Lidar observations of the temperature profile between 25 and 103 km: Evidence of strong tidal perturbation

Dao, Phan; Farley, R.; Tao, Xin; Gardner, Chester S.

doi:10.1029/95gl02950

Cited by 84 publications

(81 citation statements)

References 5 publications

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“…The ranges of amplitudes for the (2,5) mode were based on values found previously to produce reasonable agreement with the ARIA I wind observations (Parish et al, 2003), and to be consistent with values measured in recent satellite and ground based observations (e.g. Hecht et al, 1998;Karpov 1996;Dao et al, 1995). In this example, the amplitude of the geopotential height variation of the (2,5) tidal mode in the background winds has been varied between 100 m and 300 m, for a tidal phase of 3.0 h LT, where propagating tides are forced at the lower boundary of the CTIP model at 80-km altitude.…”

Section: (25) Tidal Modesupporting

confidence: 87%

Sensitivity studies of the E region neutral response to the postmidnight diffuse aurora

Parish

Lyons

2006

Ann. Geophys.

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Abstract. Measurements of the neutral thermosphere within the postmidnight substorm recovery phase diffuse aurora show very large horizontal winds, and strong vertical structure. Rocket, satellite, and ground based observations during the ARIA (Atmospheric Response in Aurora) campaigns, and earlier dawn side rocket observations, indicate neutral winds of up to 200 m/s, and a characteristic jet-like wind maximum around 110 to 120-km altitude, with strong shears above and below. The observed wind magnitudes are found to have a dependence on geomagnetic activity level, but recent modeling studies suggest that tides which propagate up from the troposphere and stratosphere may play an important role in generating the strong vertical variations in the neutral winds. The relative importance of auroral and tidal forcing in producing the measured wind structure is not known, however. Simulations have been performed using a three dimensional (3-D) high resolution limited area thermosphere model to understand the processes which generate the observed neutral structure within the postmidnight diffuse aurora. Parameters measured during the ARIA I observational campaign have been used to provide auroral forcing inputs for the model. Global background winds and tides have been provided by the CTIP (Coupled Thermosphere Ionosphere Plasmasphere) model. The sensitivity of the response of the neutral atmosphere to changes in different parameters has been examined. Variations in the amplitudes and phases of the propagating tides in the background winds are found to have significant effects on the neutral structure in the E region, and the wind structure below around 110 km is found to be mainly produced by tidal forcing. Changes in the electric field and ion density affect the winds above around 120 km, and the importance of auroral forcing is found to depend on background winds. Variations in the orientation of the aurora relative to the background field, which may be Correspondence to: H. F. Parish (helen@atmos.ucla.edu) caused by changes in the interplanetary magnetic field, are also found to modify the wind structure. When both auroral forcing and propagating tides are included, many of the basic characteristics of the wind structure are displayed, although the great strength of the wind shears is not well reproduced. The strength of the shears may be related to a currently unmodeled process, or to different types of waves.

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Section: (25) Tidal Modesupporting

confidence: 87%

Sensitivity studies of the E region neutral response to the postmidnight diffuse aurora

Parish

Lyons

2006

Ann. Geophys.

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“…The first was initially proposed by Whiteway et al (1995) and basically explains the formation of MIL by turbulent heating. The second goes back to Dao et al (1995) and was summarized e.g., by Meriwether and Gardner (2000) and explains the formation of a MIL via the interaction of tides with gravity waves. Both these scenarios are discussed in detail e.g., in the review article by Meriwether and Gerrard (2004).…”

Section: Discussionmentioning

confidence: 99%

“…2 one can see a downward phase progression of both MILs which is marked by the arrows. Using simple analysis e.g., applied by Dao et al (1995), that is by fitting a polynomial to the temperature profiles and looking on the temperature maxima, one can find that the upper MIL (86 to 89 km at the time of the rocket launch) descends approximately at a rate of 15 km per 12 h. The lower MIL descends with the same speed and is located ∼ 15 km below the upper one. Figure 3 shows temperature measurements obtained with the MLS over the rocket launch site close to the time of the ECOMA09 flight.…”

Section: Lidar Temperature Measurementsmentioning

confidence: 99%

Simultaneous observations of a Mesospheric Inversion Layer and turbulence during the ECOMA-2010 rocket campaign

et al. 2013

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From 19 November to 19 December 2010 the fourth and final ECOMA rocket campaign was conducted at Andøya Rocket Range (69° N, 16° E) in northern Norway. We present and discuss measurement results obtained during the last rocket launch labelled ECOMA09 when simultaneous and true common volume in situ measurements of temperature and turbulence supported by ground-based lidar observations reveal two Mesospheric Inversion Layers (MIL) at heights between 71 and 73 km and between 86 and 89 km. Strong turbulence was measured in the region of the upper inversion layer, with the turbulent energy dissipation rates maximising at 2 W kg⁻¹. This upper MIL was observed by the ALOMAR Weber Na lidar over the period of several hours. The spatial extension of this MIL as observed by the MLS instrument onboard AURA satellite was found to be more than two thousand kilometres. Our analysis suggests that both observed MILs could possibly have been produced by neutral air turbulence

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“…Liu et al (2000) showed that breaking gravity waves can warm the air sufficiently for the formation of MILs if the static stability of the mesosphere had been decreased by a tidal wave. Models and observations have revealed that the upper MILs have an amplitude maximum during the winter at mid-latitudes (Dao et al, 1995;Liu et al, 2000;Meriwether et al, 1998). The occurrence of the lower MILs is a characteristic and persistent feature of the winter mesosphere and lower thermosphere (MLT) (Hauchecorne et al, 1987;Meriwether and Gardner, 2000).…”

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confidence: 99%

Statistical analysis of the mesospheric inversion layers over two symmetrical tropical sites: Réunion (20.8° S, 55.5° E) and Mauna Loa (19.5° N, 155.6° W)

et al. 2017

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Abstract. In this investigation a statistical analysis of the characteristics of mesospheric inversion layers (MILs) over tropical regions is presented. This study involves the analysis of 16 years of lidar observations recorded at Réunion (20.8° S, 55.5° E) and 21 years of lidar observations recorded at Mauna Loa (19.5° N, 155.6° W) together with SABER observations at these two locations. MILs appear in 10 and 9.3 % of the observed temperature profiles recorded by Rayleigh lidar at Réunion and Mauna Loa, respectively. The parameters defining MILs show a semi-annual cycle over the two selected sites with maxima occurring near the equinoxes and minima occurring during the solstices. Over both sites, the maximum mean amplitude is observed in April and October, and this corresponds to a value greater than 35 K. According to lidar observations, the maximum and minimum mean of the base height ranged from 79 to 80.5 km and from 76 to 77.5 km, respectively. The MILs at Réunion appear on average ∼ 1 km thinner and ∼ 1 km lower, with an amplitude of ∼ 2 K higher than Mauna Loa. Generally, the statistical results for these two tropical locations as presented in this investigation are in fairly good agreement with previous studies. When compared to lidar measurements, on average SABER observations show MILs with greater amplitude, thickness and base altitudes of 4 K, 0.75 and 1.1 km, respectively. Taking into account the temperature error by SABER in the mesosphere, it can therefore be concluded that the measurements obtained from lidar and SABER observations are in significant agreement. The frequency spectrum analysis based on the lidar profiles and the 60-day averaged profile from SABER confirms the presence of the semi-annual oscillation where the magnitude maximum is found to coincide with the height range of the temperature inversion zone. This connection between increases in the semi-annual component close to the inversion zone is in agreement with most previously reported studies over tropics based on satellite observations. Results presented in this study confirm through the use of the ground-based Rayleigh lidar at Réunion and Mauna Loa that the semi-annual oscillation contributes to the formation of MILs over the tropical region.

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Lidar observations of the temperature profile between 25 and 103 km: Evidence of strong tidal perturbation

Cited by 84 publications

References 5 publications

Sensitivity studies of the E region neutral response to the postmidnight diffuse aurora

Sensitivity studies of the E region neutral response to the postmidnight diffuse aurora

Simultaneous observations of a Mesospheric Inversion Layer and turbulence during the ECOMA-2010 rocket campaign

Statistical analysis of the mesospheric inversion layers over two symmetrical tropical sites: Réunion (20.8° S, 55.5° E) and Mauna Loa (19.5° N, 155.6° W)

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Lidar observations of the temperature profile between 25 and 103 km: Evidence of strong tidal perturbation

Cited by 84 publications

References 5 publications

Sensitivity studies of the E region neutral response to the postmidnight diffuse aurora

Sensitivity studies of the E region neutral response to the postmidnight diffuse aurora

Simultaneous observations of a Mesospheric Inversion Layer and turbulence during the ECOMA-2010 rocket campaign

Statistical analysis of the mesospheric inversion layers over two symmetrical tropical sites: Réunion (20.8° S, 55.5° E) and Mauna Loa (19.5° N, 155.6° W)

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Statistical analysis of the mesospheric inversion layers over two symmetrical tropical sites: Réunion (20.8° S, 55.5° E) and Mauna Loa (19.5° N, 155.6° W)