Longitude features shown by topside sounder data and their importance in ionospheric mapping

Ben'kova, N. P.; Dëminov, M. G.; Karpachev, A. T.; Kochenova, N. A.; Kusnerevsky, Yu.V.; Migulin, V. V.; Пулинец, С. А.; Fligel, M. D.

doi:10.1016/0273-1177(90)90186-4

Cited by 16 publications

(8 citation statements)

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“…We note that the presence of the wavelike density structure was identified earlier by topside soundings from the Russian satellite Intercosmos‐19 [ Kochenova , 1987, 1988; Karpachev , 1988; Benkova et al , 1990; Karpachev et al , 2003; Deminova , 2003, 2007]. The daytime morphologies of the upward drift velocity, electric field, and equatorial electrojet that were calculated using the latitudinal profile of the F peak electron density [ Benkova et al , 1990] showed a good agreement with the recent observations. Their observation of the equatorial electron density minima at the peak locations of the upward E × B drift can be explained by the transport of the equatorial plasma to higher latitudes by the fountain effect.…”

Section: Introductionsupporting

confidence: 86%

Wave structures of the plasma density and vertical E × B drift in low‐latitude F region

et al. 2008

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[1] We investigate the seasonal, longitudinal, local time (LT), and altitudinal variations of the F region morphology at low latitudes using data from the first Republic of China satellite (ROCSAT-1), Global Ultraviolet Imager (GUVI), on board the Thermosphere Ionosphere Mesosphere Energetics and Dynamics (TIMED) satellite, and the Defense Meteorological Satellite Program (DMSP) F13 and F15 satellites. Signatures of the longitudinally periodic plasma density structure emerge before 0900 LT. The wave structure is established before noon and further amplified in the afternoon. The amplitudes of the wave structure start to diminish in the evening. The wave-4 structure is clearly distinguishable during equinox and northern hemisphere summer. During northern hemisphere winter, the density structure can be characterized to either wave-4 or wave-3 structure owing to marginal separation of the two peaks in 180°-300°E. Observations of similar density structures from ROCSAT-1 (600 km) and DMSP (840 km) at 0930 and 1800 LT indicate the extension of the wave structure to altitudes greater than 840 km. The daytime wave structure persists into the night during the equinoxes but is significantly modified during the solstices. The modification is more significant at higher altitudes and is attributed to the effects of interhemispheric winds and the prereversal enhancement. The formation of the wavelike density structure in the morning and its temporal evolution in the afternoon show a close association with the vertical E Â B drift. We conclude that the E Â B drift during 0900-1200 LT determines the formation of the wavelike density structure.

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Section: Introductionsupporting

confidence: 86%

Wave structures of the plasma density and vertical E × B drift in low‐latitude F region

et al. 2008

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“…This wave number N longitudinal structure means that there exist quasiperiodic N e peaks along longitudinal direction when the global N e map is drawn at a specific local time in the dayside. Benkova et al [] observed this longitudinal structure according to the local time and altitude. Sagawa et al [] identified the WN‐4 pattern in the observations of the far ultraviolet imager on board the IMAGE satellite.…”

Section: Introductionmentioning

confidence: 90%

Variation of the topside ionosphere during the last solar minimum period studied with multisatellite measurements of electron density and temperature

et al. 2016

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Using the ionospheric measurements of CHAMP, DEMETER, and DMSP F15, the seasonal and spatial variations of the topside ionosphere during the last solar minimum period were investigated and compared with ionospheric models. In all the satellite measurements, equatorial ionization anomaly (EIA) shows clearly longitudinal asymmetry with wave number −3 or −4 patterns. Anomalous increases of Ne in the nighttime surpassing daytime Ne, known as the Weddell Sea anomaly (WSA) or midlatitude summer nighttime anomaly (MSNA), were also observed in the global Ne distribution with differences in detailed geometry of the geomagnetic field according to the altitude. In the nighttime ionosphere, the reduced Te in the equatorial region at the DMSP altitude, identified as the equatorial plasma temperature anomaly (EPTA), was ascribed to the leftover of the prereversal enhancement of the upward plasma drift. Though the EIA, WSA, MSNA, and EPTA are all associated with the upward plasma movement, the difference in the thermal evolution is ascribable to the geometry of drift in which the plasma moves across the geomagnetic field line for the EIA and the EPTA, while along the field line for the WSA and the MSNA.

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“…The wave‐like longitudinal plasma density pattern was first reported by topside soundings from the Russian satellite Intercosmos‐19 [ Kochenova , 1987, 1988; Karpachev , 1988]. Intercosmos‐19 observed the formation of four peaks in plasma density (WN4 structure at a fixed local time) over the magnetic equator [ Benkova et al , 1990], but the focus of this study was on the displacement of the geomagnetic equator from the geographic equator and the hemispheric asymmetry induced by neutral winds.…”

Section: Introductionmentioning

confidence: 92%

Global ionospheric response to nonmigrating DE3 and DE2 tides forced from below

Mukhtarov

Pancheva

2011

J. Geophys. Res.

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[1] In this paper we present the global spatial structure and seasonal variability of the COSMIC electron density response to the forced from below DE3 and DE2 tides during the period January 2008 to March 2009. The COSMIC electron density at fixed altitudes and SABER temperatures were utilized in order to define the ionospheric DE3 and DE2 tidal response to the DE3 and DE2 temperature tides coming from below. The tidal waves from both data sets have been extracted by the same data analysis method. The latitude structure of the ionospheric response for heights up to 450-500 km is distributed on both sides of the dip equator at about ±30°modified dip latitude; above 500 km the response is approximately confined over the equator. Two altitude regions of enhanced ionospheric response are found: an upper level response (above 300 km) and a bottom level one (below 250 km); the two regions are separated by a narrow altitude zone with no tidal response. The different phase structure of the ionospheric response in both altitude regions suggests that (1) the upper level response is mainly due to the DE3/DE2 modulated vertical plasma drift and (2) the bottom level response is complex and, in all likelihood, is caused by more than one mechanism.Citation: Mukhtarov, P., and D. Pancheva (2011), Global ionospheric response to nonmigrating DE3 and DE2 tides forced from below,

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Longitude features shown by topside sounder data and their importance in ionospheric mapping

Cited by 16 publications

References 1 publication

Wave structures of the plasma density and vertical E × B drift in low‐latitude F region

Wave structures of the plasma density and vertical E × B drift in low‐latitude F region

Variation of the topside ionosphere during the last solar minimum period studied with multisatellite measurements of electron density and temperature

Global ionospheric response to nonmigrating DE3 and DE2 tides forced from below

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