A statistical analysis of Pc1–2 waves at a near-cusp station in Antarctica
© The Author(s) 2017
Received: 7 June 2017
Accepted: 25 October 2017
Published: 3 November 2017
ULF waves in the highest frequency band (0.1–5 Hz, Pc1–2 waves) have been extensively observed in the magnetosphere and on the ground at both low and high latitudes (Bolshakova et al. 1980; Anderson et al. 1992a, b; Menk et al. 1993; Mursula et al. 1994; Dyrud et al. 1997). They are generally believed to be generated by electromagnetic ion cyclotron (EMIC) resonance in the near equatorial magnetospheric regions, for example, in the storm-time ring current (Menk 2011).
The waves propagate toward the ionosphere along geomagnetic field lines as left-handed polarized Alfven waves. In the ionosphere, after a conversion into right-handed polarized isotropic compressional modes, the waves propagate horizontally in the waveguide represented by the ionosphere, becoming linearly polarized far from the injection region; the major axis of the polarization ellipse points along the direction of wave arrival in the waveguide (Tepley and Landshoff 1966; Greifinger and Greifinger 1968; Greifinger 1972a, b; Summers and Fraser 1972; Fujita and Tamao 1988). Because ionospheric boundaries are not perfect reflectors, the waves are attenuated during propagation, while leakage through the lower boundary allows their observation on the ground (Manchester 1966).
Frequency time representation of Pc1–2 waves on the ground reveals that they can be generally characterized as structured and unstructured waves.
Structured waves, called “pearls”, are characterized by periodic variations in amplitude and have been observed primarily at low and middle latitudes; they are commonly interpreted in terms of wave packets bouncing between conjugate points (Jacobs and Watanabe 1964), as waves modulated by long period ULF waves (Rasinkangas and Mursula 1998; Mursula et al. 2001), or due to a ion cyclotron resonator (Guglielmi et al. 2000), but the formation mechanism has not yet been definitely identified (Paulson et al. 2014, 2017).
Unstructured waves, which do not show a clear repetitive structure, are predominant at high latitudes, suggesting that their source is in the outer magnetospheric regions (Menk et al. 1993; Mursula et al. 1994). The occurrence of waves is characterized by a diurnal variation, with a maximum around noon, and shows an inverse relation with the solar cycle, being significantly higher during the solar minimum (Menk et al. 1993; Mursula et al. 1994; Kangas et al. 1998).
Ground and satellite observations (Popecki et al. 1993; Anderson et al. 1996) have suggested that ions of the plasma sheet, drifting from the nightside to dayside, can develop a temperature anisotropy capable of generating EMIC waves; therefore, equatorially generated EMIC waves can represent the source of high-latitude waves. Dyrud et al. (1997) examined Pc1–2 waves at cusp (74°) and polar (80°) latitudes; they found that broadband waves dominated at higher latitudes. Their occurrence was confined around local magnetic noon (within 4 h), while narrower bandwidth events are predominant at cusp latitudes and are distributed more widely in local time. The authors suggested that the narrowband waves originated in the subsolar and post-noon equatorial region, while the broadband waves originated in the high-latitude plasma mantle and at the poleward edge of the cusp.
In the outer magnetosphere (L > 9), Engebretson et al. (2002) found that most of the observed Pc1–2 waves were associated with compressions of the magnetosphere, due to enhanced solar wind (SW) densities. Analyzing spacecraft and ground data, Usanova et al. (2008) observed structured dayside Pc1 waves at L = 5–6.5 (63°–66°) related to SW density enhancements and magnetospheric compressions, which may be an important source for lower latitude EMIC waves close to the plasmapause. Similarly, Clausen et al. (2011) found that EMIC waves at geosynchronous orbit were preferentially generated during intervals of large SW density, and Tetrick et al. (2017) provided statistical evidence for the association of substorm injections and SW compressions with the onset of EMIC waves at the plasmapause. Usanova et al. (2012), analyzing THEMIS data, observed that EMIC waves occurred preferentially in the dayside outer magnetosphere and are strongly controlled by SW pressure; moreover, high EMIC occurrence, preferentially at 12–15 MLT, is also associated with high AE.
Kim et al. (2011) examined Pc1–2 events simultaneously observed along a meridional array in Antarctica (62°S to 87°S geomagnetic latitude, spanning 2920 km) during 2007; they found that the waves were observed predominantly during the daytime hours, propagated poleward in the ionospheric waveguide, changed to a linear polarization, and had an attenuation factor of ~ 10 dB/1000 km.
The importance of Pc1–2 waves as responsible for relativistic electron precipitation into the high-latitude ionosphere has been recently shown with increasing observational evidence (Rodger et al. 2008; Clilverd et al. 2010; Blum et al. 2015). Theoretical studies have demonstrated that such waves should be an effective mechanism for loss of > 1 MeV electrons from the radiation belts, through pitch angle scattering by gyro-resonant interaction (Engebretson et al. 2008, and references therein). The electron precipitation could modify, by ionization, the chemistry and electric conductivity of the atmosphere (Mironova et al. 2015), with potential effects on local or even global climate. In this regard, it is worth noting that a significant correlation between Pc1–2 power and atmospheric parameters has been recently observed in statistical analyses at Terra Nova Bay (TNB) (Francia et al. 2015; Regi et al. 2016, 2017).
In the present work, we conducted a statistical study of Pc1–2 waves in the 100–500 mHz frequency range at southern polar latitudes. We used ULF geomagnetic field measurements collected at the Italian station Mario Zucchelli (Terra Nova Bay, Antarctica, TNB, AACGM latitude 80°S, MLT = UT − 8) from 2003 to 2010, corresponding to the declining phase of solar cycle 23 and the onset of solar cycle 24. Although TNB is located in the polar cap, its latitude is such that at magnetic local noon the field line approaches the cusp and closed field lines. The availability of a long time series data allowed us to analyze the solar cycle and seasonal and local time dependence of the observed Pc1–2 waves and investigate their relationship with geomagnetic conditions and SW density.
Data and methods
We used geomagnetic field fluctuation measurements collected from a search coil magnetometer installed at TNB from 2003 to 2010, with a large data gap during 2005. The instrument provides northward H, eastward D, and vertically downward Z components of geomagnetic field variations at a 1-s sampling rate. To reduce aliasing, a low-pass filter was applied so that the response at frequencies > 450 mHz was strongly dampened.
We computed, over 30-min intervals, the power spectral density (PSD) and cross-power spectral density (CPSD), using the Hamming window and averaging 200-s subintervals with no overlap, corresponding to a frequency resolution of 5 mHz and 18 degrees of freedom. The spectra were then converted using an instrument transfer function from mV2/Hz to nT2/Hz.
We estimated the polarization parameters applying the technique for partially polarized waves as proposed by Fowler et al. (1967). In particular, the polarization ratio R, the ratio between the polarized and total intensities of the horizontal signal, ellipticity ε, the ratio between the minor and major axes of the polarization ellipse in the horizontal plane, and azimuth θ, the clockwise measured angle between the major axis of the polarization ellipse and the H direction, were evaluated over each interval. Looking downward in the southern hemisphere, a positive (negative) value of ellipticity indicates left-handed (right-handed) polarized waves; if the ellipticity is close to zero, generally |ε| < 0.2, the waves are linearly polarized.
To characterize the interplanetary and magnetospheric conditions, we used the 1-min SW and interplanetary magnetic field (IMF) data and 1-min geomagnetic activity index AE, respectively, from the OMNI database (http://cdaweb.gsfc.nasa.gov/cdaweb/istppublic/).
The statistical analysis
For each 30-min interval, we computed the power on the horizontal H and D components, P H and P D , integrated in the Pc1–2 (100–450 mHz) frequency range. Because the power and AE index typically show variations in several orders of magnitude, when computing time averages, we used log(P) (Francia et al. 2015; Regi et al. 2015, 2016) and log(AE) (Anqin et al. 2008; Schmitter 2010) that follow a quasi-normal distribution. The power was then obtained reconverting the results using the exponential function.
Figure 14 shows the event observed on August 27, 2003, just after local magnetic midnight (08 UT = 00 MLT). Corresponding to the broadband power enhancements observed in the time interval 09:00–10:00 UT, polarized, short-lived waves in the 300–400 mHz frequency band are observable. They are characterized by an ellipticity of ~ 0° (linear polarization) and a θ value of ~ 40°–50°. These waves are associated with moderate geomagnetic activity, evidenced by IMF southward fluctuations and an AE index higher than 300 nT.
Summary and discussion
We conducted a statistical study of the Pc1–2 waves at TNB, a southern polar cap station. The geomagnetic latitude (~ 80°S) is such that, during the day, the local open field lines approach the magnetopause and closed field lines around noon; it is very close to the latitude of the poleward cusp boundary, particularly during summer and equinoctial months and for northward IMF conditions, i.e., for a quiet magnetosphere (Zhou et al. 1999, 2000).
The long data series, almost continuous in the time interval 2003–2010, allowed us to the study solar cycle and seasonal and daily variations in Pc1–2 power.
We found that the Pc1–2 power seems to follow the solar activity variation, slightly decreasing through the descending phase of the solar cycle (2004–2008) to the solar minimum in 2009. In addition to this weak variation, the Pc1–2 power shows a seasonal modulation, characterized by higher values during the local summer, and a MLT dependence, characterized by a maximum around noon. Both features can be explained, considering that the TNB field lines are at the shortest distances from the outermost closed field lines during summer and around magnetic local noon. Indeed, the latitudinal position of the cusp footprint depends on the dipole tilt angle, which exhibits both an annual variation and daily variation. When the geomagnetic dipole axis tilts more toward the Sun, the cusp moves more poleward; Zhou et al. (1999) examined polar cusp crossings at high altitude, obtained from polar satellite data, and showed that the magnetic latitude of the center cusp moves from ~ 77° to ~ 81°, when the tilt angle changes from − 30° to 30°.
An analysis of Pc1–2 events indicates a seasonal variation, consistent with a similar variation in power. In contrast, examining the MLT dependence, in addition to a main peak of occurrence around noon, also observed in the power analysis, there is a minor peak near midnight. While polarized waves represent only a small fraction of the events observed around noon, midnight events are generally polarized waves. Both noon and midnight polarized waves exhibit a similar frequency distribution. The ellipticity values indicate primarily linearly polarized waves, with the major axis directed at ~ 50° with respect to the H component. Our results suggest that the power peak at noon is due primarily to unpolarized waves, with a minor contribution represented by linearly polarized waves. This observation is interpreted as waves propagated far from the injection region up to the TNB latitude, in the high-latitude ionospheric waveguide along the meridional direction (Kim et al. 2011). The midnight events are very few with respect to the noon events, but are generally consistent with linearly polarized waves.
Considering geomagnetic and SW conditions, we found that the noon peak is associated with time intervals characterized by very high SW densities and associated high AE values (Usanova et al. 2012), while the midnight peak is entirely associated with high AE values. In addition, the Pc1–2 power appears significantly related to AE through the day, particularly at midnight, and to n SW only around noon. Based on these results, we hypothesize that this observation indicates different sources for Pc1–2 waves observed at TNB. In the noon sector, compressions of the outermost closed magnetospheric field lines by the SW are important; in the declining phase of the solar cycle SW pressure variations are generally associated with the fast stream occurrence, which also produces high magnetospheric activity (high AE). We note that the noon maximum of both power and event occurrence is slightly asymmetric, shifted to the post-noon sector, in agreement with the results of previous studies. At geosynchronous orbit, a similar MLT occurrence of EMIC waves associated with SW pressure peaks was documented in Clausen et al. (2011) and Park et al. (2016); on the ground, a post-noon occurrence maximum (12–13 MLT) was observed by Kurazhkovskaya et al. (2007) at the Mirny Observatory (77°S invariant latitude, Antarctica) for magnetic impulses accompanied by Pc1 pulsations. This feature could be due to the impact of SW high density regions leading fast streams (Corotating Interaction Regions), mostly on the post-noon magnetopause, due to the IMF average orientation at the Earth’s orbit at ~ 45° with respect to the Sun–Earth direction (Rostoker and Sullivan 1987; Villante et al. 2001). In the midnight sector, Pc1–2 waves are likely caused by substorm/stormrelated ion instability occurring in the plasma sheet. The significant correlation observed between Pc1–2 power and both AE index and SW density allows us to develop a simple model to estimate Pc1–2 power from the two parameters. The model fits the experimental data well, and for time intervals outside the dataset used for the model, up to time scales as short as 6–7 h. Taking into account that the wave power attenuation along the ionospheric waveguide is ~ 10 dB/1000 km (Kim et al. 2011), we believe that the applicability of the model can be extended from auroral latitudes up to latitudes near the geomagnetic pole.
The occurrence of events shows a dependence on the solar cycle, opposite with respect to the power dependence, with an increasing number of events through the years. This feature is consistent with previous results, which showed a strong negative correlation between high-latitude Pc1 events and solar activity, and agrees with the negative correlation between SW density and solar activity (Mursula et al. 1994; Kangas et al. 1998).
We suggest that Pc1–2 events observed around noon at TNB could be due to waves generated just inside the magnetopause, near the equatorial plane, by SW compressions, which was observed in the dayside outer magnetosphere by Engebretson et al. (2002) and Usanova et al. (2012). These waves propagate along the outermost closed field lines into the ionosphere; then, they can propagate along the ionospheric waveguide far from the injection region up to the TNB latitude. For example, at noon, this is over ~ 500–600 km, the average distance of the station from the closed field lines. We hypothesize that due to the closeness of the station to the cusp around noon, TNB is subject to a mixture of different waves and only very strong signals can maintain their properties, such as the polarization degree. For example, the polarized waves of the selected noon event are associated with a long duration magnetospheric compression due to very high SW density and show an ellipticity close to zero, which indicates a linear polarization, as expected for waves propagating far in the waveguide (Greifinger and Greifinger 1968; Greifinger 1972a, b).
Nighttime events are less common, probably because in the dark sector, TNB is embedded in the polar cap, with local field lines far from the magnetospheric regions from which waves originate (as the plasma sheet). The observed waves are generally polarized, likely because additional superimposed signals are absent, as suggested by the lower power content in the nighttime spectra (Fig. 4). Pc1–2 waves are observed at TNB during perturbed geomagnetic conditions, when ion instability increases in the plasma sheet. This result is in agreement with the magnetospheric observations by Usanova et al. 2012, who also detected EMIC waves just before midnight at L = 9–10 during moderate and enhanced substorm activity. The selected nighttime event has a short duration, occurred in correspondence with a geomagnetic substorm, and shows a linear ellipticity. These features are consistent with a wave packet propagated toward the high-latitude ionosphere along magnetotail field lines, from the plasma sheet, and then along the ionospheric waveguide up to TNB.
Pc1–2 waves are observed around local magnetic noon and midnight, and are, respectively, associated with SW compressions of the magnetopause and substorm/stormrelated instabilities.
Polarized waves, primarily observed around midnight, show an almost linear polarization, suggesting wave propagation along a meridional ionospheric waveguide, from the injection region up to the latitude of Terra Nova Bay.
Based on these results, we propose a simple model to estimate Pc1–2 power variations at auroral and polar latitudes that depend on the geomagnetic activity and SW density.
MR and MM performed the data analysis. MR and PF drafted the manuscript. PF and MDL participated in the study design and interpretation of results. All authors read and approved the final manuscript.
This research activity was supported by the Italian PNRA (Programma Nazionale di Ricerche in Antartide, PdR2013/B2.09). The authors acknowledge J.H. King and N. Papatashvilli at NASA and CDAWeb for solar wind data (http://cdaweb.gsfc.nasa.gov). Measurements of the magnetic field fluctuations at Terra Nova Bay can be requested from Marcello De Lauretis at the following e-mail address: firstname.lastname@example.org. The authors thank both reviewers for their helpful comments and suggestions.
The authors declare that they have no competing interests.
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- Anderson BJ, Erlandson RE, Zanetti LJ (1992a) A statistical study of Pc 1–2 magnetic pulsations in the equatorial magnetosphere: 1. Equatorial occurrence distributions. J Geophys Res 97(A3):3075–3088. https://doi.org/10.1029/91JA02706 View ArticleGoogle Scholar
- Anderson BJ, Erlandson RE, Zanetti LJ (1992b) A statistical study of Pc 1–2 magnetic pulsations in the equatorial magnetosphere: 2. Wave properties. J Geophys Res 97(A3):3089–3101. https://doi.org/10.1029/91JA02697 View ArticleGoogle Scholar
- Anderson BJ, Denton RE, Ho G, Hamilton DC, Fuselier SA, Strangeway RJ (1996) Observational test of local proton cyclotron instability in the Earth’s magnetosphere. J. Geophys. Res. 101:21527–21544. https://doi.org/10.1029/96JA01251 View ArticleGoogle Scholar
- Anqin C, Jiawei L, Guanglin Y, Jingsong W (2008) Calculating auroral oval pattern by AE Index. Acta Meteorol Sin 22(1):91–96Google Scholar
- Blum LW, Halford A, Millan R, Bonnell JW, Goldstein J, Usanova M, Engebretson M, Ohnsted M, Reeves G, Singer H et al (2015) Observations of coincident EMIC wave activity and duskside energetic electron precipitation on 18–19 January 2013. Geophys Res Lett 42:5727–5735. https://doi.org/10.1002/2015GL065245 View ArticleGoogle Scholar
- Bolshakova O, Troitskaya V, Ivanov K (1980) High-latitude Pc1–2 geomagnetic pulsations and their connection with location of the dayside polar cusp. Planet Space Sci 28:1–7. https://doi.org/10.1016/0032-0633(80)90098-7 View ArticleGoogle Scholar
- Clausen LBN, Baker JBH, Ruohoniemi JM, Singer HJ (2011) ULF wave characteristics at geosynchronous orbit during the recovery phase of geomagnetic storms associated with strong electron acceleration. J Geophys Res 116:A09203. https://doi.org/10.1029/2011JA016666 Google Scholar
- Clilverd MA, Rodger CJ, Moffat-Griffin T, Spanswick E, Breen P, Menk FW, Grew RS, Hayashi K, Mann IR (2010) Energetic outer radiation belt electron precipitation during recurrent solar activity. J Geophys Res 115:A08323. https://doi.org/10.1029/2009JA015204 Google Scholar
- Clopper CJ, Pearson ES (1934) The use of confidence or fiducial limits illustrated in the case of the binomial. Biometrika 26:404–413View ArticleGoogle Scholar
- De Lauretis M, Francia P, Vellante M, Piancatelli A, Villante U, Di Memmo D (2005) ULF geomagnetic pulsations in the southern polar cap: Simultaneous measurements near the cusp and the geomagnetic pole. J Geophys Res 110:A11204. https://doi.org/10.1029/2005JA011058 View ArticleGoogle Scholar
- De Lauretis M, Francia P, Regi M, Villante U, Piancatelli A (2010) Pc3 pulsations in the polar cap and at low latitude. J Geophys Res 115:A11223. https://doi.org/10.1029/2010JA015967 View ArticleGoogle Scholar
- Dyrud L, Engebretson M, Posch J, Hughes W, Fukunishi H, Arnoldy R, Newell P, Horne R (1997) Ground observations and possible source regions of two types of Pc 1–2 micropulsations at very high latitudes. J Geophys Res 102:27011–27027. https://doi.org/10.1029/97ja02191 View ArticleGoogle Scholar
- Engebretson M, Peterson W, Posch J, Klatt M, Anderson B, Russell C, Singer H, Arnoldy R, Fukunishi H (2002) Observations of two types of Pc 1–2 pulsations in the outer dayside magnetosphere. J Geophys Res. https://doi.org/10.1029/2001ja000198 Google Scholar
- Engebretson MJ, Lessard MR, Bortnik J, Green JC, Horne RB, Detrick DL, Weatherwax AT et al (2008) Pc1–Pc2 waves and energetic particle precipitation during and after magnetic storms: superposed epoch analysis and case studies. J Geophys Res. https://doi.org/10.1029/2007ja012362 Google Scholar
- Fowler RA, Kotick BJ, Elliott RD (1967) Polarization analysis of natural and artificially induced geomagnetic micropulsations. J Geophys Res 72(11):2871–2883. https://doi.org/10.1029/JZ072i011p02871 View ArticleGoogle Scholar
- Francia P, Regi M, De Lauretis M (2015) Signatures of the ULF geomagnetic activity in the surface air temperature in Antarctica. J Geophys Res 120(4):2452–2459. https://doi.org/10.1002/2015JA021011 View ArticleGoogle Scholar
- Fujita S, Tamao T (1988) Duct propagation of hydromagnetic waves in the upper ionosphere, 1, Electromagnetic field disturbances in high latitudes associated with localized incidence of a shear Alfvén wave. J Geophys Res 93(A12): 14665–14673. doi:10.1029/JA093iA12p14665 View ArticleGoogle Scholar
- Greifinger P (1972a) Ionospheric propagation of oblique hydromagnetic plane waves at micropulsation frequencies. J Geophys Res 77(13):2377–2391. https://doi.org/10.1029/JA077i013p02377 View ArticleGoogle Scholar
- Greifinger P (1972b) micropulsations from a finite source. J Geophys Res 77(13):2392–2396. https://doi.org/10.1029/JA077i013p02392 View ArticleGoogle Scholar
- Greifinger C, Greifinger PS (1968) Theory of hydromagnetic propagation in the ionospheric waveguide. J Geophys Res 73(23):7473–7490. https://doi.org/10.1029/JA073i023p07473 View ArticleGoogle Scholar
- Guglielmi AV, Potapov AS, Russel CT (2000) The ion-cyclotron resonator in the magnetosphere. J Exp Theor Phys Lett 72(6):432–435View ArticleGoogle Scholar
- Jacobs J, Watanabe T (1964) Micropulsation whistlers. J Atmos Terr Phys 26(8):825–826View ArticleGoogle Scholar
- Kangas J, Guglielmi A, Pokhotelov O (1998) Morphology and physics of short-period magnetic pulsations. Space Sci Rev 83:435–512View ArticleGoogle Scholar
- Kim H, Lessard M, Engebretson M, Young M (2011) Statistical study of Pc1–2 wave propagation characteristics in the high-latitude ionospheric waveguide. J Geophys Res. https://doi.org/10.1029/2010ja016355 Google Scholar
- Kurazhkovskaya NA, Klain BI, Dovbnya BV (2007) Patterns of simultaneous observations of high-latitude magnetic impulses (MIEs) and impulsive bursts in the Pc1–2 band. J Atmos Solar Terr Phys 69:1680–1689View ArticleGoogle Scholar
- Manchester RN (1966) Propagation of Pc 1 micropulsations from high to low latitudes. J Geophys Res 71(15):3749–3754. https://doi.org/10.1029/JZ071i015p03749 View ArticleGoogle Scholar
- Menk FW (2011) Magnetospheric ULF waves: a review. In: The dynamic magnetosphere, pp 223–256. Springer. https://doi.org/10.1007/978-94-007-0501-2_13
- Menk FW, Fraser BJ, Hansen HJ, Newell PT, Meng C-I, Morris RJ (1993) Multistation observations of Pc 1–2 ULF pulsations in the vicinity of the polar cusp. J Geomagn Geoelectr 45:1159–1173. https://doi.org/10.1029/95ja00768 View ArticleGoogle Scholar
- Mironova I, Aplin K, Arnold F, Bazilevskaya G, Harrison R, Krivolutsky A, Nicoll K, Rozanov E, Turunen E, Usoskin I (2015) Energetic particle influence on the Earth’s atmosphere. Space Sci Rev 194(1–4):1–96. https://doi.org/10.1007/s11214-015-0185-4 View ArticleGoogle Scholar
- Mursula K, Blomberg L, Lindqvist P, Marklund G, Bräysy T, Rasinkangas R, Tanskanen P (1994) Dispersive Pc1 bursts observed by Freja. Geophys Res Lett 21(17):1851–1854. https://doi.org/10.1029/94gl01584 View ArticleGoogle Scholar
- Mursula K, Bräysy T, Niskala K, Russell CT (2001) Pc1 pearls revisited: structured electromagnetic ion cyclotron waves on polar satellite and on ground. J Geophys Res Space Phys 106(A12):29543–29553View ArticleGoogle Scholar
- Park J-S, Kim K-H, Shiokawa K, Lee D-H, Lee E, Kwon H-J, Jin H, Jee G (2016) EMIC waves observed at geosynchronous orbit under quiet geomagnetic conditions (Kp ≤ 1). J Geophys Res Space Phys 121:1377–1390. https://doi.org/10.1002/2015JA021968 View ArticleGoogle Scholar
- Paulson KW, Smith CW, Lessard MR, Engebretson MJ, Torbert RB, Kletzing CA (2014) In situ observations of Pc1 pearl pulsations by the Van Allen Probes. Geophys Res Lett 41:1823–1829. https://doi.org/10.1002/2013GL059187 View ArticleGoogle Scholar
- Paulson KW, Smith CW, Lessard MR, Torbert RB, Kletzing CA, Wygant JR (2017) In situ statistical observations of Pc1 pearl pulsations and unstructured EMIC waves by the Van Allen Probes. J Geophys Res Space Phys 122:105–119. https://doi.org/10.1002/2016JA023160 View ArticleGoogle Scholar
- Ponomarenko PV, Fraser BJ, Menk FW, Ables ST, Morris RJ (2002) Cusp-latitude Pc3 spectra: band-limited and power-law components. Ann Geophys 20:1539–1551. https://doi.org/10.5194/angeo-20-1539-2002 View ArticleGoogle Scholar
- Popecki M, Arnoldy R, Engebretson MJ, Cahill LJ Jr. (1993) High-latitude ground observations of Pc 1/2 micropulsations. J Geophys Res 98(A12):21481–21491. https://doi.org/10.1029/93JA02539 View ArticleGoogle Scholar
- Rasinkangas R, Mursula K (1998) Modulation of magnetospheric emic waves by Pc 3 pulsations of upstream origin. Geophys Res Lett 25(6):869–872View ArticleGoogle Scholar
- Regi M, De Lauretis M, Francia P (2014) The occurrence of upstream waves in relation with the solar wind parameters: a statistical approach to estimate the size of the foreshock region. Planet Space Sci 90:100–105. https://doi.org/10.1016/j.pss.2013.10.012 View ArticleGoogle Scholar
- Regi M, De Lauretis M, Francia P (2015) Pc5 geomagnetic fluctuations in response to solar wind excitation and their relationship with relativistic electron fluxes in the outer radiation belt. Earth Planets Space. https://doi.org/10.1186/s40623-015-0180-8 Google Scholar
- Regi M, De Lauretis M, Redaelli G, Francia P (2016) ULF geomagnetic and polar cap potential signatures in the temperature and zonal wind reanalysis data in Antarctica. J Geophys Res 121(1):286–295. https://doi.org/10.1002/2015JA022104 View ArticleGoogle Scholar
- Regi M, Redaelli G, Francia P, De Lauretis M (2017) ULF geomagnetic activity effects on tropospheric temperature, specific humidity, and cloud cover in Antarctica, during 2003–2010. J Geophys Res Atmos 122:6488–6501. doi:10.1002/2017JD027107 View ArticleGoogle Scholar
- Rodger CJ, Raita T, Clilverd MA, Seppala A, Dietrich S, Thomson NR, Ulich T (2008) Observations of relativistic electron precipitation from the radiation belts driven by EMIC waves. Geophys Res Lett 35:L16106. https://doi.org/10.1029/2008GL034804 View ArticleGoogle Scholar
- Rostoker G, Sullivan BT (1987) Polarization characteristics of Pc5 magnetic pulsations in the dusk hemisphere. Planet Space Sci 35:429View ArticleGoogle Scholar
- Schmitter ED (2010) Remote auroral activity detection and modeling using low frequency transmitter signal reception at a midlatitude site. Ann Geophys 28(9):1807–1811. https://doi.org/10.5194/angeo-28-1807-2010 View ArticleGoogle Scholar
- Summers WR, Fraser BJ (1972) Polarization properties of Pc 1 micropulsations at low latitudes. Planet Space Sci 20(8):1323–1335. https://doi.org/10.1016/0032-0633(72)90019-0 View ArticleGoogle Scholar
- Tepley L, Landshoff RK (1966) Waveguide theory for ionospheric propagation of hydromagnetic emissions. J Geophys Res 71(5):1499–1504. https://doi.org/10.1029/JZ071i005p01499 View ArticleGoogle Scholar
- Tetrick SS, Engebretson MJ, Posch JL, Olson CN, Kletzing CA, Smith CW, Thaller SA, Wygant JR, Reeves GD, MacDonald EA, Fennell JF (2017) Location of intense electromagnetic ion cyclotron (EMIC) wave events relative to the plasmapause: Van Allen Probes observations. J Geophys Res Space Phys. https://doi.org/10.1002/2016JA023392 Google Scholar
- Usanova ME, Mann IR, Rae IJ, Kale ZC, Angelopoulos V, Angelopoulos JW, Glassmeier K-H, Auster HU, Singer HJ (2008) Multipoint observations of magnetospheric compression-related EMIC Pc1 waves by THEMIS and CARISMA. Geophys Res Lett 35:L17S25. https://doi.org/10.1029/2008GL034458 View ArticleGoogle Scholar
- Usanova ME, Mann IR, Bortnik J, Shao L, Angelopoulos V (2012) THEMIS observations of electromagnetic ion cyclotron wave occurrence: dependence on AE, SYMH, and solar wind dynamic pressure. J Geophys Res 117:A10218. https://doi.org/10.1029/2012JA018049 View ArticleGoogle Scholar
- Villante U, Francia P, Lepidi S (2001) Pc5 geomagnetic field fluctuations at discrete frequencies at a low latitude station. Ann Geophys 19:321–325View ArticleGoogle Scholar
- Zhou X-W, Russell C, Le G, Fuselier S, Scudder J (1999) The polar cusp location and its dependence on dipole tilt. Geophys Res Lett 26:429–432. https://doi.org/10.1029/1998gl900312 View ArticleGoogle Scholar
- Zhou X-W, Russell C, Le G, Fuselier S, Scudder J (2000) Solar wind control of the polar cusp at high altitude. J Geophys Res 105:245–251View ArticleGoogle Scholar