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Variations of f oF2 and GPS total electron content over the Antarctic sector
Earth, Planets and Space volume 63, pages327–333(2011)
This paper presents a preliminary analysis of the variations of the critical frequency of the F2 region (foF2) and the total electron content (TEC) derived from Global Positioning System (GPS) data. Hourly foF2 values were scaled from ionograms recorded at San Martin (68.1°S, 293.0°E) and the TEC values were derived from GPS observations at O’Higgins (63.3°S, 302.5°E). The database includes measurements obtained under different seasonal and solar activity conditions. The study shows that the daily peak of foF2 occurs around local noon in winter and fall, and in spring a secondary peak is observed around midnight. In summer (January) foF2 reaches its minimum value around the noon sector while the maximum in the diurnal variation of foF2 is located in a time sector close to midnight. This behaviour is observed at low and high solar activity. The semiannual anomaly appears around noon at high and low solar activity and the winter anomaly is not observed. The effect of the solar activity is generally observed in every season. The analysis of the GPS TEC measurements in the same region indicates that the diurnal, seasonal and solar activity variations are similar to those observed in the foF2 values. An analysis of the performance of the IRI model to predict foF2 is also shown using the two IRI options (URSI and CCIR). The comparisons between the experimental values and the IRI predictions show some discrepancies.
Three latitudinal regions can be distinguished in the terrestrial ionosphere namely: the equatorial zone (within 20° of the magnetic equator), the high latitude (poleward of about 60° geomagnetic) and the middle latitude zone in between.
The knowledge of the high latitude ionosphere is more limited compared with that of the middle and low latitudes and the known features of the high latitude region have been derived mainly from observations in the Northern hemisphere. However marked differences, at the high latitudes between the hemispheres have been observed (Mallis and Essex, 1993).
Key parameters for studying the ionosphere are the critical frequency of the F2 region (foF2) and the total electron content (TEC). The foF2 is equivalent to the maximum density in the vertical distribution of the ionosphere (NmF2) and TEC is defined as the number of free electrons in a cylinder of one square metre along the radio path, a parameter that is very important for systems using transionospheric radio waves.
The combination of data obtained by different techniques (from ground-based instruments to satellite observations) assists with improving the understanding of the complex phenomena and high variability of the ionosphere at the high latitudes. The increase in availability of total electron content data (TEC) over the last ten years has largely come from a rapid increase in the number of Global Positioning System receiver stations available from which TEC data (GPS TEC) can be derived. Compared with the long record, almost 50 years of ionospheric observations available from ground based measurements, the GPS TEC database is relatively short. However the increase in the number of GPS receiver sites is now providing an important database for studying the ionosphere.
In the Argentine Antarctic sector there are two ionospheric stations: San Martin (68.1°S, 293.0°E; Geomagnetic: 53.0°S) and Belgrano (77.9°S, 321.4°E; Geomagnetic: 67.5°S). They have been operating for more than four decades and in 1994 the two ionospheric stations were equipped with KEL AEROSPACE IPS 42 ionosondes and a digitized system for the vertical incident soundings. However, as far as the authors of this paper know, there are few published studies using ionosonde data from the Argentine Antarctic region (Mosert et al., 2003).
The San Martin ionosonde station is located at an high geographic latitude but is a middle-latitude station in terms of geomagnetic coordinates. Belgrano is an auroral station from the geographic and geomagnetic point of view. Both stations offer an excellent opportunity for studying the complex behaviour of this remote region and for contributing the improvement of ionospheric models.
Several empirical models for the middle and high latitude F-region exist. One of them is the International Reference Ionosphere (IRI) model (Bilitza, 2001; Bilitza and Reinisch, 2008). It was formulated by the Committee on Space Research (COSPAR) and the International Union of Radio Science (URSI) in the sixties. The model has been validated using a large data base and it is continuously improved taking into account experimental evidence (Bilitza, 2001; Bilitza and Reinisch, 2008). Authors of this paper have validated the IRI model using ionospheric data from low and middle latitudes (Ezquer et al., 1996, 1997, 1998, 1999; Mosert et al., 2004).
The aim of this contribution is to analyze the variations of the critical frequency of the ionospheric F2 region (foF2) equivalent to the maximum electron density (NmF2) and the total electron content derived from GPS observations (GPS TEC), using the new database from the Antarctic region as a first step towards contributing to the characterisation of the ionospheric behaviour in this geographic area. The ability of the IRI model to predict foF2 over the Argentine Antarctic region is also investigated and presented in this paper.
2. Data Used
The study was made using two Antarctic stations situated close to each other: San Martin (68.1 S, 293.0 E; Geomagnetic 53.0°S) for the foF2 measurements and O’Higgins (63.3 S, 302.5 E; Geomagnetic: 48.6°S) for the GPS TEC values. The foF2 measurements were recorded with an ionosonde (KEL Aeropace) and the TEC values were obtained from Global Positioning System (GPS) data. The GPS TEC values were derived from GPS slant TEC observations using the LPIM algorithm developed by the Argentine La Plata Group (Brunini et al., 2001). As it is known GPS TEC represents a measurement of TEC up to around 20000 km (height of the GPS satellites), including the major part of the plasmaspheric electron content.
The data base includes hourly monthly median values of foF2 and GPS TEC obtained during the representative months of summer (January), winter (July), fall (April) and spring (October) during high solar activity (HSA) years: 2000 (Rz12 = 117), 2001 (Rz12 = 111) and low solar activity (LSA) years: 2007 (Rz12 = 8), 2008 (Rz12 = 3). In addition, median foF2 values obtained at San Martin and Great Wall (77.7°S, 318.5°E; Geomagnetic: 67.2°S) during the LSA years 1996 (Rz12 = 9) and 1997 (Rz12 = 23) were also used.
It is important to remember that at high latitudes all ionosondes are subject to several rather severe limitations during space weather events such as, magnetic storms and sub-storms and associated auroral and polar absorption, auroral events, spread F conditions and sporadic E layer effects which can produce a blanketing of the signal trace. For this reason it is particularly important for the ionospheric data to be manually edited prior to use. The KEL Aerospace ionosonde does not allow automatic scaling of the ionograms, and therefore, all data used in this analysis was selected to be quality and manually scaled. For this reason we have included in our analysis only data from San Martin station.
3. Analysis of the Results
3.1 Behaviour of foF2
In Fig. 1 the median values of foF2 are plotted against the local time (LT) for the 4 different seasons to illustrate the diurnal and seasonal variations for the years (a) 2000 and (b) 2001 representing the HSA period and the years (c) 2007 and (d) 2008 representing the low solar activity period. It can be observed that at the LSA and HSA periods the daily foF2 peak over the San Martin station occurs around the local noon and the minimum values around sunrise in winter and fall. In spring a secondary peak is observed around midnight (this is more evident at LSA than at HSA). Different behaviour is observed in summer for both solar activity levels: the maximum value of the F2-layer is not observed close to noon but in a time sector close to midnight. Furthermore, the minimum value of the parameter is observed mainly close to noon. This behaviour is found at LSA and HSA. The anomalous diurnal variation in foF2 was also reported by Sojka et al. (1988) and Pavlov et al. (2008) using data from the Argentine Islands ionosonde station (65.2°S, 295.7°E). It is important to point out that this anomalous diurnal variation was also observed in the Southern Hemisphere and it is known as the Weddell Sea Anomaly in NmF2 (Horvath, 2007). This behaviour indicates that diurnal variations of foF2 have a weak solar zenith dependence. These diurnal variations of foF2 are explained by Pavlov and Pavlova (2009) by changes in the neutral wind-induced drift along the magnetic field lines and by neutral density variations. A poleward neutral wind causes a lowering of the F2-region height and a reduction of the density peak NmF2 due to an increase in the loss rate of O+ ions with N2 and O2. An equatorward wind tends to increase the value of NmF2 by transporting the plasma up along field lines to regions of lower loss of O+. Close to the noon sector, the F2 layer is lowered into an altitude of higher recombination rates of O+ causing a decreasing of NmF2. Close to the midnight sector, the F2-layer is raised and maintained by plasma drift. As the ionosphere is sunlit during the long summer day in January NmF2 increases producing the observed higher NmF2 values close to midnight (Pavlov et al., 2008; Pavlov and Pavlova, 2009).
The results of Fig. 1 also illustrates that in the HSA period the winter anomaly is slightly present in the year 2000 during post noon hours (13.00 and 14.00 LT) and it is not observed in the year 2001. In 2007 (in 2008 are missing the winter foF2 values) the foF2 summer-winter differences around noon are more pronounced than in the years of HSA (2000–2001). These results indicate that the winter anomaly decays in amplitude or it is not present with decreasing solar activity (Torr and Torr, 1973).
Torr and Torr (1973) studying the winter anomaly by using noon monthly median values data of foF2 for a chain of stations over the globe under different solar activity conditions, concluded that the winter anomaly is more pronounced in the Northern Hemisphere than in the Southern Hemisphere and the magnitude of the winter anomaly decrease with decreasing solar activity.
Other feature of the seasonal variation of f o F2 is the semi-annual anomaly that it is characterized by maximum values of foF2 around noon in the equinoctial months. It can be seen in Fig. 1 that the spring and fall values of foF2 around noon are generally greater than the winter and summer foF2 values.
The analysis of Fig. 1 also illustrates that in summer, spring and fall the median values of foF2 are greater at high solar activity than at low solar activity during all the hours of the day. The values range between 2.3 and 9.8 Mhz during the HSA years and between 2.1 and 7.2 Mhz during the LSA years. In winter this behaviour is observed only between 08.00 LT and 18.00 LT. From 00.00 LT and 07.00 LT the effect of the solar activity on foF2 is not observed.
Figure 2 shows the monthly median values of foF2 for Great Wall and San Martin during the LSA years: 1996 and 1997 and for the 4 seasons. It can be seen that the diurnal and seasonal variations are similar to those observed in Fig. 1. Particularly, it is observed the absence of the winter anomaly, the presence of the equinoctial peaks around noon and the anomalous diurnal variations of foF2 in summer (the maximum value is displaced from the expected noon sector to a sector close to midnight).
3.2 Behaviour of GPS TEC
In Fig. 3 the monthly median values TEC values (in TEC units of 1016 e/m2) derived from GPS observations (GPS TEC) are plotted against the time for the 4 different seasons to illustrate the diurnal and seasonal variations for the years (a) 2000 and (b) 2001 representing the high solar activity and (c) 2007 and (d) 2008 representing the low solar activity. Note that in Fig. 3(a) and (c) are missing the spring values.
Theanalysis of the observed GPS TEC values in the close region where the foF2 values were measured indicates that the diurnal, seasonal and solar activity behaviour is similar to that observed in the foF2 values. The anomalous diurnal variations of foF2 observed in summer are also found in the corresponding GPS TEC values (the daytime observations are lower than the night-time values). The winter anomaly is not present (the GPS TEC measurements are greater in summer than in winter in the LSA and HSA years). The semi-annual anomaly around noon is generally present in all the years. The only exception is in 2007 (where the spring values are missing). The effect of the solar activity on the GPS TEC values is also observed: the values range between 2 and 17 TECU at LSA and between 4 and 55 TECU at HSA.
As it is known GPS TEC represents a measurement of TEC up to around 20000 km (height of the GPS satellites), including the ionospheric TEC (bottom and topside) and the plasmaspheric TEC. Nevertheless, previous studies (Belehaki et al., 2003, 2004; Mosert et al., 2007) that analyze the behaviour of TEC obtained by GPS observations and the ionospheric TEC obtained with the technique proposed by Huang and Reinisch (2001) show that the seasonal and solar activity variations of GPS TEC follow very well the corresponding ionospheric TEC variations.
3.3 Comparison between foF2 measurements and the IRI model
Figure 4 shows the comparison between the foF2 monthly median values for San Martin and the two options (URSI and CCIR) provided by the IRI model (Bilitza and Reinisch, 2008) to predict the density peak foF2 during a high solar activity year (2000). The seasons are represented by (a) January for summer, (b) April for fall, (c) July for winter and (d) October for spring. Figure 5 shows the same comparisons for a year of low solar activity (2007).
It can be seen that, in general, the two models estimations (CCIR and URSI) follow the diurnal trend of the experimental foF2 curves in winter (July) and fall (April): lower values are observed during night-time than during daytime in the three curves at both levels of solar activity. In generally the IRI predictions overestimate the observations during April at HSA and a good agreement is observed during LSA. In spring (October) the IRI predictions do not reproduced the post sunset peak observed in the experimental values. The model overestimation is also present in this month particularly at HSA. In summer (January) the diurnal variation observed in foF2 is notpredicted by the model at HSA: The night time maximum is not reproduced by the IRI predictions. It is important to point out that in this season during night-time the URSI values are closer to the observations than the CCIR IRI option values. Moreover it is noted that the night/day differences are more pronounced in the measurements than in the IRI predictions. This is more evident at HSA.
Using ionosonde observations at San Martin (68.1°S; 293.0°E geographic; 53°S magnetic) and GPS observations at O’Higgins (63.3°S, 302.5°E; magnetic 48.6°S), hourly monthly median values of foF2 (critical frequency of the F2 region) and GPS TEC (vertical GPS total electron content) have been derived. The diurnal, seasonal and solar activity variations of both parameters in this Antarctic region have been analyzed. The study shows that the daily peak of foF2 occurs around local noon in winter and fall, in spring a secondary peak is observed around midnight (this is more evident at LSA than at HSA). In summer (January) foF2 reaches its minimum value around the noon sector while the maximum in the diurnal variation of foF2 is located in a time sector close to midnight. This behaviour is observed at low and high solar activity. The seasonal variations of foF2 indicate that the winter anomaly is slightly present at HSA and it is not observed in the LSA years, and that the semi-annual anomaly occurs in all the cases analyzed. Our analysis also illustrates that in summer, spring and fall the median values of foF2 are greater at high solar activity than at low solar activity during all the hours of the day. The values range between 2.3 and 9.8 Mhz during the HSA years and between 2.1 and 7.2 Mhz during the LSA years. In winter this behaviour is observed only between 08.00 LT and 18.00 LT. From 00.00 LT and 07.00 LT the effect of the solar activity on foF2 is not observed.
It is important to point out that this analysis is a first attempt to analyze ionospheric parameters using data from the Argentine Antarctic region. An extension of this study is being done using data from the Belgrano station and parameters derived from electron density profiles.
Although the results here presented are preliminary we consider important to report them in order to show that the observational database in this remote region can help to describe better the morphology and modelling of the high latitude ionosphere particularly in the Southern Hemisphere.
Belehaki, A., N. Jakowski, and B. W. Reinisch, Comparison of ionospheric ionization measurements over Athens using ground ionosonde and GPS derived TEC values, Radio Sci., 38 (6), 1105, 2003, 10.1029/2003RS002868
Belehaki, A., N. Jakowski, and B. W. Reinisch, Plasmaspheric electron content derived from GPS TEC and digisonde ionograms, Adv. Space Res., 33, 833–837, 2004, 10.1016/j.asr.2003.07.008
Bilitza, D., International Reference Ionosphere 2000, Radio Sci., 36, 261–275, 2001, 10.1029/2000RS002432
Bilitza, D. and B. W. Reinisch, International Reference Ionosphere: Improvements and new parameters, Adv. Space Res., 42 (4), 599–609, 2008. 10.1016/j.asr.2007.07.048
Brunini, C., A. Meza, and A. Diaz, Regional vertical total electron content using GPS observation, Proceedings of the 2001 IAG Scientific Assembly (CD edition), Budapest, Hungary, 2001.
Ezquer, R. G., R. Del V. Oviedo, and C. Jadur, Ionospheric predictions for South American latitudes, Radio Sci., 31 (2), 381–388, 1996. 10.1029/95RS03366
Ezquer, R. G., N. Jakowski, and C. Jadur, Predicted and measured total electron content over Havana, J. Atmos. Sol.-Terr. Phys., 59 (5), 591–596, 1997. 10.1016/S1364-6826(96)00049-1
Ezquer, R. G., C. Jadur, and M. Mosert, IRI-95 TEC predictions for the South American peak of the equatorial anomaly, Adv. Space Res., 59 (5), 811–814, 1998. 10.1016/S0273-1177(98)00103-3
Ezquer, R. G., M. A. Cabrera, and J. R. Manzano, Predicted and measured electron density at 600 km altitude in the South American peak of the equatorial anomaly, Atmos. Sol. Terr. Phys., 61 (5), 415–421, 1999. 10.1016/S1364-6826(98)00146-1
Horvath, I., Impact of 10 January 1997 geomagnetic storm on the night-time Weddell Sea Anomaly: A study utilizing data provided by the TOPEX/Poseidon mission and the Defense Metereological Satellite Program, and simulations generated by the Coupled Termosphere/Ionosphere Plasmasphere model, J. Geophys. Res., 112, A06329, doi:10.1029/2006JA012153, 2007.
Huang, X. and B. W. Reinisch, Vertical electron content from ionograms in real time, Radio Sci., 22 (6), 335–342, 2001. 10.1029/1999RS002409
Mallis, M. and E. A. Essex, Diurnal and seasonal variability of the southern-hemisphere main ionospheric trough from differential-phase measurements, J. Atmos. Terr. Phys., 55, 1021, 1993. 10.1016/0021-9169(93)90095-G
Mosert, M., R. G. Ezquer, G. Miro, B. Lazo, and L. de la Zerda, A preliminary analysis of the variability of ionospheric characteristics, Proceedings of the IRI Task Force Activity 2002, IC/IR/2003/3, pag. 17, ISBN 92 95003 18-7, Triste Italy, 2003.
Mosert, M., D. Buresova, R. G. Ezquer, and G. Mansilla, Behaviour of the bottomside electron density profile over Pruhonice, Adv. Space Res., 34 (9), 1982–1989, 2004. 10.1016/j.asr.2004.03.017
Mosert, M., M. Gende, C. Brunini, R. G. Ezquer, and D. Altadill, Comparisons of IRI TEC predicitons with GPS and digisonde measurements at Ebro, Adv. Space Res., 39, 841–847, 2007. 10.1016/j.asr.2006.10.020
Pavlov, A. V. and N. M. Pavlova, Anomalous variations of NmF2 over the Argentine Islands: a statical study, Ann. Geophys., 27, 1363–1375, 2009. 10.5194/angeo-27-1363-2009
Pavlov, A. V., N. M. Pavlova, S. F. Makarenko, and V. N. Shubin, Anomalous variation in the structure of the ionospheric F2 region at geomagnetic midlatitudes of the Southern and Northern hemispheres in going from summer conditions at high solar activity, Geomag. Aeron., 48, 75–88, 2008. 10.1134/S001679320801009X
Sojka, J. J., R. W. Schunk, and G. L. Wrenn, A comparison of foF2 obtained from a time-dependent ionospheric model with Argentine Islands data for quiet conditions, J. Atmos. Terr. Phys., 50, 1027–1039, 1988. 10.1016/0021-9169(88)90092-X
Torr, D. G. and M. R. Torr, The seasonal behaviour of the F2 layer of the ionosphere, J. Atmos. Terr. Phys., 35, 2237–2251, 1973. 10.1016/0021-9169(73)90140-2
This work was made possible by a bilateral grant project “Polar Ionospheric Characterisation” funded by the Ministery of Science, Technology and Productive Innovation (MINCyT) of Argentina and the National Research Fundation (NRF) of South Africa. The authors also want to thank to Dr. A. Foppiano who provided the data from the Great Wall station.
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Mosert, M., McKinnell, L.A., Gende, M. et al. Variations of f oF2 and GPS total electron content over the Antarctic sector. Earth Planet Sp 63, 327–333 (2011). https://doi.org/10.5047/eps.2011.01.006
- high latitude
- f o F 2
- GPS TEC