Mesosphere summer echoes observed with the SuperDARN Hokkaido HF radar at Rikubetsu, Japan (43.5°N)
© The Society of Geomagnetism and Earth, Planetary and Space Sciences (SGEPSS); The Seismological Society of Japan; The Volcanological Society of Japan; The Geodetic Society of Japan; The Japanese Society for Planetary Sciences; TERRAPUB. 2013
Received: 2 May 2013
Accepted: 24 July 2013
Published: 6 December 2013
Using the SuperDARN Hokkaido HF radar located at Rikubetsu in Hokkaido, Japan (43.5°N), we present first oblique-incidence observations of midlatitude mesosphere summer echoes (MSE) at the HF band (HF-MSE). Three HF-MSE events in June 2009 are case-studied. Analyses of HF-MSE data together with VHF and MF radar data obtained at Wakkanai, 260 km northwest of Rikubetsu, indicate the following: (1) in two events HF-MSE were accompanied by MSE at VHF (VHF-MSE), and in one event only HF-MSE were observed. (2) In accordance with southward neutral winds observed with the MF radar, HF-MSE exhibited high Doppler velocities with a maximum of about 60 m/s toward the south, and also HF-MSE regions moved southward with time, suggesting that irregularities and/or cold ice particles responsible for the radar wave scattering might be advected southward from higher latitudes.
Strong radar echoes, called polar mesosphere summer echoes (PMSE), from the cold summer mesopause region at high latitudes have been observed mainly with VHF radars (hereafter called VHF-PMSE) (e.g., Rapp and Lübken, 2004 and references therein; Bremer et al., 2006; Morris et al., 2009). It is believed that mesospheric neutral air turbulence and heavy charged ice aerosol particles are important for the creation of PMSE (Rapp and Lübken, 2004). VHF radar echoes similar to VHF-PMSE have been observed at higher midlatitudes in Germany (e.g., Reid et al., 1989; Latteck et al., 1999), the UK (Thomas et al., 1992), and Japan (Ogawa et al., 2011): these echoes, called mesosphere summer echoes (MSE), appear mainly at the 80-90 km altitudes. Though compared with VHF-PMSE, MSE at VHF (hereafter called VHF-MSE) exhibit rather rare occurrence and weak echo intensity, and appear only during the daytime, VHF-MSE are believed to be also related to the cold mesopause temperature (e.g., Gerding et al., 2007).
VHF radars used for PMSE and MSE observations are usually equipped with vertical and narrow beams, and have an altitude resolution of less than 1 km. Vertical-incidence HF radars have also been used for PMSE detection (e.g., Ramos et al., 2009 and references therein). (Ogawa et al. 2002, 2003) showed that PMSE are also detectable with an oblique-incidence Super Dual Auroral Radar Network (SuperDARN) HF radar (Greenwald et al., 1995; Chisham et al., 2007). This paper presents first MSE observations using a midlatitude SuperDARN radar located at Rikubetsu in Hokkaido, Japan (e.g., Nishitani and Ogawa, 2005) to demonstrate the capability of midlatitude SuperDARN radars for MSE study. This HF radar provides horizontal two-dimensional distribution of MSE regions. However, it has a wide beam width in the vertical plane and a coarse range resolution, making it difficult to know exact echo altitudes. To overcome this problem, we use vertical-incidence VHF and MF radars located at Wakkanai in Hokkaido. MSE events observed with both radars in 2000 and 2009 have been reported by Ogawa et al. (2011). By using data from three radars, this paper discusses some new features of midlatitude MSE at HF (HF-MSE).
The VHF and MF radars are located at Wakkanai (45.4°N, 141.8°E), about 260 km northwest of Rikubetsu (Fig. 1): see Ogawa et al. (2011) for the main technical parameters of both radars. In brief, the 46.5-MHz VHF radar with a peak power of 80 kW is equipped with 144 three-element Yagis for transmission and reception, and has a beam width of 6° in the vertical. The altitude and time resolutions are 600 m and 3 min, respectively. The collocated 1.96-MHz MF radar with a peak power of 50 kW is equipped with four crossed-dipole antennas for transmission and reception, and has a beam width of about 40° in the vertical, and altitude and time resolutions of 2 km and 6 min, respectively. Horizontal winds are derived by using the conventional full correlation analysis method. Both radars detect echoes from a common volume over Wakkanai.
Figure 2(c) shows two-dimensional Doppler velocity maps at 0718 and 0802 JST. In the 0718 JST map, the high velocity region was localized at ground ranges of 495-675 km on beams 0–4. This high velocity region moved southward with time, as can be observed in Figs. 2(a) and 2(b), and at 0802 JST it was located mainly at ranges of 315–540 km on beams 0–7. After 0802 JST this high velocity region continued to move southward.
It is difficult to know exact echo altitudes from the current HF radar observations because the radar has the broad beam width (~ 30°) in the vertical plane and the coarse range resolution (45 km). Here, we consult with VHF and MF radar data obtained at Wakkanai (Ogawa et al., 2011). Figure 3(a) displays altitude-time plot of the signal-to-noise ratios (SNR) observed with the VHF radar on the same day. After the short-lived, weak echoes at the 86–87 km altitudes at around 0820 JST, there appears a long-lasting (~ 4 hours) echo layer with a thickness of less than 3 km. The layer altitudes are modulated due to short-period atmospheric gravity waves (AGW) with a period of about one hour, and descend gradually with time at about 0.3 m/s due to tides (Ogawa et al., 2011). The RTV plot on the HF radar beam 1 is shown in Fig. 3(b), where the strong HF echoes with high positive velocities exist only at 0745–0820 JST before the VHF-MSE appearance at around 0820 JST. Note that the HF echo region at ranges of 300–450 km at around 0800 JST is located at about 150–250 km east-northeast of Wakkanai (see Fig. 2(c)). The horizontal wind vectors, averaged over 18 min, observed with the MF radar are plotted in Fig. 3(c) where the VHF-MSE areas in Fig. 3(a) are marked by rectangles. When VHF-MSE appear at altitudes of 84–89 km at around 0820 JST and after 1000 JST, the winds at the same altitudes have southward (equatorward) component with a maximum of about 50 m/s except for the period of 1000-1100 JST. Nearly simultaneous occurrence of VHF-MSE at the 86–87 km altitudes and HF-MSE during 0745–0820 JST suggest that the HF-MSE altitudes are also 86–87 km or 84–89 km where the winds advecting echo targets are southward to cause the positive Doppler velocities of HF-MSE.
The second simultaneous VHF- and HF-MSE event on 29 June 2009 is shown in Figs. 3(d) and 3(e). In Fig. 3(d) VHF-MSE also modulated with short-period AGW appear at 83–90 km altitudes. Figure 3(e) displays RTV plots of the HF radar echoes (with echo power higher than 10 dB) observed on beams 0, 2, 12 and 14. There appear high positive velocities with a maximum of about 50 m/s at ranges of 270–400 km during 0600–0730 JST on beams 12 and 14 (also on beams 10,11,13 and 15; not shown), and during 0930-1010 JST on beams 0 and 2 (also on beams 1 and 3–6; not shown). HF-MSE on beams 10–15 appear around the start of VHF-MSE, and those on beams 0–6 do during 0930-1010 JST when VHF-MSE subside for a while. The HF-MSE region on beams 10–15 is located at about 200-300 km east of Wakkanai and that on beams 0–6 at about 150–250 km east-northeast of it. It is noted that foE s over Sarobetsu was less than 6 MHz during the HF-MSE event in Fig. 3(e), and that there appear no signatures of coherent echoes due to E s -FAIs in this figure. The meridional winds at 84–88 km altitudes during 0900–1200 JST are southward with a maximum of about 40 m/s (not shown), in line with the positive Doppler velocities of HF-MSE. Unfortunately, the wind data before 0900 JST are not available.
In the above-mentioned two events, the HF-MSE occurrences are clearly related to VHF-MSE ones. In some cases, HF-MSE (VHF-MSE) were observed without any signatures of VHF-MSE (HF-MSE). As an example, Figs. 4(a) and 4(b) display an HF-MSE event, not accompanied by VHF-MSE, on 16 June 2009. Figure 4(a) shows RTV plot (with echo power higher than 20 dB) observed on the HF radar beams 1, 3, 5, 11, 13 nd 15. The radar frequency and range resolution are 9.1 MHz and 15 km, respectively. Clearly, the echo regions with high positive Doppler velocities with a maximum of about 60 m/s move southward with time and away from the radar FOV after 0800 JST. It is discernible from Fig. 4(b) that the main echo region exists at ranges of 285–480 km on beams 0–9 at 0715 JST and at ranges of 225–300 km on beams 0–14 at 0735 JST. Noteworthy is that foEs over Sarobetsu was less than 7 MHz during 0630–0800 JST, and that no signatures of coherent echoes due to Es -FAIs are discernible in Figs. 4(a) and 4(b). In Fig. 4(c) the meridional winds (averaged over 12 min) at 82–88 km during 0700–0800 JST are mostly southward.
It is noted that the high Doppler velocities appearing in Figs. 4(a) and 4(b) have strong echo powers, as demonstrated in Fig. 2, and narrow spectral widths of less than 10 m/s (not shown): HF-MSE in Figs. 2 and 3(e) also have such narrow spectral widths.
4. Discussion and Summary
We have presented three examples of HF-MSE observations in June 2009 with the SuperDARN Hokkaido radar. HF-MSE on 30 June (Fig. 2) and 29 June (Fig 3(e)) are related to VHF-MSE over Wakkanai, 260 km northwest of Rikubetsu. Ogawa et al. (2011) have reported that VHF-MSE on 30 June are accompanied by simultaneous MSE over Wakkanai at the MF band (MF-MSE). For the 29 June event, no echo power data from the MF radar are available, and therefore we do no know whether MF-MSE existed or not. HF-MSE on 16 June (Figs. 4(a) and 4(b)) are not accompanied by VHF-MSE, but by simultaneous MF-MSE at 84–90 km altitudes (not shown), indicating that HF-MSE are located somewhere at these altitudes. It is noted that a
SuperDARN radar in Finland and a VHF radar in Sweden, being separated by 650 km each other, simultaneously observed PMSE at 80–90 km altitudes (Ogawa et al., 2003).
Plasma turbulence and/or electron density structure appearing around the cold mesopause are responsible for the generation of echoes at the VHF (wavelength ~6 m), HF (~30 m), and MF (~150 m) bands (e.g., Rapp and Lübken, 2004). VHF-PMSE are due to backscatter from Bragg-scale electron density irregularities. Partial reflection or Fresnel reflection from sharp electron density gradients along radar beam is another candidate for the backscatter. Partial reflection seems to dominate at the HF and MF bands (e.g., Röttger, 1994). In our observations, MSE did not always appear simultaneously at the three frequency bands, the reasons of which may be as follows: (1) when the plasma turbulence and structure have spectral components of the order of the above-mentioned wavelengths, simultaneous MSE appear at the three bands, while for example, when no components of 6 m or less exist, VHF-MSE are not expected. Moreover, the turbulent spectrum and plasma structure may be variable in space and time mainly due to short-period AGW. (2) The VHF and MF radars observe a common volume over Wakkanai, while the HF radar FOV is located at least 150 km to the east of Wakkanai. If the MSE region in the horizontal plane is wide enough to cover both the VHF and HF FOVs, HF-MSE and VHF-MSE are expected to be observed simultaneously. (3) HF-MSE are observed with the oblique-incidence HF radar, suggesting that scatterers inducing the HF backscatter are rather isotropic (weakly aspect sensitive) (e.g., Ogawa et al., 2002, 2003). If the scatterers are highly anisotropic (highly aspect sensitive), MSE would be detected with the vertical-incidence VHF and MF radars, but not with the oblique-incidence HF radar. See a paper by Rapp and Lübken (2004) for discussion about aspect sensitivity (i.e., signal dependence on radar beam tilted from the vertical direction) of VHF-PMSE.
HF-MSE exhibit high Doppler velocities with a maximum of about 60 m/s toward the south, and the HF-MSE region move southward with time, both being consistent with the background meridional winds observed with the MF radar (Figs. 3(c) and 4(c)). The southward winds are also responsible for the VHF-MSE occurrence over Wakkanai (Ogawa et al., 2011). These facts suggest that irregularities and/or cold ice particles may be advected southward from higher latitudes, as already pointed out (e.g., Gerding et al., 2007; Morris et al., 2009).
Finally, we detected for the first time MSE at the HF band using a midlatitude SuperDARN HF radar in combination with VHF and MF radars. Surely, in the future we need to observe a common volume with three radars to answer some questions raised in this paper. The existing and planned SuperDARN radars at midlatitude can contribute to the better understanding of midlatitude MSE.
This work was supported by a Grant-in-Aid for Scientific Research of the Ministry of Education, Culture, Sports, Science and Technology (MEXT) of Japan (19340141), and also by Special Funds for Education and Research (Energy Transport Processes in Geospace) of MEXT.
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