A new method for measuring the geomagnetic field in the ionosphere by the integrated use of vertical sounding radar (ionosonde) and incoherent scatter radar, its capabilities and features of the technical implementation, as well as the first results of an experimental test are considered.Розглянуто новий спосіб вимірювання геомагнітного поля в іоносфері шляхом інтегрального використання радару вертикального зондування (іонозонду) і радару некогерентного розсіяння, його можливості й особливості технічної реалізації, а також перші результати експериментального випробування

Belozerov, D. P.

Emelyanov, L. Ya.

Fesun, A. V.

Skvortsov, T. A.

Electronic National Technical University &quot;Kharkiv Polytechnic Institute&quot; Institutional Repository (eNTUKhPIIR)

 ISSN 2078-9998. Вісник НТУ “ХПІ”. 2014. № 47 (1089)   UDC 550.380:550.388.1:550.389.5: 537.67  T.A. SKVORTSOV, D.Sc., Prof., NTU “KhPI”; L.Ya. EMELYANOV, PhD, head of department, Institute of Ionosphere, Kharkiv; A.V. FESUN, PhD student, NTU “KhPI”; D.P. BELOZEROV, PhD, junior research scientist, Institute of Ionosphere, Kharkiv  MEASUREMENT OF THE GEOMAGNETIC FIELD IN THE IONOSPHERE USING RADAR METHODS  A new method for measuring the geomagnetic field in the ionosphere by the integrated use of vertical sounding radar (ionosonde) and incoherent scatter radar, its capabilities and features of the technical implementation, as well as the first results of an experimental test are considered. Key words: geomagnetic field, ionosphere, incoherent scatter radar, ionosonde.  Introduction. Currently, measurements of the geomagnetic field (GMF) in the ionosphere are realized at altitudes of flight of the Earth artificial satellites [1]. Currently, measurements of the geomagnetic field (GMF) in the ionosphere are realized at altitudes of flight of the Earth artificial satellites [1]. At first, the magnetic studies, which proved the presence of ionosphere sources, originative the changes of the GMF, have been carried out by the third Soviet satellite in 1958 [2]. However, measurements of the GMF in the ionosphere by satellites have the following weaknesses: 1. Area of the ionosphere near the ionospheric peak and below is practically beyond the observation zone due to short life of satellites in the specified area. At the same time, one can expect the greatest GMF variations associated with ionospheric currents just in this area. 2. Continuous monitoring of GMF in a fixed region of space is impossible due to the movement of satellites, making it difficult to study the temporal variations in GMF. 3. Simultaneous and continuous measurement of the characteristics of the ionosphere and magnetosphere in the area above IS radar is practically impossible. This reduces the possibility of studying magnetosphere-ionosphere coupling. Thus, the topical problem is to develop methods for measuring the GMF in the region near the ionospheric peak and below. To investigate the interaction of the magnetosphere and ionosphere, it is desirable to carry out combined in time and space measurement of the magnetosphere and ionosphere parameters. Such measurements can be performed using the method developed at Institute of Ionosphere [3] and described below.   © T.A. Skvortsov, L.Ya. Emelyanov, A.V. Fesun, D.P. Belozerov, 2014 57 ISSN 2078-9998. Вісник НТУ “ХПІ”. 2014. № 47 (1089)  The method allows measuring the vertical component of intensity of the GMF in region near the ionospheric peak under ionospheric observatory by the integrated use of vertical sounding radar (ionosonde) and incoherent scatter (IS) radar. Purpose is to consider the possibility of measuring the geomagnetic field at the dense ionosphere altitudes. Method for measuring GMF in the ionosphere. The Faraday effect is used to measure GMF by IS radar. The effect appears that, when the radio wave passes through the magnetized ionospheric plasma from the radar up to a height h and backwards, its polarization ellipse is rotated by an angle       hdllNlHkh0,       (1) where k =0,0594.f0–2, f0 is operating frequency, N(h) is the electron density, and H is the longitudinal component of the GMF intensity. In accordance with (1) and the mean value theorem there is in a specified height interval [h1, h2] such height xh , for which           2112hhxxdhhNhkHhhh .   (2) Thus, we have from (2):     IkNhhHMxx,      (3)  where                       21hhdhhFI       (4)    MNhNhF    is normalized to the maximum height profile of the electron density. As seen from (3), if we measure the Faraday effect, the normalized profile and maximum of the electron density, we can calculate the intensity of the GMF at a certain height within a specified interval of heights. For measuring the Faraday effect, transmitter radiates a signal with linear polarization and we carry out reception of the left and right circular polarization components. At the same time, optimal algorithm of estimate formation is of the form [4]         hrhrhrhrarctghssccscsc2121122121ˆ ,                                       (5) 58 ISSN 2078-9998. Вісник НТУ “ХПІ”. 2014. № 47 (1089)   where rc1s2, rc2s1, rc1c2, rs1s2 are estimates of the cross correlations of the signal quadrature components at the receiver outputs. To determine the  hF  function using the IS radar, the signal power  hP , electron  hTe  and ion  hTi  temperatures are measured, and then we calculate and normalize a function        hThThhСPhNie12 ,          (6) where C is any constant. MN  is measured using ionosonde. As it is necessary to radiate a long pulse with circular polarization for  hTe  and  hTi measurement, we proposed to use the sound signal, consisting of the first pulse with circular polarization and the second pulse with linear polarization [1]. The first pulse has long duration to ensure the accuracy of temperature measurement, and the second pulse has short duration to ensure high correlation between ordinary and extraordinary waves, as well as high resolution of IS signal for power measurement. Thus, we obtain the estimate    INkhhHMxx ˆˆˆˆ  ,      (7) where HNMMH IINNHH    ˆ,ˆ,ˆ,ˆ ,  , εI, εH, εN are errors of measurement. Estimation of the method accuracy. Assuming smallness of  , εI, εH, εN measurement errors and under condition of absence of their cross-correlation, we obtain on basis of (7) a formula for the relative variance of measurement error of the longitudinal component of the GMF intensity at the height xh  22222222INHINH   ,          (8) where 222 ,, IN  are variances of , Nm, and I measurement. The error due to uncertainty of the height hx can be significant in case of strong GMF change within the altitude range 12 hh  and high requirements to accuracy of binding measured GMF intensity to the height. If we represent a law of change in the GMF intensity within this altitude range as Taylor series and confine oneself to linear approximation    00 21hhHhH   ,      (9) 59 ISSN 2078-9998. Вісник НТУ “ХПІ”. 2014. № 47 (1089)  where H0 – GMF intensity at the height 2210hhh , we obtain 2222222222HINHIMNH  ,     (10) where II21 ,   dhhhhFI hh 2101 .  The height profile of the electron density can be approximated by the function           2000 hhbhhahFhF  .  (11) Then    2022222222212   hFhaHINHIMNH . (12)  We assume that the variance  r  12 22  makes the main contribution to the variance (12). Here 2  is the variance of the error of the parameter Φ, and r is the cross-correlation of errors for the heights h1 and h2, which depends on the amplitude-frequency response of the receiver. We can show that the Cramér–Rao bound for the variance 2 under optimal measurement algorithm (5) is defined by formula   122222112222121141111qqMqqqq,  (13) where  is the coefficient of correlation between the ordinary and extraordinary waves, M is the number of processed sounding cycles, q1 and q2 are the signal-to-noise ratio at the receiver outputs. The values 2   for the case of М=5800 (accumulation during a 15-min session) are presented in Table 1.   Table 1 – Standard deviation of error in measurement of the angle of the polarization ellipse rotation  q1 = q2 = 2 q1 = q2 = 4 q1 = q2 = 10 q1 = q2 = 50  = 0.5 0.022 0.017 0.014 0.012  = 0.7 0.0165 0.012 0.009 0.007  = 0.9 0.0126 0.008 0.005 0.004 60 ISSN 2078-9998. Вісник НТУ “ХПІ”. 2014. № 47 (1089)   Such potential accuracy allows expecting the fact that measurement errors in intensity of GMF can be comparable with its disturbances during geomagnetic storms. Results of experimental test of the method. Some results of the first test of the described method for measuring GMF are presented below. In this case, the one channel of the transmitter and one of two orthogonal antenna dipoles were used to emit linearly polarized waves. When sampling a signal, we used a step in height =4550 m. Because of the small step, the integral (4) for the i-interval of heights was calculated by the formula        iixi hFhFhI 215,0  .                 (14) Parameter Φ was determined according to the algorithm (5). The signal power was determined for the echo signal from the short pulse by equalizing the receiver gains, subtraction of the noise power from the signal plus noise power, accounting gain of antenna switches with gas-filled dischargers for each segment of the radar sweep, and summing the results. Dependence of vertical component of intensity of GMF on a height, got at watching 15 minutes presented on Fig. 1.   Fig. 1 – Intensity of Hz-component of geomagnetic field.  Local time in Kharkiv 13:20–13:36 (12.11.2012).   Curve 1 corresponds to the DGRF/IGRF Geomagnetic Field Model of [5], and curves 2 and 3 got experimentally. Curve 2 got with the use of temperatures in accordance with the model of IRI-2007 [6], and curve 3 – with the use of the temperatures measured by IS radar. A stroke vertical marks the height of a maximum of ionizing. 61 ISSN 2078-9998. Вісник НТУ “ХПІ”. 2014. № 47 (1089)  Apparently, in area of high concentration (230-300 kilometers) the measured values are near to the model.  It is of interest that the size of the measured intensity on the average a bit increases with a height, unlike the DGRF/IGRF model. In principle, such effect can be caused by the error of measuring of temperatures. A calculation was therefore produced with the use of model of temperatures of IRI-2007, that  confirmed the effect of increase of vertical component of intensity with a height. This fact requires additional research. However it is known that GMF in an ionosphere can have noticeable local differences from the accepted models [1, 2].  Conclusion. Theoretical estimation and experimental test indicate that it is possible to measure the vertical component of the GMF intensity in the ionosphere by the proposed method with a relative root mean square error of a few percent. We can further improve the accuracy of these measurements, in particular due to the following: – correction of errors due to errors in setting the polarization of the antenna; – improving the signal-to-noise ratio by using two channels of the transmitter for formation of the sound signal with linear polarization; – use of the polarization modulation of the sound signal, which allows to measure the electron and ion temperatures simultaneously with the signal polarization (Faraday rotation measurement). Finally, we can evaluate quality of the GMF measurement using IS radar and ionosonde after optimization of equipment and measurement algorithms, and also the analysis of experimental data with the use of a sufficiently large statistical material.  References: 1.  Ionosphere geomagnetic field: Comparison of IGRF model prediction and satellite measurements 1991 – 2010 [Электронный ресурс] // Radio Sci. – 2011. – № 46. – P. 1-10. – URL:  http://onlinelibrary.wiley.com/doi/10.1029/2010RS004529/pdf (дата обращения: 25.05.2014). 2. Aleksandrov S.G. Soviet satellites and spaceships / S.G. Aleksandrov, R.E. Fedorov. – Moscow: Academic Science, 1961. – 440 p. (in Russian). 3. Patent 71162. Ukraine, G01S 13/95. A method of measuring the parameters of the ionosphere and magnetosphere / L. Ya. Emelyanov, T. A. Skvortsov, I. B. Sklyarov, A. V. Fesun.; patented 14.11.2011; published 10.07.2012, Bulletin № 13 (in Ukrainian). 4. Tkachev G.N. The measurement of phase differential between ordinary and extraordinary waves which was scattered by thermal fluctuation electron density of ionosphere / G.N. Tkachev, V.D. Karlov // Harbinger KPU. – 1981. – № 183. – P. 18-27. (in Russian). 5. http://ccmc.gsfc.nasa.gov/modelweb/models/igrf_vitmo.php. 6. Woodfield E. E. Combining incoherent scatter radar data and IRI-2007 to monitor the open closed field line boundary during substorms / E.E. Woodfield, J.A. Wild., A.J. Kavanagh, A. Senior, and S.E. Milan // J. Geophys. Res. – 2010. – № 115. [Электронный ресурс] / URL: http://onlinelibrary.wiley.com/doi/10.1029/2010JA015751/pdf (дата обращения: 25.05.2014).  Received 16.05.2014     62 ISSN 2078-9998. Вісник НТУ “ХПІ”. 2014. № 47 (1089)   UDC 550.380:550.388.1:550.389.5: 537.67 Measurement of the geomagnetic field in the ionosphere using radar methods / T. A. Skvortsov, L. Ya. Emelyanov, A. V. Fesun, D. P. Belozerov // Bulletin of NTU “KhPI”. Series: Radiophysics and ionosphere. – Kharkiv: NTU “KhPI”, 2014. – No. 47 (1089). – P. 57-63. Ref.: 6 titles.  Рассмотрен новый способ измерения геомагнитного поля в ионосфере путем комплексного использования радара вертикального зондирования (ионозонда) и радара некогерентного рассеяния, его возможности и особенности технической реализации, а также первые результаты экспериментального испытания. Ключевые слова: геомагнитное поле, ионосфера, радар некогерентного рассеяния, ионозонд.  Розглянуто новий спосіб вимірювання геомагнітного поля в іоносфері шляхом інтегрального використання радару вертикального зондування (іонозонду) і радару некогерентного розсіяння, його можливості й особливості технічної реалізації, а також перші результати експериментального випробування. Ключові слова: геомагнітне поле, іоносфера, радар некогерентного розсіяння, іонозонд. 63

Measurement of the geomagnetic field in the ionosphere using radar methods

Library of National Technical University "Kharkiv Polytechnic Institute"

 ISSN 2078-9998. Вісник НТУ “ХПІ”. 2014. № 47 (1089) 
 
 
UDC 550.380:550.388.1:550.389.5: 537.67 
 
T.A. SKVORTSOV, D.Sc., Prof., NTU “KhPI”; 
L.Ya. EMELYANOV, PhD, head of department, Institute of Ionosphere, 
Kharkiv; 
A.V. FESUN, PhD student, NTU “KhPI”; 
D.P. BELOZEROV, PhD, junior research scientist, Institute of Ionosphere, 
Kharkiv 
 
MEASUREMENT OF THE GEOMAGNETIC FIELD IN THE 
IONOSPHERE USING RADAR METHODS 
 
A new method for measuring the geomagnetic field in the ionosphere by the integrated use of vertical 
sounding radar (ionosonde) and incoherent scatter radar, its capabilities and features of the technical 
implementation, as well as the first results of an experimental test are considered. 
Key words: geomagnetic field, ionosphere, incoherent scatter radar, ionosonde. 
 
Introduction. Currently, measurements of the geomagnetic field (GMF) in 
the ionosphere are realized at altitudes of flight of the Earth artificial satellites [1]. 
Currently, measurements of the geomagnetic field (GMF) in the ionosphere are 
realized at altitudes of flight of the Earth artificial satellites [1]. At first, the 
magnetic studies, which proved the presence of ionosphere sources, originative the 
changes of the GMF, have been carried out by the third Soviet satellite in 1958 [2]. 
However, measurements of the GMF in the ionosphere by satellites have the 
following weaknesses: 
1. Area of the ionosphere near the ionospheric peak and below is practically 
beyond the observation zone due to short life of satellites in the specified area. At 
the same time, one can expect the greatest GMF variations associated with 
ionospheric currents just in this area. 
2. Continuous monitoring of GMF in a fixed region of space is impossible 
due to the movement of satellites, making it difficult to study the temporal 
variations in GMF. 
3. Simultaneous and continuous measurement of the characteristics of the 
ionosphere and magnetosphere in the area above IS radar is practically impossible. 
This reduces the possibility of studying magnetosphere-ionosphere coupling. 
Thus, the topical problem is to develop methods for measuring the GMF in 
the region near the ionospheric peak and below. 
To investigate the interaction of the magnetosphere and ionosphere, it is 
desirable to carry out combined in time and space measurement of the 
magnetosphere and ionosphere parameters. 
Such measurements can be performed using the method developed at Institute 
of Ionosphere [3] and described below.  
 
© T.A. Skvortsov, L.Ya. Emelyanov, A.V. Fesun, D.P. Belozerov, 2014 
57
 ISSN 2078-9998. Вісник НТУ “ХПІ”. 2014. № 47 (1089) 
 
The method allows measuring the vertical component of intensity of the GMF 
in region near the ionospheric peak under ionospheric observatory by the 
integrated use of vertical sounding radar (ionosonde) and incoherent scatter (IS) 
radar. 
Purpose is to consider the possibility of measuring the geomagnetic field at 
the dense ionosphere altitudes. 
Method for measuring GMF in the ionosphere. The Faraday effect is used 
to measure GMF by IS radar. The effect appears that, when the radio wave passes 
through the magnetized ionospheric plasma from the radar up to a height h and 
backwards, its polarization ellipse is rotated by an angle 
      
h
dllNlHkh
0
,       (1) 
where k =0,0594.f0
–2, f0 is operating frequency, N(h) is the electron density, and 
H is the longitudinal component of the GMF intensity. 
In accordance with (1) and the mean value theorem there is in a specified 
height interval [h1, h2] such height xh , for which 
          
2
1
12
h
hxx
dhhNhkHhhh .   (2) 
Thus, we have from (2): 
 
   
IkN
h
hH
M
x
x


,      (3)  
where 
                     
 
2
1
h
h
dhhFI       (4) 
   
MN
hN
hF   
 
is normalized to the maximum height profile of the electron 
density. 
As seen from (3), if we measure the Faraday effect, the normalized profile 
and maximum of the electron density, we can calculate the intensity of the GMF at 
a certain height within a specified interval of heights. 
For measuring the Faraday effect, transmitter radiates a signal with linear 
polarization and we carry out reception of the left and right circular polarization 
components. At the same time, optimal algorithm of estimate formation is of the 
form [4] 
     
   







hrhr
hrhr
arctgh
sscc
scsc
2121
1221
2
1ˆ ,                                       (5) 
58
 ISSN 2078-9998. Вісник НТУ “ХПІ”. 2014. № 47 (1089) 
 
 
where rc1s2, rc2s1, rc1c2, rs1s2 are estimates of the cross correlations of the signal 
quadrature components at the receiver outputs. 
To determine the  hF  function using the IS radar, the signal power  hP , 
electron  hTe  and ion  hTi  temperatures are measured, and then we calculate and 
normalize a function 
     
  







hT
hT
hhСPhN
i
e12 ,          (6) 
where C is any constant. MN  is measured using ionosonde. 
As it is necessary to radiate a long pulse with circular polarization for  hTe  
and  hTi measurement, we proposed to use the sound signal, consisting of the first 
pulse with circular polarization and the second pulse with linear polarization [1]. 
The first pulse has long duration to ensure the accuracy of temperature 
measurement, and the second pulse has short duration to ensure high correlation 
between ordinary and extraordinary waves, as well as high resolution of IS signal 
for power measurement. 
Thus, we obtain the estimate 
   
INk
h
hH
M
x
x ˆˆ
ˆ
ˆ  ,      (7) 
where HNMMH IINNHH    ˆ,ˆ,ˆ,ˆ ,  , εI, εH, εN are 
errors of measurement. 
Estimation of the method accuracy. Assuming smallness of  , εI, εH, εN 
measurement errors and under condition of absence of their cross-correlation, we 
obtain on basis of (7) a formula for the relative variance of measurement error of 
the longitudinal component of the GMF intensity at the height xh  
2
2
2
2
2
2
2
2
INH
INH 





  ,          (8) 
where 222 ,, IN  are variances of , Nm, and I measurement. 
The error due to uncertainty of the height hx can be significant in case of 
strong GMF change within the altitude range 12 hh  and high requirements to 
accuracy of binding measured GMF intensity to the height. 
If we represent a law of change in the GMF intensity within this altitude 
range as Taylor series and confine oneself to linear approximation 
   00 2
1
hhHhH   ,      (9) 
59
 ISSN 2078-9998. Вісник НТУ “ХПІ”. 2014. № 47 (1089) 
 
where H0 – GMF intensity at the height 
2
21
0
hh
h

 , we obtain 
2
2
2
2
2
2
2
2
2
2
HINH
I
M
NH









  ,     (10) 
where 
I
I
2
1 ,   dhhhhFI h
h 
2
1
01 .  
The height profile of the electron density can be approximated by the function 
  
        
2
000 hhbhhahFhF  .  (11) 
Then 
 
 
 
2
0
2
2
2
2
2
2
2
2
2
12 






 








 
hF
ha
HINH
I
M
NH . (12)  
We assume that the variance  r  12 22  makes the main contribution 
to the variance (12). Here 2  is the variance of the error of the parameter Φ, and r 
is the cross-correlation of errors for the heights h1 and h2, which depends on the 
amplitude-frequency response of the receiver. 
We can show that the Cramér–Rao bound for the variance 2 under optimal 
measurement algorithm (5) is defined by formula  
 






















12
22
2
2112
2
2
2
1
2
1
14
111
1
qq
M
qqqq
,  (13) 
where  is the coefficient of correlation between the ordinary and extraordinary 
waves, M is the number of processed sounding cycles, q1 and q2 are the signal-to-
noise ratio at the receiver outputs. The values 2   for the case of М=5800 
(accumulation during a 15-min session) are presented in Table 1.  
 
Table 1 – Standard deviation of error in measurement of the angle of the polarization ellipse 
rotation 
 q1 = q2 = 2 q1 = q2 = 4 q1 = q2 = 10 q1 = q2 = 50 
 = 0.5 0.022 0.017 0.014 0.012 
 = 0.7 0.0165 0.012 0.009 0.007 
 = 0.9 0.0126 0.008 0.005 0.004 
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Such potential accuracy allows expecting the fact that measurement errors in 
intensity of GMF can be comparable with its disturbances during geomagnetic 
storms. 
Results of experimental test of the method. Some results of the first test of 
the described method for measuring GMF are presented below. In this case, the 
one channel of the transmitter and one of two orthogonal antenna dipoles were 
used to emit linearly polarized waves. When sampling a signal, we used a step in 
height =4550 m. Because of the small step, the integral (4) for the i-interval of 
heights was calculated by the formula 
       iixi hFhFhI 215,0  .                 (14) 
Parameter Φ was determined according to the algorithm (5). The signal power 
was determined for the echo signal from the short pulse by equalizing the receiver 
gains, subtraction of the noise power from the signal plus noise power, accounting 
gain of antenna switches with gas-filled dischargers for each segment of the radar 
sweep, and summing the results. 
Dependence of vertical component of intensity of GMF on a height, got at 
watching 15 minutes presented on Fig. 1. 
 
 
Fig. 1 – Intensity of Hz-component of geomagnetic field.  
Local time in Kharkiv 13:20–13:36 (12.11.2012). 
  
Curve 1 corresponds to the DGRF/IGRF Geomagnetic Field Model of [5], 
and curves 2 and 3 got experimentally. Curve 2 got with the use of temperatures in 
accordance with the model of IRI-2007 [6], and curve 3 – with the use of the 
temperatures measured by IS radar. A stroke vertical marks the height of a 
maximum of ionizing. 
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Apparently, in area of high concentration (230-300 kilometers) the measured 
values are near to the model.  
It is of interest that the size of the measured intensity on the average a bit 
increases with a height, unlike the DGRF/IGRF model. In principle, such effect 
can be caused by the error of measuring of temperatures. A calculation was 
therefore produced with the use of model of temperatures of IRI-2007, that  
confirmed the effect of increase of vertical component of intensity with a height. 
This fact requires additional research. However it is known that GMF in an 
ionosphere can have noticeable local differences from the accepted models [1, 2].  
Conclusion. Theoretical estimation and experimental test indicate that it is 
possible to measure the vertical component of the GMF intensity in the ionosphere 
by the proposed method with a relative root mean square error of a few percent. 
We can further improve the accuracy of these measurements, in particular due to 
the following: 
– correction of errors due to errors in setting the polarization of the antenna; 
– improving the signal-to-noise ratio by using two channels of the transmitter 
for formation of the sound signal with linear polarization; 
– use of the polarization modulation of the sound signal, which allows to 
measure the electron and ion temperatures simultaneously with the signal 
polarization (Faraday rotation measurement). 
Finally, we can evaluate quality of the GMF measurement using IS radar and 
ionosonde after optimization of equipment and measurement algorithms, and also 
the analysis of experimental data with the use of a sufficiently large statistical 
material. 
 
References: 1.  Ionosphere geomagnetic field: Comparison of IGRF model prediction and satellite 
measurements 1991 – 2010 [Электронный ресурс] // Radio Sci. – 2011. – № 46. – P. 1-10. – URL:  
http://onlinelibrary.wiley.com/doi/10.1029/2010RS004529/pdf (дата обращения: 25.05.2014). 
2. Aleksandrov S.G. Soviet satellites and spaceships / S.G. Aleksandrov, R.E. Fedorov. – Moscow: 
Academic Science, 1961. – 440 p. (in Russian). 3. Patent 71162. Ukraine, G01S 13/95. A method of 
measuring the parameters of the ionosphere and magnetosphere / L. Ya. Emelyanov, T. A. Skvortsov, 
I. B. Sklyarov, A. V. Fesun.; patented 14.11.2011; published 10.07.2012, Bulletin № 13 (in Ukrainian). 
4. Tkachev G.N. The measurement of phase differential between ordinary and extraordinary waves 
which was scattered by thermal fluctuation electron density of ionosphere / G.N. Tkachev, V.D. Karlov 
// Harbinger KPU. – 1981. – № 183. – P. 18-27. (in Russian). 
5. http://ccmc.gsfc.nasa.gov/modelweb/models/igrf_vitmo.php. 6. Woodfield E. E. Combining 
incoherent scatter radar data and IRI-2007 to monitor the open closed field line boundary during 
substorms / E.E. Woodfield, J.A. Wild., A.J. Kavanagh, A. Senior, and S.E. Milan // J. Geophys. Res. – 
2010. – № 115. [Электронный ресурс] / URL: 
http://onlinelibrary.wiley.com/doi/10.1029/2010JA015751/pdf (дата обращения: 25.05.2014). 
 
Received 16.05.2014 
 
 
 
 
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UDC 550.380:550.388.1:550.389.5: 537.67 
Measurement of the geomagnetic field in the ionosphere using radar methods / 
T. A. Skvortsov, L. Ya. Emelyanov, A. V. Fesun, D. P. Belozerov // Bulletin of NTU “KhPI”. Series: 
Radiophysics and ionosphere. – Kharkiv: NTU “KhPI”, 2014. – No. 47 (1089). – P. 57-63. Ref.: 6 titles. 
 
Рассмотрен новый способ измерения геомагнитного поля в ионосфере путем комплексного 
использования радара вертикального зондирования (ионозонда) и радара некогерентного 
рассеяния, его возможности и особенности технической реализации, а также первые результаты 
экспериментального испытания. 
Ключевые слова: геомагнитное поле, ионосфера, радар некогерентного рассеяния, 
ионозонд. 
 
Розглянуто новий спосіб вимірювання геомагнітного поля в іоносфері шляхом 
інтегрального використання радару вертикального зондування (іонозонду) і радару 
некогерентного розсіяння, його можливості й особливості технічної реалізації, а також перші 
результати експериментального випробування. 
Ключові слова: геомагнітне поле, іоносфера, радар некогерентного розсіяння, іонозонд. 
63


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Measurement of the geomagnetic field in the ionosphere using radar methods

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Measurement of the geomagnetic field in the ionosphere using radar methods

Abstract

Similar works

Full text

Available Versions

Electronic National Technical University &quot;Kharkiv Polytechnic Institute&quot; Institutional Repository (eNTUKhPIIR)

Library of National Technical University "Kharkiv Polytechnic Institute"

Electronic National Technical University "Kharkiv Polytechnic Institute" Institutional Repository (eNTUKhPIIR)