Introduction to Flight Testing. James W. Gregory

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Integration of Eq. (2.18) gives the pressure ratio as a function of the temperature ratio, i.e.,

(2.19)

where p_ref and T_ref are the pressure and temperature at a reference altitude, respectively. Again applying the ideal gas law, Eq. (2.14), the density ratio is given by

(2.20)

Thus, for regions of the atmosphere with linear temperature lapse rates, Eqs. (2.10), (2.12), (2.19), and (2.20) form a complete description of the temperature, viscosity, pressure, and density variation with altitude. The reference condition for the base of each region is simply the values corresponding to the top of the previous (lower) region.

      In the flight testing community and elsewhere, we often express the above ratios as specific variables referenced to sea level conditions. Temperature ratio, pressure ratio, and density ratio are defined as

(2.21)

In the standard atmosphere, sea level conditions are defined as T_SL = 288.15 K, p_SL = 101.325 kPa, and ρ_SL = 1.225 kg/m³, where the subscript “SL” denotes sea level. The ratios defined in Eq. (2.21) still satisfy the ideal gas law, giving

      (2.22)

      It is important to bear in mind that these equations are a function of geopotential altitude, which presumes constant gravitational acceleration. If properties are desired as a function of geometric altitude, then the corresponding geometric altitudes can be found by solving for h_G in Eq. (2.9).

      2.2.6 Operationalizing the Standard Atmosphere

      Applying the equations developed above, we can take one of several approaches to implementing the standard atmosphere for flight testing work. Most simply, these equations form the basis for tabulated values of the standard atmosphere, which are tabulated by NOAA et al. (1976) or ICAO (1993). In addition, a limited subset of the U.S. Standard Atmosphere (NOAA et al. 1976) is reproduced in Appendix A. Alternatively, pre‐written standard atmosphere computer codes may be downloaded and used in a straightforward manner. Popular examples include the MATLAB code by Sartorius (2018) or the Fortran code by Carmichael (2018). If these are not suitable for a particular purpose, then custom code can be written, as described below in a form that simplifies the coding.

      In the troposphere where the temperature gradient is a = dT/dh = − 6.5 K/km, the temperature distribution in Eq. (2.10) can be expressed as a linear function

      (2.23)

      where h is the geopotential altitude and k = 2.256 × 10⁻⁵ m⁻¹ = 6.876 × 10⁻⁶ ft⁻¹ is a decaying rate. According to Eqs. (2.19) and (2.20), the pressure ratio and density ratio in the troposphere (0 ≤ h ≤ 11 km) are given by

      (2.24)

      and

      (2.25)

      where n = − g₀/aR = 5.2559.

Figure 2.4 The normalized temperature, pressure, and density distributions in the standard atmosphere.

In the lower stratosphere (11 km < h ≤ 20 km), the atmospheric temperature is constant at 216.65 K. If we define the critical altitude at the tropopause to be h_trop = 11 km, then the temperature and pressure ratios at the tropopause are θ_trop = 0.7518 and δ_trop = 0.2233, respectively. Recasting (2.16) in terms of these ratios, we obtain

      (2.26)

      for the pressure ratio in the lower stratosphere. Finally, the density ratio in the lower stratosphere is simply found by the ideal gas law,

      (2.27)

Figure 2.4 shows the pressure, density, and temperature distributions normalized by the sea level conditions in the standard atmosphere.

      2.2.7 Comparison with Experimental Data

      The above equations describe the idealized atmosphere where the parameters

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