The uppermost layer of the Earth's atmosphere, the thermosphere, extends from ∼90 up to ∼600 km (e.g., Kato, 2007;Richmond, 1983). Early studies evaluated densities of the thermosphere based on the measurement of orbital decay of artificial satellites. Jacchia (1965) developed a global empirical model of thermospheric densities under the assumption of diffusive equilibrium. A by-product of the model was an estimate of the global distribution of air pressure. Theoretical studies found that the model pressure provides useful information for evaluating the global wind system in the thermosphere (Geisler, 1967;Kohl & King, 1967). It has been demonstrated that global motion of the air above approximately 150 km is primarily driven by solar-induced pressure gradients. That is, horizontal winds blow from the higher-temperature (and higher-pressure) dayside to the lower-temperature (and lower-pressure) nightside. On the other hand, the motion of the air in the lower thermosphere (<150 km) is often dominated by waves from the lower layers of the atmosphere. In particular, atmospheric tides (e.g., Lindzen & Chapman, 1969) are known to play an important role in the meteorology of the mesosphere and lower thermosphere.Theoretical models of the thermosphere were developed and used to explain how solar heating, as well as Joule heating in the polar region, drives the global circulation of the thermosphere under different seasonal conditions (e.g.,