# Influence of Ionospheric Irregularities on GNSS Remote Sensing

Authors: M. V. Tinin
Journal: Advances in Meteorology
 (2015)

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## Abstract

We have used numerical simulation to study the effects of ionospheric irregularities on accuracy of global navigation satellite system (GNSS) measurements, using ionosphere-free (in atmospheric research) and geometry-free (in ionospheric research) dual-frequency phase combinations. It is known that elimination of these effects from multifrequency GNSS measurements is handi-capped by diffraction effects during signal propagation through turbulent ionospheric plasma with the inner scale being smaller than the Fresnel radius. We demonstrated the possibility of reducing the residual ionospheric error in dual-frequency GNSS remote sensing in ionosphere-free combination by Fresnel inversion. The inversion parameter, the distance to the virtual screen, may be selected from the minimum of amplitude fluctuations. This suggests the possibility of improving the accuracy of GNSS remote sensing in meteorology. In the study of ionospheric disturbances with the aid of geometry-free combination, the Fresnel inversion eliminates only the third-order error. To eliminate the random TEC component which, like the measured average TEC, is the first-order correction, we should use temporal filtering (averaging).


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## Body

## 1. Introduction

At present, remote sensing methods relying on ground-based and low-orbit observations of signals from global navigation satellite systems (GNSS) such as GLONASS and GPS are finding ever-widening application in environmental research [1–8]. These methods allow remote diagnostics of wide sectors of overground space, which makes them attractive for use especially in the Arctic region. However, the spatially and temporally variable ionosphere significantly affects the accuracy and reliability of GNSS remote sensing. Therefore, it is necessary to study effects of ionospheric irregularities on GNSS measurements and to find possibilities of their elimination. Unfortunately, the ionospheric variability impedes elimination of ionospheric errors through modeling. Particularly, the ionospheric error reduction with the aid of the well-known Klobuchar model [9, 10] does not exceed 50% [11]. A more precise approach makes use of the frequency dependence of ionospheric error. Here we will restrict our consideration to phase measurements as being more precise versus measurements of time delay of signal (code measurements). Let us have a phase path φf measured taking into account the whole number of wavelengths determined by methods for phase ambiguity resolution (see, e.g., [12]). Then the first geometrical optics approximation yields [9, 10](1)φf=D-40.3f2I1gf+⋯.Here the pseudo distance D comprises, besides the distance between a satellite and a ground-based observer, all other frequency-independent corrections (errors opposite in sign) to phase path (e.g., delay in the troposphere); consider(2)I1g=∫z0ztNz′dz′is the electron density integral along a ground-based-receiver-satellite line, which is called total electron content (TEC); f is the radiation frequency. The first-order correction, the second term in (1) proportional to f-2, describes ionospheric plasma effects on GNSS signal propagation, ignoring diffraction effects, geomagnetic field effect (second-order correction), and ray bending (the third-order correction). Here we use a generally accepted (see, e.g., [13–15]) notation of the i-order correction for the term in observation equations (1) and below, which is proportional to f-i-1.GNSS remote sensing methods (see, e.g., [1–8]) rest on the relation of terms on the right-hand side of (1) with environmental parameters. The distance included into D depends on the observation point. Therefore, if the observer is on the Earth’s surface, motions of this surface can be seen in D variations. On the other hand, the atmospheric phase delay of signal included into D is determined by the refractive index which depends on atmospheric temperature and density and vapor pressure. Thus, D measurements can provide parameters important for meteorology. Estimating the second term in (1) allows us to acquire data on ionospheric plasma disturbances from the spatial and temporal TEC behavior.In order to find the pseudo distanceD and TEC I1g from (1), we need to perform dual-frequency measurements. These measurements give the following system:(3)φ1=φgf1=D-40.3I1gf12,φ2=φgf2=D-40.3I1gf22.By solving system (3) for two unknowns D and I1g, we obtain the result of the dual-frequency measurements:(4)D≈D2=φ1f12-φ2f22f12-f22,(5)I(2)=f12f2240.3φ1-φ2f12-f22.Equations (4) and (5) are so-called ionosphere-free and geometry-free observation combinations, respectively [16].The dual-frequency measurements from formula (4) reduce the ionospheric distance-measurement error by 99% [17]. In practice, this is usually quite sufficient. However, in atmospheric investigations, in studies of crust movements during earthquakes and volcanic activity and other precisional GNSS measurements, this decimetric accuracy is not sufficient. Therefore, many researchers have been exploring the possibility of improving the accuracy of dual-frequency measurements.The second-order correction which takes into account geomagnetic effects on the ionospheric refractive index is ignored in dual-frequency measurements (3). This correction has been examined in many studies (see, e.g., [1, 13–15, 18–21]). It has been revealed that in the thin layer approximation whose error is 1-2 mm this correction is expressed through the first-order one [13, 15, 22]. Therefore, it can be taken into account by calculating with the familiar geomagnetic field model [1, 13–15] or by considering directly in dual-frequency measurements through modification of the ionosphere-free combination [22, 23].After accounting for the second-order residual error, further accuracy improvement is associated with the consideration of the third-order error. In the geometrical optics approximation, this error is largely attributed to the path deviation from the straight line and can be eliminated in triple-frequency measurements [23, 24]. Yet, like dual-frequency measurements, triple-frequency measurements yield a system of three observation equations from which we can find D, first-order correction (TEC), and third-order correction (ray bending). This can only be done, however, when scales of ionospheric irregularities exceed the Fresnel radius, and the geometrical optics approximation is applicable. Unfortunately, scales of ionospheric irregularities range widely from tens of meters to tens of kilometers [25–27]. In this case, the lower bound (so-called inner scale) of the ionospheric turbulent spectrum may be less than the Fresnel radius which varies with the elevation angle in the 200–700 m range (see, e.g., [23]). As a result, in triple-frequency measurements, as compared to dual-frequency ones, only the average error decreases, whereas the random error variance increases [23, 28].The above results of studies of GNSS ionospheric errors largely refer to the results obtained with ionosphere-free combination (4), that is, during GNSS measurements of frequency-independent characteristics such as crust movement and tropospheric parameters. At present, however, GNSS measurements are widely used for studying traveling ionospheric disturbances as well as the ionosphere’s behavior during earthquakes and magnetic storms [7, 29]. Yet TEC measurements (2) obtained from geometry-free combination (5) are utilized. It is obvious that in the study of this large-scale structure of the ionosphere and its dynamics, a significant role in formation of the measurement error will be played by ionospheric irregularities of less scale. In this paper, therefore, we will present results of investigations into residual ionospheric errors of dual-frequency GNSS measurements for both combinations (4) and (5).


## 2. Ionospheric Effects in Single-Frequency GNSS Measurements

Consider the behavior of GNSS signal in the form of harmonic wave with the time dependenceU(r)exp⁡-iωt. Since the GNSS satellite is far from the ionosphere, our task reduces to the study of incidence of the plane-wave U0z=A0exp⁡ikz-z0 with k=2π/λ (λ is the wavelength) on an inhomogeneous anisotropic ionosphere. Let the z-axis of our Cartesian coordinate system x,y,z=ρ,z pass through the source point r0=0,z0 and the point 0,zt located in the vicinity of the receiving point rt=ρ,zt. At GNSS frequencies, sizes of ionospheric irregularities lN usually exceed λ(6)klN=2πlNλ≫1.With condition (6) fulfilled, when solving the wave equation, we use the second Rytov approximation and obtain the following solution [30, 31]: (7)Ur=U0zexp⁡Φ1r+Φ2r,where(8)Φ(r)=Φ1(r)+Φ2(r)is the complex phase whose first Φ1(r) and second Φ2(r) approximations have the forms:(9)Φ1r=-ik40.3f2∫z0ztdz′∫-∞∞∫-∞∞d2κNκκ,z′·exp⁡-iκ22zt-z′k+iκρ,Φ2r=ik240.3f22∫z0ztdz′·∫z0z′∫z0z′dz1dz2∫-∞∞∫-∞∞d2κ1·∫-∞∞∫-∞∞d2κ2κ1κ2Nκκ1,z1Nκκ2,z2·exp⁡⁡-iStκ1,κ2,z′,z1,z2,k+iκ1+κ2ρ.Because the geomagnetic field effect on the velocity of GNSS signal propagation in the ionosphere can be taken into account, say, in the modified dual-frequency reception [22, 23], we do not discuss it here. In (9)(10)Nκκ,z=12π2∫-∞∞∫-∞∞d2ρNρ,zexp⁡-iκρis the 2D spectrum of electron density of ionospheric plasma and(11)Stκ1,κ2,z′,z1,z2,k=0.5κ12zt-z1+0.5κ22zt-z2+κ1κ2zt-z′k.The imaginary part of the complex phase Φ(r) determines the GNSS signal phase which, with the point of observation on the z axis (ρ=0), is(12)ImΦ(r)ρ=0+kz-z0=kφr.The real part of the complex phase Φ(r) is associated with the level (13)ReΦ(r)ρ=0=ln⁡A(r)A0.Equations (12), (8), and (9) for the phase path φr yield the observation equation [31]:(14)φf=D-40.3f2I1df-40.3f22I3df,where (15)I1df=∫z0ztdz′∫-∞∞∫-∞∞d2κNκκ,z′·cos⁡κ22zt-z′k,I3df=-0.5∫z0zdz′∫z0z′∫z0z′dz1dz2·∫-∞∞∫-∞∞d2κ1∫-∞∞∫-∞∞d2κ2κ1κ2×Nκκ1,z1Nκκ2,z2·cos⁡Sκ1,κ2,z′,z1,z2.The second term on the right-hand side in (14) is the first-order correction which, unlike (2), accounts for diffraction effects; the third term is the diffraction variant of the third-order correction. When the minimum size of irregularities lm=1/max⁡κ exceeds the Fresnel radius rFr(16)lm2≫rFr2≡zt-z′k,(14) and (15) give the geometrical optics approximation [23, 31](17)φgf=D(1)≈D-40.3I1gf2-40.32f-4I3g,where(18)I3g=0.5∫z0zt∫z0z∂Nρ,z′∂ρρ=0dz′2dz.In this case, unlike first approximation formula (1), besides the first-order correction proportional to the total electron content I1g=∫z0ztNz′dz′, the third-order correction (the final term on the right-hand side in (17)) associated with the path deviation from the straight line in the inhomogeneous ionosphere is taken into consideration. When ignoring the third-order correction, (17) yields (1) from which follow formulas (4) and (5) of dual-frequency measurements.Thus, the errors to be considered are associated in the geometrical optics approximation with the GNSS ray bending. Moreover, it is necessary to correctly describe the interaction of the wave field with the irregularities for which conditions of the geometrical optics approximation (16) are not fulfilled. Expression (14), derived in the second Rytov approximation, accounts both for the ray bending and for the diffraction effects.The electron density of ionospheric plasma is normally represented as sum of two components(19)Nr=N-r+N~r.Here N-r is the average electron density, that is, density of the background ionosphere and its medium-scale disturbances being of the utmost interest for ionosphere researchers [7, 29]; N~r is the random component of electron density associated with small-scale irregularities.The electron densityN-r of the large-scale background ionosphere and its medium-scale disturbances largely fulfills the condition of validity of the geometrical optics approximation (16) at GNSS frequencies. Besides, ray bending effects in the background ionosphere are sufficiently small [13, 24, 31]. Therefore, diffraction effects in GNSS measurements are associated first and foremost with random small-scale irregularities caused by ionospheric plasma turbulence.Random ionospheric irregularities are usually represented by a random, quasi-homogeneous, normally distributed field with a given spectrumΦNκ,r related to the correlation function ΨNΔr,r=N~rN~r+Δr by the relation (20)ΦNκ,r=2π-3∫-∞∞∫-∞∞∫-∞∞d3ΔrΨNΔr,r·exp⁡-iκΔr.The spectrum of turbulence irregularities is often as follows [32]:(21)ΦNκ,z=σN2zΓp/2κ0p-3π3/2Γ(p-3)/2κ02+κ2-p/2exp⁡-κ2κm2,where σN2z is the dispersion of electron density fluctuations, κ0=2π/L0, κm=2π/lm.Spectrum (21) is bounded by the outer scale L0 in the order of several tens of kilometers and by the inner scale lm≈50–700 m.By substituting (19) in (15), we can express characteristics of the random Iidf (i=1,3) through corresponding characteristics of the random field Nr. For spectrum (21) the average I-idf=Iidf and the correlation functions Ψidf1,f2=Iidf1Iidf2 are determined by the following relations [31]:(22)I0=I1g=∫z0ztN-z′dz′,(23)I-3df=I3d=kπΓ2-p/2Γp/2κ0p-3p/2-1Γ(p-3)/2κmp-2·∫z0ztdz′σN2z′ImQp/2-1z′,k1,where Qz′,k=1-iκm2zt-z′/k,(24)Ψ1df1,f2=I~1df1I~1df2=2πΓp-2/2κ0Γ(p-3)/2∫z0ztσN2(z)dz·1+κ0κmp-2×πΓp-2/2-12sin(πp/2)πΓp-2/2-12sin(πp/2)·ReQp/2-1z,k++Qp/2-1z,k-,(25)k+,--1=0.5k1-1±k2-1,ki=2πfic,Ψ3df1,f2=I~3df1I~3df2=Ψ3Bf1,f2+Ψ3Rf1,f2,(26)Ψ3Bf1,f2=πΓp/2Γ2-p/2κ0p-3Γ(p-3)/2κmp-4·∫z0ztdz′∫z0z′dz′′p-Nz′p-Nz′′×∫z0z′′dz1σN2z1·ReQp/2-2z1,k++Qp/2-2z1,k-,(27)Ψ3Rf1,f2=Γp/2κ0p-3Γ(p-3)/2κmp-422Γ4-p×∫z0ztdz′∫z0z′dz′′∫z0z′′dz1σN2z1·∫z0z′′dz2σN2z2∫-ππdφ-cos⁡2φ-∫0πdφ+sin3-pφ+×ReV+p-4f1,f2,z′,z′′+V-p-4f1,f2,z′,z′′+V+p-4f1,f2,z′′,z′+V-p-4f1,f2,z′′,z′,(28)V+,-f1,f2,z′,z′′=2Qz1,k+,-Qz2,k+,--icos⁡φ-sinφ+κm2zt-z′k1±zt-z′′k2.Note that contrary to the second term, the first term on the right-hand side in (25) accounts for the regular-refraction influence on the random component of the third-order error. According to the numerical simulation, the contribution of the first term is much less than that of the second term [31].


## 3. Ionospheric Effects in Dual-Frequency GNSS Measurements

After substituting (14) in dual-frequency ionosphere-free combination (4), we obtain(29)Dd2f1,f2≈D-ΔD1d2f1,f2-ΔD3d2f1,f2,where(30)ΔD1d(2)f1,f2=40.3I1d(f1)-I1d(f2)f12-f22is the first-order correction and(31)ΔD3d(2)f1,f2=40.32I3d(f1)f1-2-I3d(f2)f2-2f12-f22is the third-order correction.By substituting (14) in geometry-free combination (5), we get (32)Id2f1,f2=I0-ΔI1d2f1,f2-ΔI3d2f1,f2,where I0 is, according to (22), the mean first-order TEC value,(33)ΔI1d(2)(f1,f2)=I~1d(f1)f22-I~1d(f2)f12f12-f22is the random component of the first-order TEC, and (34)ΔI3d(2)(f1,f2)=40.3I3d(f1)f2/f12-I3d(f2)f1/f22f12-f22is the third-order TEC correction.Note that in (32), unlike (29), both the measured mean TEC I0 and its random component ΔI1d(2)(f1,f2) are first-order corrections.Now it is easy to find statistical characteristics of dual-frequency measurement errors. For measurements with ionosphere-free combination (4), the average correction is equal to the average third-order correction [23]:(35)ΔDd2f1,f2≈ΔD3d2f1,f2=-40.32I-3df1f1-2-I-3df2f2-2f12-f22,where the average I-3R(f) is determined by (23). The correction variance of this combination is [23](36)ΔD~d2f1,f22=ΔD~1d2f1,f22+ΔD~3d(2)(f1,f2)2,where the first-order correction variance is (37)ΔD~1d2f1,f22=40.3f12-f222·Ψ1d(f1,f1)+Ψ1d(f2,f2)-2Ψ1d(f1,f2)and the third-order correction variance is(38)ΔD~3d2f1,f22=(40.3)2f12-f222×f1-4Ψ3df1,f1+f2-4Ψ3df2,f2-2f1-2f2-2Ψ3df1,f2.The correlation functions Ψ1d(f1,f2) and Ψ3d(f1,f2) are defined by (24) and (25)–(28), respectively.For measurements with geometry-free combination (5), the average correction is(39)ΔId2f1,f2=ΔI3d2f1,f2=40.3I-3d(f1)f2/f12-I-3d(f2)f1/f22f12-f22.Variance of this correction is(40)ΔI~d2f1,f22=ΔI~1d2f1,f22+ΔI~3d(2)(f1,f2)2,where (41)ΔI~1d2f1,f22=f12f12f12-f122·f1f2-2Ψ1df1,f1+f1f22f1f2-2·Ψ1df2,f2-2Ψ1df1,f2is the first-order correction variance and(42)ΔI~3d2f1,f22=40.3f12-f222·f1f2-4Ψ3df1,f1+f1f24f1f2-4·Ψ3df2,f2-2Ψ3df1,f2is the third-order correction variance.To assess probable errors in dual-frequency measurements, we have performed numerical simulation with (35)–(42). For the model of background ionospheric layer we took the Chapman layer(43)N-z=fc280.6exp⁡0.51-ζ(z)-exp⁡ζ(z),where ζ(z)=z2+2zResinα+Re2-hm-Re/H and fc=15×106 Hz is the layer critical frequency; Re=6370 km is the Earth’s radius and H=70 km is the characteristic scale of the layer; hm=320 km is the height of its maximum. Such parameters corresponded to a vertical electron content of 81 TECU (1TECU=1016 m2). Random ionospheric irregularities were specified by spectrum (21). Yet we took values for the outer scale L0=20 km, for the index p=11/3, and for the coordinate dependence of rms deviation of electron density fluctuation σN(r) we assumed the proportionality to the background electron density N-(r): σNr=σ0N-r. In the calculations, we set σ0=0.1, and for radiation frequencies we took GPS frequencies f1=1572.42×106 Hz, f2=1227.6×106 Hz.Figures1 and 2 illustrate elevation angle dependence of average (a) and standard deviations (b) of corrections of first (dashed line) and third (solid line) orders at inner sizes of 50 m (blue line), 200 m (green line), and 1000 m (red line), using the ionosphere-free (Figure 1) and geometry-free (Figure 2) combinations.Figure 1
Elevation angle dependence of average (a) and standard deviations (b) of corrections of first (dashed line) and third (solid line) orders for ionosphere-free combination (4) at inner sizes of 50 m (blue line), 200 m (green line), and 1000 m (red line).
(a)
(b)Figure 2
The same as in Figure1 for geometry-free combination (5).
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(b)A characteristic property of absolute average corrections and standard deviations is their increase with decreasing elevation angle (see Figures1 and 2) associated with the wave-path extension in the inhomogeneous layer. What stands out here is (see Figure 1(a)) the weak dependence of the average correction in ionosphere-free combination (4) on the inner scale lm. This is due to the fact that the greatest contribution to this correction, as is clear from (23), is made by the irregularities located at a distance z′ where κm2zt-z′/k≫1. In this area, the dependence of the integral in (23) on κm=2π/lm is offset by the factor before the integral. Figure 1(b) shows that the standard deviation of the third-order correction (solid line) in D measurements can exceed the standard deviation of the first-order correction (dashed line). The weak dependence of the standard deviation of the first-order (dotted lines in Figure 2(b)) on the inner scale is not associated with diffraction effects, as in the case of the average correction in Figure 1(a). Here we deal with phase variance that, as is known [32], is generally determined by large-scale irregularities and slightly depends on the high-frequency part of irregularity spectrum which is associated with the inner scale lm. The results of Figure 2 suggest that a probable error in TEC measurements may reach 1 TECU. Third-order corrections increase with decreasing inner sizes, and, as their averages (Figure 2(a)) are other than zero, they cannot be eliminated after time averaging. This, of course, must be taken into account in studying features of ionospheric disturbances of the same order via GNSS. The results of Figure 1 also suggest probable errors in D measurements to be of order of several centimeters, which is comparable with effects measured with GNSS in atmosphere [7].In [23], numerical simulation was used to explore the possibility of improving the accuracy of GNSS measurements with increasing number of frequencies. It emerged that when the inner scale exceeds the Fresnel radius, the transition from dual-frequency to triple-frequency measurements reduces the ionospheric correction. However, if the Fresnel radius exceeds the inner scale, such a transition decreases only the average correction. The correction variance in this case only rises. Let us, therefore, consider possibilities of improving the accuracy of GNSS measurements with the aid of spatial processing.


## 4. Eliminating GNSS Measurement Errors via Fresnel Inversion

As is well known, with the Green function at a given wave field on the plane where the wave leaves the inhomogeneous medium, it is possible to find the field on another, distant plane. When the medium between these planes is homogeneous, we can take the field of point source in free space as the Green function. This Kirchhoff approximation is widely used for analyzing wave propagation behind the slightly inhomogeneous layer. Yet the wave field where the wave leaves this layer can be described using the geometrical optics approximation. The Kirchhoff formula allows us to calculate this field in the distant region exhibiting various diffraction effects, caustics, and strong fluctuations for which the geometrical optics approximation does not work. Since the small-angle approximation is applicable to large-scale irregularities, the Kirchhoff formula takes the form of Fresnel transform [3]:(44)Uρ,z≈-ik2π∫S′Uρ′,zb·exp⁡ikρ-ρ′22zt-zb+ikzt-zbd2ρ′.When the inhomogeneous layer is sufficiently thin, it modulates only the transmitted wave phaseUρ′,zb=U0zbexp⁡ikφbρ′,zb and from (44) we can obtain the phase screen model which has been used for analyzing various problems of wave propagation in a randomly inhomogeneous ionosphere.On the other hand, inversion of Fresnel transform (44) (Fresnel inversion) allows us, by measuring the field on the plane z=zt, to find the field on the plane z=zb nearby the irregularity where diffraction effects are absent and thus increases the accuracy of dual-frequency combinations (4) and (5) in determining D and I. Besides reduction of diffraction effects, ray path variations are low and consequently the third-order error is small nearby the irregularity. Let us analyze the action of the inverse operator in the form of inverse Fresnel transform U(ρ,ρ0):(45)U^ρ∗,zb=L^bUρ,zt=ik2πzt-zb·∫-∞∞d2ρUρ,ztexp⁡-ikρ∗-ρ22zt-zb.Substituting second Rytov approximation (7)–(11) in (45) yields (for details see [28]) formulas analogous to the above ones. When the virtual screen plane z=zb is in a homogeneous medium between an irregularity and an observer, it is the natural result of using the Kirchhoff formula in determining the field on the plane z=zb from values of this field on the plane z=zt. However, formally we may apply transform (45) at any position of the virtual screen. This is also suggested by the results of using the double weighted Fourier transform to study wave propagation through a distant inhomogeneous region [33].Figure3 presents the results of calculation of the average correction (а) and the standard deviation (b) of first- and third-order corrections in determining the pseudo distance D from ionosphere-free combination (4) after Fresnel processing (45) of GNSS measurements. These results are represented as virtual screen position functions at lm=50 m for elevation angles of 90∘ (blue line), 50∘ (green line), and 20∘ (red line). After spatial processing (45), the condition of validity of geometrical optics approximation (16) takes the form(46)lm2≫rFrb2≡zb-z′k.As is seen from (46), bringing the virtual screen nearer to the irregularity (zb→z′) leads to the elimination of diffraction effects. Note that zb=0 corresponds to the above case of absence of spatial processing. Figure 3 shows that the absolute average corrections (see Figure 3(a)) and standard deviations (see Figure 3(b)) decrease with increasing distance zb between the observer and the screen and have minimums at the defined zb=zbmin⁡. These minimums for a narrow region with irregularities are close to zero. However, in the case of large extent of the region with irregularities, condition (46) works only for some irregularities and error values in zb=zbmin⁡ increase. According to the analysis, these minimums are located at distances corresponding roughly to the points of intersection of the observer-satellite line and the layer maximum which for our model of irregularities corresponds to the σN(r) maximum. With this position of the virtual screen, the error is minimal because condition (46) is fulfilled for the most part of the inhomogeneous layer. From the well-known relation between wave amplitude fluctuations and diffraction effects [32] follows an analogous dependence of the amplitude scintillation index on the screen position after spatial processing (45).Figure 3
Virtual screen position dependencies of the average (a) and standard deviation (b) of corrections of first (dashed line) and third (solid line) orders for ionosphere-free combination (4) at the inner scale of 50 m and elevation angles of 90° (blue line), 50° (green line), and 20° (red line).
(a)
(b)Figure4 for the L1 frequency (f1=1572.42×106 Hz) with the same parameters presents calculations of the amplitude scintillation index U(ρ,ρ0)4-U(ρ,ρ0)22/U(ρ,ρ0)22 of the wave processed by the algorithm of Fresnel inversion (45). This figure implies that processing (45) reduces the scintillation index and the minimum of amplitude fluctuations is very close to the minimum of GNSS measurement errors.Figure 4
Virtual screen position dependencies of the scintillation index for the frequency L1 (f1=1572.42×106 Hz) for the same elevation angles as in Figure 3.In Figure5 are the results of the simulation for dual-frequency TEC measurements with geometry-free combination (5). Referring to Figure 5(a), in this case the Fresnel inversion can also reduce the average correction of TEC measurements through the proper choice of distance to the virtual screen zb. However, the standard deviation of the first-order correction (dashed lines in Figure 5(b)) varies slightly during spatial processing. This is attributed to the said (Figure 2(b)) relationship between the variance of the first-order correction and the variance of the first-approximation phase which weakly depends on diffraction effects [32]. However, the standard deviation of the third-order correction (solid lines in Figure 5(b)) in optimum Fresnel processing (at zb=zbmin⁡) reduces due to elimination of the diffraction effects and decrease in the ray bending.Figure 5
The same as in Figure3 for geometry-free combination (5).
(a)
(b)


## 5. Conclusion

In this study, ionospheric errors of GNSS remote sensing using both ionosphere-free and geometry-free combinations were analyzed. In the former case, we demonstrated the possibility of reducing residual ionospheric errors in ionosphere-free combination by Fresnel inversion. The inversion parameter, the distance to the virtual screen, may be selected from the minimum of amplitude fluctuations. This suggests the possibility of improving the accuracy of GNSS remote sensing in meteorology.In investigations into ionospheric disturbances through geometry-free combinations, the Fresnel inversion eliminates only the third-order correction. To eliminate the random TEC component which, like the measured average TEC, is the first-order correction, we should use temporal filtering (averaging). However, measurements of this random TEC component allow us to examine the fine structure of ionospheric plasma via GNSS.The Fresnel spatial processing requires constructing a phase GNSS array of sufficiently large sizes. Despite the difficulty in constructing this array, it seems necessary to develop the array, taking into account feasibility of using it in many fields of research on the troposphere, ionosphere, earthquakes, and volcanic activity.



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