Density of air

 ( Atmospheric Thermodynamics ) 

The density of air or atmospheric density, denoted ρ,Rho is widely used as a generic symbol for density is the mass per unit volume of Earth's atmosphere at a given point and time. Air density, like air pressure, decreases with increasing altitude. It also changes with variations in atmospheric pressure, temperature, and humidity. According to the ISO International Standard Atmosphere (ISA), the standard sea level density of air at 101.325 kPa (abs) and is .

At the non-standard sea level temperature of , the density would decrease to . This is about that of water with a density of about .

Air density is a property used in many branches of science, engineering, and industry, including aeronautics;Olson, Wayne M. (2000) AFFTC-TIH-99-01, Aircraft Performance FlightICAO, Manual of the ICAO Standard Atmosphere (extended to 80 kilometres (262 500 feet)), Doc 7488-CD, Third Edition, 1993, .Grigorie, T.L., Dinca, L., Corcau J-I. and Grigorie, O. (2010) Aircraft's Altitude Measurement Using Pressure Information:Barometric Altitude and Density Altitude gravimetric analysis;A., Picard, R.S., Davis, M., Gläser and K., Fujii (CIPM-2007) Revised formula for the density of moist air the air-conditioning industry;S. Herrmann, H.-J. Kretzschmar, and D.P. Gatley (2009), ASHRAE RP-1485 Final Report atmospheric research and meteorology;F.R. Martins, R.A. Guarnieri e E.B. Pereira, (2007) O aproveitamento da energia eólica (The wind energy resource).Andrade, R.G., Sediyama, G.C., Batistella, M., Victoria, D.C., da Paz, A.R., Lima, E.P., Nogueira, S.F. (2009) Mapeamento de parâmetros biofísicos e da evapotranspiração no Pantanal usando técnicas de sensoriamento remotoMarshall, John and Plumb, R. Alan (2008), Atmosphere, ocean, and climate dynamics: an introductory text . agricultural engineering (modeling and tracking of Soil-Vegetation-Atmosphere-Transfer (SVAT) models);Pollacco, J. A., and B. P. Mohanty (2012), Uncertainties of Water Fluxes in Soil-Vegetation-Atmosphere Transfer Models: Inverting Surface Soil Moisture and Evapotranspiration Retrieved from Remote Sensing, Vadose Zone Journal, 11(3), .Shin, Y., B. P. Mohanty, and A.V.M. Ines (2013), Estimating Effective Soil Hydraulic Properties Using Spatially Distributed Soil Moisture and Evapotranspiration, Vadose Zone Journal, 12(3), .Saito, H., J. Simunek, and B. P. Mohanty (2006), Numerical Analysis of Coupled Water, Vapor, and Heat Transport in the Vadose Zone, Vadose Zone J. 5: 784–800. and the engineering community that deals with compressed air.Perry, R.H. and Chilton, C.H., eds., Chemical Engineers' Handbook, 5th ed., McGraw-Hill, 1973.

Depending on the measuring instruments used, different sets of equations for the calculation of the density of air can be applied. Air is a mixture of gases and the calculations always simplify, to a greater or lesser extent, the properties of the mixture.

---

Temperature Other things being equal (most notably the pressure and humidity), hotter air is less dense than cooler air and will thus rise while cooler air tends to fall due to buoyancy. This can be seen by using the ideal gas law as an approximation.

---

Dry air The density of dry air can be calculated using the ideal gas law, expressed as a function of temperature and pressure:

where:

• $\backslash rho$, air density (kg/m³)In the SI unit system. However, other units can be used.
• $p$, absolute pressure (Pa)
• $T$, absolute temperature (K)
• $R$ is the gas constant, in joule⋅kelvin⁻¹⋅mol⁻¹
• $M$ is the molar mass of dry air, approximately in kilogram⋅mol⁻¹.
• $k\_\{\backslash rm\; B\}$ is the Boltzmann constant, in joule⋅kelvin⁻¹
• $m$ is the molecular mass of dry air, approximately in kilogram.
• $R\_\backslash text\{specific\}$, the specific gas constant for dry air, which using the values presented above would be approximately in J⋅kg⁻¹⋅K⁻¹.

Therefore:

• At IUPAC standard temperature and pressure (0Celsius and 100kPa), dry air has a density of approximately 1.2754kilogram/m³.
• At 20°C and 101.325kPa, dry air has a density of 1.2041 kg/m³.
• At 70Fahrenheit and 14.696psi, dry air has a density of 0.074887lb/cubic foot.

The following table illustrates the air density–temperature relationship at 1 atm or 101.325 kPa:

---

Humid air The addition of water vapor to air (making the air humid) reduces the density of the air, which may at first appear counter-intuitive. This occurs because the molar mass of water vapor (18g/mol) is less than the molar mass of dry airas dry air is a mixture of gases, its molar mass is the weighted average of the molar masses of its components (around 29g/mol). For any ideal gas, at a given temperature and pressure, the number of molecules is constant for a particular volume (see Avogadro's Law). So when water molecules (water vapor) are added to a given volume of air, the dry air molecules must decrease by the same number, to keep the pressure from increasing or temperature from decreasing. Hence the mass per unit volume of the gas (its density) decreases.

The density of humid air may be calculated by treating it as a mixture of . In this case, the partial pressure of water vapor is known as the vapor pressure. Using this method, error in the density calculation is less than 0.2% in the range of −10 °C to 50 °C. The density of humid air is found by: Shelquist, R (2009) Equations - Air Density and Density Altitude $$\backslash rho\_\backslash text\{humid\; air\}\; =\; \backslash frac\{p\_\backslash text\{d\}\}\{R\_\backslash text\{d\}\; T\}\; +\; \backslash frac\{p\_\backslash text\{v\}\}\{R\_\backslash text\{v\}\; T\}\; =\; \backslash frac\{p\_\backslash text\{d\}M\_\backslash text\{d\}\; +\; p\_\backslash text\{v\}M\_\backslash text\{v\}\}\{R\; T\}$$

where:

• $\backslash rho\_\backslash text\{humid\; air\}$, density of the humid air (kg/m³)
• $p\_\backslash text\{d\}$, partial pressure of dry air (Pa)
• $R\_\backslash text\{d\}$, specific gas constant for dry air, 287.058J/(kg·K)
• $T$, temperature (K)
• $p\_\backslash text\{v\}$, pressure of water vapor (Pa)
• $R\_\backslash text\{v\}$, specific gas constant for water vapor, 461.495J/(kg·K)
• $M\_\backslash text\{d\}$, molar mass of dry air, 0.0289652kg/mol
• $M\_\backslash text\{v\}$, molar mass of water vapor, 0.018016kg/mol
• $R$, gas constant, 8.31446J/(K·mol)

The vapor pressure of water may be calculated from the saturation vapor pressure and relative humidity. It is found by: $$p\_\backslash text\{v\}\; =\; \backslash phi\; p\_\backslash text\{sat\}$$

where:

• $p\_\backslash text\{v\}$, vapor pressure of water
• $\backslash phi$, relative humidity (0.0–1.0)
• $p\_\backslash text\{sat\}$, saturation vapor pressure

The saturation vapor pressure of water at any given temperature is the vapor pressure when relative humidity is 100%. One formula is Tetens equation from Shelquist, R (2009) Algorithms - Schlatter and Baker used to find the saturation vapor pressure is: $$p\_\backslash text\{sat\}\; =0.61078\; \backslash exp\backslash left(\backslash frac\{17.27\; (T-273.15)\}\{T-35.85\}\backslash right)$$ where:

• $p\_\backslash text\{sat\}$, saturation vapor pressure (kPa)
• $T$, temperature (K)

See vapor pressure of water for other equations.

The partial pressure of dry air $p\_\backslash text\{d\}$ is found considering partial pressure, resulting in: $$p\_\backslash text\{d\}\; =\; p\; -\; p\_\backslash text\{v\}$$ where $p$ simply denotes the observed absolute pressure.

---

Variation with altitude

---

Troposphere To calculate the density of air as a function of altitude, one requires additional parameters. For the troposphere, the lowest part (~10 km) of the atmosphere, they are listed below, along with their values according to the International Standard Atmosphere, using for calculation the gas constant instead of the air specific constant:

• $p\_0$, sea level standard atmospheric pressure, 101325Pa
• $T\_0$, sea level standard temperature, 288.15K
• $g$, earth-surface gravitational acceleration, 9.80665m/s²
• $L$, temperature lapse rate, 0.0065K/m
• $R$, ideal (universal) gas constant, 8.31446J/(mol·K)
• $M$, molar mass of dry air, 0.0289652kg/mol

Temperature at altitude $h$ meters above sea level is approximated by the following formula (only valid inside the troposphere, no more than ~18km above Earth's surface (and lower away from Equator)): $$T\; =\; T\_0\; -\; L\; h$$

The pressure at altitude $h$ is given by: $$p\; =\; p\_0\; \backslash left(1\; -\; \backslash frac\{L\; h\}\{T\_0\}\backslash right)^\backslash frac\{g\; M\}\{R\; L\}$$

Density can then be calculated according to a molar form of the ideal gas law: $$$$

 \rho = \frac{p M}{R T}
      = \frac{p M}{R T_0 \left(1 - \frac{Lh}{T_0}\right)}
      = \frac{p_0 M}{R T_0} \left(1 - \frac{L h}{T_0} \right)^{\frac{g M}{R L} - 1}
     

where:

• $M$, molar mass
• $R$, ideal gas constant
• $T$, absolute temperature
• $p$, absolute pressure

Note that the density close to the ground is $\backslash rho\_0\; =\; \backslash frac\{p\_0\; M\}\{R\; T\_0\}$

It can be easily verified that the hydrostatic equation holds: $$\backslash frac\{dp\}\{dh\}\; =\; -g\backslash rho\; .$$

---

Exponential approximation As the temperature varies with height inside the troposphere by less than 25%, and one may approximate: $$$$

  \rho = \rho_0 e^{\left(\frac{g M}{R L} - 1\right) \ln \left(1 - \frac{L h}{T_0}\right)}
 \approx \rho_0 e^{-\left(\frac{g M}{R L} - 1\right)\frac{L h}{T_0}}
       = \rho_0 e^{-\left(\frac{g M h}{R T_0} - \frac{L h}{T_0}\right)}
     

Thus: $$\backslash rho\; \backslash approx\; \backslash rho\_0\; e^\{-h/H\_n\}$$

Which is identical to the isothermal solution, except that H _n, the height scale of the exponential fall for density (as well as for number density n), is not equal to RT₀/ gM as one would expect for an isothermal atmosphere, but rather: $$\backslash frac\{1\}\{H\_n\}\; =\; \backslash frac\{g\; M\}\{R\; T\_0\}\; -\; \backslash frac\{L\}\{T\_0\}$$

Which gives H _n = 10.4km.

Note that for different gasses, the value of H _n differs, according to the molar mass M: It is 10.9 for nitrogen, 9.2 for oxygen and 6.3 for carbon dioxide. The theoretical value for water vapor is 19.6, but due to vapor condensation the water vapor density dependence is highly variable and is not well approximated by this formula.

The pressure can be approximated by another exponent: $$$$

     p = p_0 e^{\frac{g M}{R L} \ln \left(1 - \frac{L h}{T_0}\right)}
 \approx p_0 e^{-\frac{g M}{R L}\frac{L h}{T_0}}
       = p_0 e^{-\frac{g M h}{R T_0}}
     

Which is identical to the isothermal solution, with the same height scale . Note that the hydrostatic equation no longer holds for the exponential approximation (unless L is neglected).

H _p is 8.4km, but for different gasses (measuring their partial pressure), it is again different and depends upon molar mass, giving 8.7 for nitrogen, 7.6 for oxygen and 5.6 for carbon dioxide.

---

Total content Further note that since g, Earth's gravitational acceleration, is approximately constant with altitude in the atmosphere, the pressure at height h is proportional to the integral of the density in the column above h, and therefore to the mass in the atmosphere above height h. Therefore, the mass fraction of the troposphere out of all the atmosphere is given using the approximated formula for p: $$1\; -\; \backslash frac\{p(h\; =\; 11\backslash text\{\; km\})\}\{p\_0\}\; =\; 1\; -\; \backslash left(\backslash frac\{T(11\backslash text\{\; km\})\}\{T\_0\}\; \backslash right)^\backslash frac\{g\; M\}\{R\; L\}\; \backslash approx\; 76\backslash \%$$

For nitrogen, it is 75%, while for oxygen this is 79%, and for carbon dioxide, 88%.

---

Tropopause Higher than the troposphere, at the tropopause, the temperature is approximately constant with altitude (up to ~20km) and is 220K. This means that at this layer and , so that the exponential drop is faster, with for air (6.5 for nitrogen, 5.7 for oxygen and 4.2 for carbon dioxide). Both the pressure and density obey this law, so, denoting the height of the border between the troposphere and the tropopause as U:

$$\backslash begin\{align\}$$

    p &=    p(U) e^{-\frac{h - U}{H_\text{TP}}} =    p_0 \left(1 - \frac{L U}{T_0}\right)^\frac{g M}{R L} e^{-\frac{h - U}{H_\text{TP}}} \\
 \rho &= \rho(U) e^{-\frac{h - U}{H_\text{TP}}} = \rho_0 \left(1 - \frac{L U}{T_0}\right)^{\frac{g M}{R L} - 1} e^{-\frac{h - U}{H_\text{TP}}}
     

\end{align}

---

Composition

---

See also

• Air
• Atmospheric drag
• Lighter than air
• Density
• Atmosphere of Earth
• International Standard Atmosphere
• U.S. Standard Atmosphere
• NRLMSISE-00

---

Notes

---

External links

• Conversions of density units ρ by Sengpielaudio
• Air density and density altitude calculations and by Richard Shelquist
• Air density calculations by Sengpielaudio (section under Speed of sound in humid air)
• Air density calculator by Engineering design encyclopedia
• Atmospheric pressure calculator by wolfdynamics
• target="_blank" rel="nofollow"> Air iTools - Air density calculator for mobile by JSyA
• Revised formula for the density of moist air (CIPM-2007) by NIST

Post Comment