Density of air

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The density of air, ρ (Greek: rho) (air density), is the mass per unit volume of Earth's atmosphere, and is a useful value in aeronautics. In the SI system it is measured as the number of kilograms of air in a cubic meter (kg/m³). At sea level and at 20 °C dry air has a density of approximately 1.2 kg/m³. varying with pressure and temperature. Air density and air pressure decrease with increasing altitude.

Contents

1 Effects of temperature and pressure
2 Effect of water vapor
3 Effects of altitude
4 Importance of temperature
5 See also
6 External links

Effects of temperature and pressure

The formula for the density of air is given by:

[\rho = \frac]

where ρ is the air density, p is pressure, R is the gas constant, and T is temperature.

The individual gas constant R for dry air is:

[R_\mathrm = 287.05 \frac} \cdot \mbox}]

Therefore:

At standard temperature and pressure (0 °C and 101.325 kPa), dry air has a density of ρ_STP = 1.293 kg/m³.
At standard ambient temperature and pressure (25 °C and 100 kPa), dry air has a density of ρ_SATP = 1.168 kg/m³.
At standard ambient temperature and pressure (70 °F and 14.696 psia), dry air has a density of ρ_STP = 0.075 lb_{m_/ft³.}

Effect of water vapor

The addition of water vapor to air (making the air humid) reduces the density of the air, which may at first appear contrary to logic.

This occurs because the molecular mass of water (18) is less than the molecular mass of air (around 29). For any gas, at a given temperature and pressure, the number of molecules present is constant for a particular volume. So when water molecules (vapor) are introduced to the air, the number of air molcules must reduce by the same number in a given volume, without the pressure or temperature increasing. Hence the mass per unit volume of the gas decreases, hence the density reduces.

The magnitude of the effect is determined according to the absolute humidity rather than the relative humidity.

Effects of altitude

To calculate the density of air as a function of altitude, one requires additional parameters. They are listed below, along with their values according to the International Standard Atmosphere, using the universal gas constant instead of the specific one:

sea level atmospheric pressure p₀ = 101325 Pa = 1013.25 mbar or hPa = 101.325 kPa (= 101325 kg/(m*s²))
sea level standard temperature T₀ = 288.15 K
Earth-surface gravitational acceleration g = 9.80665 m/s².
temperature lapse rate L = −0.0065 K/m
universal gas constant R = 8.31447 J/(mol·K)
molecular weight of dry air M = 0.0289644 kg/mol

Temperature at altitude h metres above sea level is given by the following formula (only valid below the tropopause):

[T = T_0 + L \cdot h]

The pressure at altitude h is given by:

[p = p_0 \cdot \left(1 + \frac \right)^\frac]

Density can then be calculated according to a molar form of the original formula:

[\rho = \frac]

Importance of temperature

The below table demonstrates that the properties of air change significantly with temperature.

Table — speed of sound in air c, density of air ρ, acoustic impedance Z vs. temperature °C
Impact of temperature
°C c in m/s ρ in kg/m³ Z in Pa·s/m
- 10 325.4 1.341 436.5
- 5 328.5 1.316 432.4
0 331.5 1.293 428.3
+ 5 334.5 1.269 424.5
+ 10 337.5 1.247 420.7
+ 15 340.5 1.225 417.0
+ 20 343.4 1.204 413.5
+ 25 346.3 1.184 410.0
+ 30 349.2 1.164 406.6

Impact of temperature
°C	c in m/s	ρ in kg/m³	Z in Pa·s/m
- 10	325.4	1.341	436.5
- 5	328.5	1.316	432.4
0	331.5	1.293	428.3
+ 5	334.5	1.269	424.5
+ 10	337.5	1.247	420.7
+ 15	340.5	1.225	417.0
+ 20	343.4	1.204	413.5
+ 25	346.3	1.184	410.0
+ 30	349.2	1.164	406.6

External links