Corresponding author: J. Y-K. Cho, School of Physics and Astronomy, Queen Mary University of London, London, United Kingdom. (J.Cho@qmul.ac.uk)
 Data from the Galileo Probe, collected during its descent into Jupiter's atmosphere, is used to obtain a vertical profile of the zonal wind from ~0.5 bar (upper troposphere) to ~0.1 µbar (lower thermosphere) at the probe entry site. This is accomplished by constructing a map of gravity wave Lomb-Scargle periodograms as a function of altitude. The profile obtained from the map indicates that the wind speed above the visible cloud deck increases with height to ~150 m s-1 and then levels off at this value over a broad altitude range. The location of the turbopause, as a region of wide wave spectrum, is also identified from the map. In addition, a cross-equatorial oscillation of a jet, which has previously been linked to the QQO in the stratosphere, is suggested by the profile.
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 The horizontal structure of Jupiter's zonal (east-west) winds at the level of the visible cloud deck on Jupiter has been observed for many decades [e.g., Limaye, 1992; Ingersoll et al., 2004; García-Melendo and Sánchez Lavega, 2001; Vasavada and Showman, 2005; Li et al., 2006]. In contrast, the vertical structure of zonal winds is not well known—especially away from the cloud deck and in the equatorial region. This is because of the lack of usable tracers and the breakdown of the thermal wind relation near the equator, preventing latitudinal temperature measurements to be related to the vertical wind shear.
 In December 1995, the Galileo probe entered Jupiter's upper atmosphere at 6°N, above a 5 µm hot spot in the north equatorial belt. During the descent, the Atmospheric Structure Instrument on-board collected information about the density, pressure, and temperature of the atmosphere [Seiff et al., 1998]. Analysis of the temperature profile in the thermospheric and stratospheric regions identified discernible perturbations that have been interpreted as manifestations of internal, or vertically propagating, gravity waves [Young et al., 1997, 2005; Matcheva and Strobel, 1999]. Vertical temperature profiles for Jupiter's atmosphere have also been obtained from occultation studies using stars and other spacecraft. A number of these profiles contain oscillations that have been characterized as manifestations of internal gravity waves as well [French and Gierasch, 1974; Lindal, 1986; Hubbard et al., 1995; Raynaud et al., 2003, 2004].
 Gravity waves are oscillations of fluid parcels about their altitudes of neutral buoyancy [Gossard and Hooke, 1975]. The waves are a common feature of stably stratified atmospheres. They have been captured in images of Jupiter's clouds, typically near the planet's equator [Flasar and Gierasch, 1986; Arregi et al., 2009; Reuter et al., 2007]. Figure 1 shows an example. Internal gravity waves (hereafter simply gravity waves) grow in amplitude due to the fall in background atmospheric density. The dynamics of such waves is described by the Taylor–Goldstein equation [Taylor, 1931; Goldstein, 1931]:
 Here, w is the perturbation in the vertical wind, which is adjusted for the amplitude growth and also assumed to be oscillatory (wave-like) in the horizontal direction and time; F is a function that represents the source and dissipation of waves; and m is the vertical wave number, which depends on the physical properties of the medium in which the waves propagate. Specifically,
where N is the Brunt–Väisälä (buoyancy) frequency; I is the intrinsic phase speed, c – u0, where c is the horizontal phase speed and u0 is the zonal wind; H is the density scale height; and k is the horizontal wave number. In general, all of the variables depend on altitude z. Crucially, the zonal wind profile u0(z) can be obtained by solving for I = I(H, k, N, m) in equation ((2)). In this letter, we present a profile from this inversion that span much larger range of altitude above the 1 bar level (range of ~500 km) than in past analyses.
 For the inversion, we compute H from the collected density profile. We also use k = 2π/300 km-1 from the average value obtained in analysis of Voyager images [Flasar and Gierasch, 1986]. Other analyses have reported slightly different values [e.g., average of 2π/165 km-1 by Arregi et al., 2009]; however, as long as k2 ≪ m2 (as is the case here), the value of k does not significantly alter the result of the inversion. N and m are obtained from the potential temperature, θ = T(pref/p)κ, related to specific entropy of the atmosphere; here, T is the temperature, p is the pressure, pref = 1 bar is a constant reference pressure, and κ = R/cp with R as the specific gas constant and cp as the specific heat at constant pressure. To obtain N and m, we decompose θ into a mean background (extracted using a spatially moving fitting window) and a small perturbation Δθ about the mean (presumed caused by mesoscale gravity waves). Such decomposition of temperature is standard in gravity wave studies [Lindzen, 1990; Nappo, 2002; Young et al., 1997], and is reasonable here given that the spatial scales of the background and waves are well separated. Further, the horizontal distance traveled by the probe in the region studied (3300 km) is small compared with Jupiter's circumference and is completely within the hot spot entered by probe [Orton et al., 1998]; hence, zonal variation in the background over this distance is not expected to be significant.
 Figure 2a shows the relative perturbation, Δθ/, resulting from a 75-km-wide moving window. We have checked that the result is not affected by the choice of window size by varying the size from 55 to 85 km. Figure 2b shows resulting from the decomposition; here, g = g(z) is the gravity. In the figure, note that N is much smaller in the region below ~20 km than that above (the stratosphere)—in agreement with Magalhães et al. , whose observations give N ≈ 6 × 10-3 s-1 in the lower region. This represents a possible ducting region, a source for the waves in the probe data.
 Although w information was not collected by the probe, m(z) can still be obtained from Δθ through the polarization relation [e.g., Watkins and Cho, 2010]. For this, we generate a series of Lomb-Scargle periodograms [Scargle, 1982] of the Δθ data, which is nonuniformly spaced in z. The nonuniform spacing renders analysis by standard Fourier or wavelet transforms unsuitable. One periodogram at each z is generated using a smoothing window. We have also verified in this procedure that the obtained result varies little between different sized smoothing windows. All the periodograms are subsequently combined to produce a two-dimensional map of the wave spectral energy density as a function of wave number and altitude, = (m*, z), shown in Figure 3; here, m* is the vertical wave number m before an adjustment for wave propagation geometry. Before discussing this adjustment, we discuss three features that are already apparent in the map.
 First, gravity waves identified previously [Young et al., 2005] are recovered (W1 and W2 in the map). This agreement gives confidence in our procedure. In addition to those waves, we identify in our analysis new gravity waves throughout the analyzed domain. In particular, note the high-energy density (dark red) regions near the 50, 300, and 400 km altitudes all with m* ≈ 0.25. These constitute new waves.
 Second, we identify a region consistent with a turbopause ~50 km thick, centered at approximately 400 km altitude. This is the region where the width of the subspectrum containing significant energy increases markedly. In this region, molecular diffusion becomes comparable with eddy diffusion and gravity waves—growing in amplitude as they propagate upward—break, transferring energy into the higher wave numbers. Above this region, energy is lower across the entire spectrum and the spectrum itself is much steeper (i.e., narrower) than that for the turbopause region. Above the turbopause region, the atmosphere becomes inhomogeneous, separating out into layers of different molecular species. Past studies have placed Jupiter's turbopause at the ~5 µbar [Festou et al., 1981] and ~0.5 µbar [Yelle et al., 1996] levels based on observations and modeling. Our result supports the latter location.
 Third, in the lower part of the analyzed domain, there appears to be a ducting region, a region with a sharp jump in N. As already noted, such a region can serve as a source of gravity waves. Horizontally propagating gravity waves in this region have previously been observed (see, e.g., Figure 1), which have been suggested as waves trapped in a “leaky” duct. The ducted wave travels horizontally by undergoing internal reflections at the boundaries; however, part of the wave escapes the duct to propagate vertically. Because the wave number with maximum energy in the map can be traced down to the ducting region, it is likely that the waves have come from there.
 Note that, above the ducting region, the number of local peaks in the spectrum generally reduces with altitude (the centroid of the spectrum at each height is shifted to lower wave number). Also, the magnitude of the peak energy in the low wave number (white line in Figure 3) is high at first, then decreases, and then increases again along the white line, until the topside of the turbopause region at ~425 km above the 1 bar level. This is indicative of wave saturation or encounters with a critical layer, where I = 0 locally, for high number wave numbers as they propagate upward. The second or third multipeaked altitude regions, between ~200 and ~300 km above the 1 bar level, may be due to wave breaking and secondary wave generation from breaking layers.
 As alluded to earlier, m* differs from the required wave number m. The latter is the wave number that would be observed by a probe traveling in a vertical direction. However, throughout most of its entry phase, the probe had a shallow angle of attack (~7° below the horizontal), which changes the wave number observed by the probe during its passage in the upper part of the analyzed domain. We use the geometry of the probe's path to obtain the true vertical wave number,
where γ is the angle of attack and β is the angle the wave vector makes with the horizontal. We make no correction for the relative motion of the probe with respect to the wave because the probe's velocity is supersonic (indeed, hypersonic, with up to Mach 51) for much of the entry phase. Gravity wave phase speeds are subsonic.
 Although γ = γ(z) is known from the probe's trajectory [Seiff et al., 1998], β is not. To estimate this quantity, we assume that the probe's trajectory is vertical in the period just before parachute deployment. This is not far from the actual situation since the probe's angle of attack was 83° just before the parachute was deployed, near the lower boundary of our domain. In this region, m* ≈ m, and since
we have β ≈ 85°. Also, in this region, m ≈ 0.25 km-1 (giving vertical wavelength of ≈25 km), in good agreement with previously recovered values [Magalhães et al., 2002; Arregi et al., 2009]. Now, all the parameters required to recover I have been obtained, and a vertical profile for I can be estimated.
 Finally, to obtain μ0 from I, a value for the horizontal phase speed c is required. This is not well known. However, equatorial gravity waves with a phase speed of about 100 m s-1 greater than the winds have been observed in images of Jupiter's clouds returned by New Horizons [Reuter et al., 2007]. This gives c ≈ 180 m s-1. The Doppler Wind Experiment (DWE) on the probe has measured the zonal winds to be approximately this speed in the deeper atmosphere [Atkinson et al., 1998], suggesting that the waves could have been driven by convective overshoot below the clouds. This value also agrees well with the 140–195 m s-1 range reported for the similar region, at the probe entry site [Magalhães et al., 2002]. Somewhat smaller values (approximately 70–145 m s-1) have been obtained for waves at different longitudes [Arregi et al., 2009]. Such variation in c does not change the shape of the μ0 profile we recover, but the magnitude would be reduced. Variations of c with altitude would increase the uncertainty as well, but they are expected to be small and not fundamentally change the profile. This gives the profile for μ0(z) shown in Figure 4a. Here, we have used c = 180 m s-1. The standard deviation shown indicates the variation in the profile given by the various smoothing window sizes considered in constructing .
 The DWE reported flow speeds that increase with depth reaching 170 m s-1 at the 5 bar level and then remaining high at lower levels [Atkinson et al., 1998]. The upper part of the DWE profile is shown in Figure 4a. The wind speed at the bottom of our profile agrees well with that at the top of the DWE profile. Our profile shows increasing zonal wind speed with altitude (up to ~100 km above the 1 bar level). This implies that the wind speed is a minimum near the cloud-top level. This is similar to what has been observed from studies using the thermal wind equation [Flasar et al., 2004; Simon-Miller et al., 2006]. However, in our profile, this high-speed wind is not a jet, as the zonal wind speed does not diminish appreciably with altitude near this level. In fact, the speed is roughly constant throughout the stratosphere, starting from this level. There are some fluctuations of the order of 20 m s-1 in the wind speed in the thermosphere. The Richardson number, Ri = N2(dμ0/dz)-2, is greater than 1/4 for the entire profile, which indicates the flow is stable with respect to Kelvin–Helmholtz instability.
 Temporal variations in the temperature profile of Jupiter's equatorial stratosphere have been observed to have a period of 4–5 years and are therefore known as the quasi-quadrennial oscillation (QQO) [Leovy et al., 1991; Friedson, 1999]. These oscillations have been linked to variations in the zonal wind observed via cloud tracking on Jupiter with a period of ~4.4 years [Simon-Miller et al., 2007]. Further, a jet located just north of the equator, derived using the thermal wind equation applied to data gathered in December 2000 and January 2001, has been linked to the QQO [Flasar et al., 2004]. A jet of similar magnitude, just south of the equator, has been observed in observations gathered in 1979 [Simon-Miller et al., 2006] (which fits well with a period of 4.4 years), suggesting that this jet may be oscillating about the equator. No such jet is visible in our profile. However, the probe entered Jupiter's atmosphere 5 years before the northern jet was observed. Thus, our profile is consistent with such an oscillation as the jet would be located south of the equator, away from the probe entry site, at the time the probe entered.
 Gravity wave creation and dissipation is associated with heating and cooling of the atmosphere. Ignoring molecular viscosity, which is only important above the turbopause, the heating rate is proportional to the vertical gradient of energy flux—specifically,
 We estimate the energy flux, , from Δθ using the polarization relations to derive the perturbations in the geopotential φ and the vertical velocity w. The flux comes from the zonal average of the product of these quantities. Because the product is not available to us, we average over a single vertical wavelength instead. The heating rate profile thus obtained is shown in Figure 4b. It can be seen that heating is small through the stratosphere. Indeed, on average, it is very close to zero. It is only in the thermosphere that the average heating rate deviates from zero with a magnitude of ~ 0.5 K per Jupiter rotation. The flux responsible for heating in this region is small (Fz < 10−3 W m-2) compared with radiation fluxes measured in the troposphere (3 < Fz < 16 W m-2) [Sromovsky et al., 1998]. Nevertheless, the peak heating rate magnitude is about 50 times larger partly because the lower thermosphere is much less dense than the troposphere.
 The circulation of Jupiter's stratosphere is important for understanding the planet's circulation as a whole. The location of the turbopause is essential for understanding the coupling between Jupiter's upper atmosphere and the circulation in the lower atmosphere. The Juno mission will explore the troposphere of Jupiter to depths of 100 bar or more. This will provide better insight to the source and behavior of gravity waves in the troposphere, possibly allowing better limits to be derived for the wave vector angle β in our analysis and better understanding of the mechanisms that generate the gravity waves. The planned Jupiter Icy Moon Explorer mission will directly study gravity wave activity and zonal winds in the stratosphere of Jupiter, extending the result present here.
 C.W. is supported by the Science and Technology Facilities Council, and J.Y.-K.C. is supported by the Science and Technology Facilities Council PP/E001858/1 grant. The authors acknowledge H. Thrastarson, I. Polichtchouk, and C. Agnor for useful discussions. We thank the reviewers for helpful suggestions.