear upper limit to the thermosphere, it is convenient to consider it extending several thousand kilometers. Embedded within the thermosphere is the ionosphere, comprising those atmospheric layers in which the ionized molecules and atoms are dominating the processes.

Molecular species dominate the lower thermosphere, while atomic species are dominant above 190 mi (300 km). The distribution of the constituents is controlled by diffusive equilibrium in which the concentration of each constituent decreases exponentially with height according to its molecular weight. Hence the concentration of the heavier constituents such as nitrogen, oxygen, and carbon dioxide will decrease with height faster than the lighter constituents such as helium and hydrogen. At an altitude of 560 mi (900 km) helium becomes the dominant constituent while hydrogen dominates above 1900 mi (3000 km).

The ionosphere can be defined operationally as that part of the atmosphere that is sufficiently ionized to affect the propagation of radio waves. In the ionosphere, the dominant negative ion is the electron, and the main positive ions include O⁺, NO⁺, and O₂⁺. The ionosphere is classified into four subregions. The D region extends from 40 to 60 mi (60 to 90 km) and contains complex ionic chemistry; most of the ionization is caused by ultraviolet ionization of NO and by galactic cosmic rays. This region is responsible for the daytime absorption of radio waves, which prevents distant propagation of certain frequencies. The E region extends from 60 to 90 mi (90 to 150 km) and is caused primarily by the x-rays from the Sun. The F1 region from 90 to 125 mi (150 to 200 km) is caused by the extreme ultraviolet radiation from the Sun and disappears at night. Finally, the F2 region includes all the ionized particles above 125 mi (200 km), with the peak ion concentrations occurring near 190 mi (300 km). See also Cosmic rays; Ionosphere.

The exosphere is the atmosphere above 300 mi (500 km) where the probability of interatomic collisions is so low that some of the atoms traveling upward with sufficient velocity can escape the Earth's gravitational field. The dominant escaping atom is hydrogen since it is the lightest constituent. Calculations of the thermal escape of hydrogen (also known as the Jeans escape) yield a value of about 3 × 10⁸ atoms · cm⁻² · s⁻¹. This is a very small amount since at this rate less than 0.5% of the oceans would disappear over the current age of the Earth.

The magnetosphere is the region surrounding the Earth where the movement of ionized gases is dominated by the geomagnetic field. The lower boundary of the magnetosphere, which occurs at an altitude of nearly 75 mi (120 km), can be roughly defined as the height where there are enough neutral atoms that the ion-neutral particle collisions dominate the ion motion. The dynamics of the magnetosphere is dictated in part by its interaction with the plasma of ionized gases that blows away from the Sun, the solar wind. The solar wind interacts with the Earth's magnetic field and severely deforms it, producing a magnetosphere around the Earth. It extends about 40,000 mi (60,000 km) toward the Sun but extends beyond the orbit of the Moon away from the Sun. See also Magnetosphere; Solar wind; Van Allen radiation.

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noun

1. The gaseous mixture enveloping the earth: air. See high/low, place.
2. A general impression produced by a predominant quality or characteristic: air, ambiance, aura, feel, feeling, mood, smell, tone. See be.
3. The totality of surrounding conditions and circumstances affecting growth or development: ambiance, climate, environment, medium, milieu, mise en scène, surroundings, world. See be, limited/unlimited, place.
4. A distinctive yet intangible quality deemed typical of a given thing: aroma, flavor, savor, smack. See taste/bad taste.

The earth's atmosphere is simple in some respects, and complex in others. It is relatively uniform in composition with respect to its major mass components (oxygen and nitrogen), yet extremely variable in some minor components, such as water vapor and ozone (O₃), which play major roles in its heat and radiation fluctuations. The atmosphere has a complex structure based on temperature gradients. This structure governs its mixing characteristics and the buildup of contaminants, yet is usually invisible, except when light-scattering particles suspended in the air make it visible. The structure of the atmosphere is of major importance to the dilution and dispersion of contaminants. It is governed by the lapse rate, which is the rate of change of air temperature with height above the ground.

The lowest of the atmospheric layers is the troposphere, which contains about 75 percent of the mass of the atmosphere, and almost all of its moisture. It extends to a height that varies from about 9 kilometers at the poles to about 15 kilometers at the equator, and it has an average lapse rate of about −6.5°C/km. The boundary between the troposphere and the next layer, the stratosphere, is known as the tropopause. The stratosphere contains essentially all of the remainder of the mass of the atmosphere; it is nearly isothermal (the temperature does not change with altitude) in the lower regions and shows a temperature increase with height in the upper regions. There is very little air exchange between the well-mixed and turbulent troposphere and the nearly stagnant stratosphere.

The major constituents of dry air at ground level are nitrogen (N₂) at 78.1 percent by volume, oxygen (O₂) at 21.0 percent, and argon (Ar) at 0.9 percent. Carbon dioxide (CO₂) is present at about 330 ppm by volume and methane (CH₄) at about1.5 ppm by volume. About 3 percent of the total mass of the lower atmosphere is water vapor (H₂O), but the concentration is extremely variable in both space and time. In general, the warmer portions of the atmosphere contain more water vapor. The water vapor content becomes lower with increasing altitude and with increasing latitude. Water vapor plays a critical role in governing the earth's heat exchange and the motion of the atmosphere, due to its high heat capacity, absorption of infrared radiation, and heat of vaporization. Further effects attributable to atmospheric water result when air motion creates clouds (aerosols of water droplets), in which the energy received as sunshine in one place is liberated as the latent heat of vaporization in another.

Of the incoming radiant energy, about 30 to 50 percent is scattered back toward space, reflected primarily by clouds and, to some extent, by solid particles or by the earth's surface. About 20 percent of the incident radiant energy is absorbed as it passes through the atmosphere. Stratospheric O₃ absorbs about 1 to 3 percent, primarily in the short-wave ultraviolet (UV) portion of the spectrum; this effectively limits further penetration to those wavelengths greater than 0.3 microns. In the troposphere, 17 to 19 percent of the incoming radiation is absorbed, due primarily to water vapor and secondarily to CO₂.

The average radiation into space essentially equals that absorbed from the sun, and a substantial amount of energy must flow from the tropics toward the poles within the oceans and the troposphere. This flow of energy is accomplished primarily by systems of warm air and ocean currents that flow toward the poles and cool currents that flow toward the tropics.

The dispersion of contaminants within the atmosphere is generally referred to as diffusion. For practical purposes, the dispersion of contaminants by molecular diffusion is negligible because the extent of movements are generally infinitesimal compared to the movements of the air volumes containing them by the turbulent motions of the air (turbulent diffusion).

Atmospheric turbulence is a complicated phenomenon that has defied mathematical description. When considering contaminant dispersion, contaminant sources can be divided into three different categories: (1) point sources, such as tall industrial smokestacks; (2) line sources, such as highways; and (3) area sources, such as whole urban regions. The simplest is an elevated point source. The light-scattering properties of the aerosol in the plume from such a stack, consisting of fly ash and condensed water, enable us to observe plume dispersion with the unaided eye.

The vertical mixing of air is dependent upon the temperature profile of the atmosphere (the lapse rate). The immediate ground level concentrations of air contaminants may be reduced by vertical mixing, since dispersal into higher regions dilutes the contaminants. Poor vertical mixing may allow concentrations released at low altitudes to remain there in relatively concentrated form. An extreme case of atmospheric stability occurs when the atmospheric lapse rate is negative (when the temperature increases with altitude). This condition is known as a temperature inversion. There is virtually no vertical air movement within inversion layers and contaminants accumulate within them.

(SEE ALSO: Airborne Particles; Ambient Air Quality [Air Pollution]; Climate Change and Human Health)

— MORTON LIPPMANN

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n.the air enveloping the earth.

See the Introduction, Abbreviations and Pronunciation for further details.

1. The layer of air surrounding the Earth, with an average composition, by volume, of 79% nitrogen, 20% oxygen, 0.03% carbon dioxide, and traces of rare gases. This surprisingly uniform composition is achieved by convection in the turbosphere and by diffusion above it, especially above 100 km, where diffusion is rapid in the thin atmosphere, and stirring is weak. Also present are atmospheric moisture, ammonia, ozone, and salts and solid particles. The atmosphere is commonly divided into the troposphere, the stratosphere, and the ionosphere.

Since the troposphere contains the majority of the atmospheric mass, and virtually all of the atmospheric water vapour, most weather events occur within it.

2. A unit of air pressure; one atmosphere is equal to the pressure exerted by the weight of a column of 760 mm of mercury at 0 °C, under standard gravity, at sea level.

1. Gases enveloping the Earth at sea level consisting of approximately 78% nitrogen. 20.95% oxygen, and 0.37% carbon dioxide, and variable amounts of water vapour.

2. Unit of pressure; one normal atmosphere equals 101 325 N m⁻².

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Atm is the abbreviation for atmosphere, which in the wine world is the measurement for pressure used to produce sparkling wines. Technically, it's the normal air pressure at sea level, approximately 14.7 pounds per square inch. In the production of a standard sparkling wine such as champagne or spumante the pressure should be 6 atm. A crémant-style sparkling wine has about half that pressure, and some frizzante-style Italian wines may have only 2 atm of pressure.

To convert from atmospheres to:

ton/sq. inch, multiply by 0.007348.
cms of mercury, multiply by 76.
ft. of water (at 4 degrees C), multiply by 33.9.
in. of mercury (at 0 degrees C), multiply by 29.92.
kgs/sq. cm, multiply by 1.0333.
kgs/sq. meter, multiply by 10332.
pounds/sq. in, multiply by 14.7.
tons/sq. ft, multiply by 1.058.

Convert:  Into:  ton/sq. inch cms of mercury ft. of water (at 4 degrees C) in. of mercury (at 0 degrees C) kgs/sq. cm kgs/sq. meter pounds/sq. in tons/sq. ft

Result:

Mixture of gases that surround and are gravitationally attached to a planet.

IN BRIEF: The gases around a planet or star. The feeling of a place.

A loving atmosphere in your home is the foundation of your life.

LearnThatWord.com is a free vocabulary and spelling program where you only pay for results!

sign description: One A hand makes a circular motion around the index finger of the opposite hand.

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The blanket of gas on the surface of a planet or satellite.

The atmosphere of the Earth is roughly eighty percent nitrogen and twenty percent oxygen, with traces of other gases. (See ionosphere, stratosphere, and troposphere.)

i. The mixture of gases and particles surrounding the earth where weather occurs. This body of air, which surrounds the earth (or for that matter any other celestial body), is defined at its outer limits by the actual presence of air particles. However, they are so few in numbers that collisions between them are so rare as to make force of gravity the only means of keeping them associated with air particles at lower altitudes. Atmosphere is divided into a number of layers, and temperatures within these layers follow a set pattern. These layers are the troposphere, stratosphere, mesosphere, and thermosphere. Another method of dividing the atmosphere is into lower and outer atmospheres. For aerodynamic calculations, norms set in international standard atmosphere are followed.
ii. The unit of air pressure, based on the pressure exerted by the air on the surface of the earth (i.e., 1 atm (atmosphere) = 1.0333 kg/cm2 /14.7 lb, or about 1,013,246 dyn/cm2 .

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1. The environment in which a food is eaten, as is in a restaurant. That is, the other sensory cues accompanied with the flavor while it is being perceived. In other words, the flavor's atmosphere is the environment in which the perception of many secondary senses occurs. Examples of this are the visual cloudiness of orange juice (light), the fizz of champagne or the crunch of a nacho chip (sound), the temperature of meat, the heat of chili (touch and trigeminal sensation). Therefore, the ambience of the surroundings plays an importance in the overall perception of the flavor and the degree to which positive flavor cognition is derived and remembered.
   
2. The measurement of the normal pressure of air at sea level.
   
3. The quality of the air around a substance chemically, sensorially, and physically. The atmosphere around a Maillard Reaction brought to high pressures and temperatures is often purged by a nitrogen blanket. In this manner, the replaced atmosphere contains little oxygen, and the development of harmful phenolic substances is avoided. See Food Technology, Oxidation.
   

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1. the envelope of gas surrounding the Earth.
2. any local gaseous environment.
3. symbol: atm; a non-SI unit of pressure equal to 101.325 kPa; the pressure that will support a column of mercury 760 mm high at 273.15 K, sea-level, and latitude 45°.

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n
atm

The natural body of air, composed of approximately 20% oxygen, 78% nitrogen, and 2% carbon dioxide and other gases, that covers the surface of the earth.

For a list of words related to atmosphere, see:

• Earth’s Atmosphere and Topographic Features - atmosphere: air forming gaseous envelope that surrounds Earth, consisting of troposphere, stratosphere, mesosphere, thermosphere, ionosphere, and exosphere, which merges into outer space at altitude of several hundred miles
• Forecasting and Meteorology - atmosphere: entire mass of air enveloping Earth
• Celestial Phenomena and Points - atmosphere: gaseous envelope surrounding star, planet, or other celestial body
• Tools, Tests, Units, and Scales - atmosphere: unit of pressure equal to that exerted by a column of mercury 760 mm high, equal to 101,325 pascal, based on average atmospheric pressure at sea level
• Devices, Techniques, and Elements - atmosphere: dominant mood or tone of a work

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See words rhyming with "atmosphere."

  See crossword solutions for the clue Atmosphere.

This entry is from Wikipedia, the leading user-contributed encyclopedia. It may not have been reviewed by professional editors (see full disclaimer)

Dansk (Danish)
n. - atmosfære, luftlag

idioms:

• one could cut the atmosphere with a knife    luften var så tyk, at man kunne skære i den
• with atmosphere    stemningsfuld

Nederlands (Dutch)
atmosfeer, sfeer, dampkring, (eenheid van) luchtdruk luchtlaag

Français (French)
n. - (lit, Phys) atmosphère, (fig) atmosphère, ambiance

idioms:

• one could cut the atmosphere with a knife    l'atmosphère était très tendue

Deutsch (German)
n. - Atmosphäre, Klima, Luft

idioms:

• one could cut the atmosphere with a knife    die Luft war zum Schneiden, die Atmosphäre war zum Zerreißen gespannt

Ελληνική (Greek)
n. - (μετεωρ.) ατμόσφαιρα, (μτφ.) κλίμα, (γενική) ατμόσφαιρα

idioms:

• one could cut the atmosphere with a knife    η ατμόσφαιρα ήταν άκρως τεταμένη
• with atmosphere    (για χώρο) με κατάλληλη ατμόσφαιρα

Italiano (Italian)
atmosfera

idioms:

• festive atmosphere    aria di festa
• layer of the atmosphere    strato dell'atmosfera
• with atmosphere    con ambiente
• work atmosphere    ambiente di lavoro
• working atmosphere    ambiente lavorativo

Português (Portuguese)
n. - atmosfera (f), ambiente (m)

idioms:

• festive atmosphere    atmosfera festiva
• layer of the atmosphere    camada (f) da atmosfera
• with atmosphere    com ambiente
• work atmosphere    ambiente de trabalho
• working atmosphere    ambiente de trabalho

Русский (Russian)
обстановка, атмосфера, воздух, озоновый слой

idioms:

• festive atmosphere    праздничная атмосфера
• layer of the atmosphere    атмосферный слой
• with atmosphere    с атмосферой (обыкн. позитивной)
• work atmosphere    рабочая обстановка
• working atmosphere    рабочая обстановка

Español (Spanish)
n. - ambiente, clima, atmósfera

idioms:

• one could cut the atmosphere with a knife    el ambiente se podía cortar con un cuchillo

Svenska (Swedish)
n. - atmosfär, stämning

中文（简体）(Chinese (Simplified))
大气, 气氛

idioms:

• one could cut the atmosphere with a knife    气氛很热闹
• with atmosphere    具有艺术气氛

中文（繁體）(Chinese (Traditional))
n. - 大氣, 氣氛

idioms:

• one could cut the atmosphere with a knife    氣氛很熱鬧
• with atmosphere    具有藝術氣氛

한국어 (Korean)
n. - 대기, 기압, 분위기, 맛

idioms:

• with atmosphere    ~의 분위기를 가진

日本語 (Japanese)
n. - 大気, 空気, 四囲の情況, 気圧, 全体的な感じ, 雰囲気, 一風変わった感じ

idioms:

• with atmosphere    ムードのある

العربيه (Arabic)
‏(الاسم) الجو, الغلاف الجوي‏

עברית (Hebrew)
n. - ‮אווירה, אטמוספירה, חלל האוויר, השפעה, יחידת לחץ השווה לממוצע הלחץ האטמוספרי בגובה פני-הים, אווירה נפשית, מצב-רוח, אווירה מתוחה, רגשות הנובעים מהתבוננות בתמונה או האזנה למוסיקה‬

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