Coherent radar imaging (CRI), which is fundamentally a beamforming process, has been used to create images of microscale, reflectivity structures within the resolution volume of atmospheric Doppler radars. This powerful technique has the potential to unlock many new discoveries in atmospheric studies. The Turbulent Eddy Profiler (TEP) is a unique 915 MHz boundary layer radar consisting of a maximum of 91 independent receivers. The TEP configuration allows sophisticated CRI algorithms to be implemented providing significant improvement in angular resolution. The present work includes a thorough simulation study of some of the capabilities of the TEP system. The pulse pair processor, used for radial velocity and spectral width estimation with meteorological radars, is combined with beamforming technique, in an efficient manner, to the imaging radar case. By numerical simulation the new technique is shown to provide robust and computationally efficient estimates of the spectral moments. For this study, a recently developed atmospheric radar simulation method is employed that uses the ten thousand scattering points necessary for the high resolution imaging simulation. Previous methods were limited in the number of scatterers due to complexity issues. Radial velocity images from the beamforming radar are used to estimate the three-dimensional wind field map within the resolution volume. It is shown that a large root mean square (RMS) error in imputed three-dimensional wind fields can occur using standard Fourier imaging. This RMS error does not improve even as SNR is increased. The cause of the error is reflectivity variations within the resolution volume. The finite beamwidth of the beamformer skews the radial velocity estimate, and this results in poor wind field estimates. Adaptive Capon beamforming consistently outperforms the Fourier method in the quantitative study and has been demonstrated to enhance the performance compared to the Fourier method.
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 Techniques similar to CRI have been used for a wide range of applications, from seismology, sonar, medical imaging, and radio astronomy [e.g., Haykin, 1985]. The term beamforming is used in many other fields to describe the imaging process. The first use of CRI for probing of the atmosphere was provided by Kudeki and Sürücü , who used the Jicamarca Radio Observatory for observations of the equatorial electrojet. They used a Fourier-based method for imaging which has well-known resolution limitations. In an effort to increase angular resolution, the Maximum Entropy method, made popular in the radio astronomy community, has been used for imaging of F region irregularities [Hysell, 1996; Hysell and Woodman, 1997]. Subsequently, much research has been conducted related to finding the optimum algorithm, in terms of angular resolution, computational complexity, and robustness [Yu et al., 2000]. For example, the Capon algorithm [Capon, 1969] has proven to have moderate computational complexity and resolution approaching that of the Maximum Entropy method under certain conditions [Palmer et al., 1998].
 A generalized presentation of CRI by Woodman  provided a mathematical foundation for this promisingtechnique. Further, many statistical studies have been presented in the literature comparing the various algorithms available for CRI [e.g., Yu et al., 2000; Chau and Woodman, 2001]. Undoubtedly, new algorithms will be devised with ever improving resolution and robustness.
 Given these technical and scientific advances, the use of CRI is becoming commonplace in newly developed atmospheric radar systems. For example, a French stratosphere-troposphere (ST) radar has recently been outfitted with CRI capabilities allowing intriguing studies of aspect sensitivity at VHF wavelengths [Hélal et al., 2001]. New commercial systems are also being deployed throughout the world with multiple receivers capable of CRI research [e.g., Yu et al., 2001]. In addition to the Jicamarca Radio Observatory, many of the most powerful mesosphere-stratosphere-troposphere (MST) radars are being upgraded to allow CRI studies. For example, the MU radar [Fukao et al., 1985a, 1985b], which was originally designed with only four independent receivers, is currently being enhanced to 25 receivers. This exciting modification will provide significant CRI capabilities. As another example, researchers at the Indian MST radar facility [Rao et al., 1995; Jain et al., 1995] are designing independent receive arrays with the intent of implementing CRI. For a thorough review of the advantages of CRI, and other related techniques, the reader is referred to an article by Luce et al. . With these recent developments and previous research accomplishments, it is apparent that CRI is becoming an important tool for studies of the atmosphere.
 As mentioned earlier, the work reviewed has found application throughout all atmospheric layers. Typically, the radar systems used for this research were limited to several independent receivers. For the purpose of imaging the ABL, a 915 MHz imaging radar was developed by researchers at the University of Massachusetts-Amherst [Mead et al., 1998; Pollard et al., 2000], and was called the Turbulent Eddy Profiler (TEP). This system is capable of observing the ABL in a 25° cone above the surface using 61–91 independent receiving antennas, depending on the configuration. This unique design allows the use of sophisticated beamforming/imaging algorithms, which have numerous advantages.
 The present study details recent advances that are applicable to imaging radars for high-resolution measurements of the reflectivity and wind fields. Many of the results are based on numerical simulations of the TEP radar configuration. Although this specific system is simulated, the results are generally applicable. In section 2 an efficient algorithm is presented for spectral moment estimation using imaging radars. A new numerical simulation method recently developed by Cheong et al.  was used in order to properly and efficiently emulate the high angular resolution TEP system. These results will be provided in section 3 providing wind field estimates for a variety of reflectivity fields. Finally, conclusions are provided in the final section.
2. Pulse Pair Beamforming
 CRI, or beamforming, provides an estimate of the received signal from distinct angular positions within the transmit beam of the radar. This is accomplished by coherently combining signals arriving at different spatial locations in order to estimate the signal for a particular direction. Often, the signal is used to estimate the echo power but there is no restriction that only this parameter can be obtained. Given a radar array positioned on the ground, it is possible to image within a particular solid angle for each range. One can create an image by raster scanning through a desired x and y range. If echo power is calculated from the signal, the resulting map, or image, is proportional to the reflectivity within the beam of the radar. Using a similar notation to that of Palmer et al. , let x(t) represent a vector of received signals from n sensors. By combining these n signals with the complex coefficients in w, the output of the beamformer at time t will be given by complex scalar y(t) as
where the dagger represents the Hermitian operator (conjugate transpose). Typically, the elements of w are chosen to create constructive interference at a particular angle. The resulting signal could be used directly to calculate the Doppler spectrum. However, this computational burden is not needed if the three spectral moments would suffice.
 The autocovariance function of the output signal can be expressed as
where Rxx(τ) is the autocovariance matrix of the received signals in x(t).
Each element in Rxx(τ) represents the autocovariance of signals from a pair of receivers.
 A typical choice of w, which provides unity gain in the direction of the wavenumber vector k, is called the Fourier imaging method and the weight vector is given by
where k = [sin θ sin ϕ sin θ cos ϕ cos θ], with θ and ϕ as the zenith and azimuth angles, respectively. Di represents the position vector for the phase center of receiver i. By substituting wf into equation (1), we obtain the Fourier-based estimate of the output sequence.
 Using the concept behind the pulse pair processor [Doviak and Zrnić, 1993], the power, radial velocity and spectral width for direction k can be calculated using a temporal sampling of Ryy(τ) at τ = Ts. The parameters can be expressed as follows:
where S is the signal power. In practice, Rxx(0), Rxx(Ts) and S are replaced by their estimates. One could estimate the noise power from the “spike” of the autocorrelation function at lag-0 when no signal is present and subtract that from Ryy(0) to obtain the estimate of signal power S. The combined technique of pulse pair processing and beamforming is termed pulse pair beamforming (PPB). In essence, PPB exploits the linear relationship between the beamformer inputs and output to generate covariance lags of the output by using those that are computed for the inputs. The pulse pair relationship for the various spectral moments can be computed based on input correlations as opposed to the correlations of the outputs. This enhances our ability to image inside the beam of the radar. While computationally less efficient than conventional weight-and-sum beamforming, this formulation is advantageous in adaptive algorithms that require computation of the covariance matrix to determine the weights. Hence it provides an efficient method of estimating the spectral moments for imaging applications using adaptive algorithms. It should be noted that many of the concepts behind PPB can be related to the early work of Kudeki and Woodman  and Palmer et al. .
 With this obvious extension of the pulse pair processor to imaging applications, one can make use of the extensive literature on the statistical characteristics of the pulse pair processor, in general [see Doviak and Zrnić, 1993, and references therein]. It should be noted that the PPB algorithm described in the previous equations requires estimation of the covariance function. Standard estimation schemes, including incoherent integration, etc., can be employed for this purpose. Fourier imaging techniques are simple to implement and efficient algorithms such as FFT-based implementations can be used for various applications. However, it is well known that Fourier-based algorithms also suffer in the presence of clutter due to the fixed high sidelobes and have limited resolution. More sophisticated adaptive methods were developed in the late 1960s, producing higher resolution and the ability to null the interfering signals coming from ground clutter, for example. One such technique is known as Capon's method [Capon, 1969] but is also referred to as the Minimum Variance Method. Since the Fourier beamformer has a fixed beam pattern, which behaves similar to sin (x)/x, it inherently has fixed-gain sidelobes. Strong echoes can leak through sidelobes to the region of interest, possibly masking the desired signal. The Capon method attempts to minimize the output power of the beamformer with the constraint of maintaining unity gain in the desired direction. The minimization helps reduce leakage of high power signals through antenna pattern sidelobes. The optimization problem can be expressed mathematically as
where e = [ … ]T is the steering vector for the look direction resulting in wavenumber vector k.
 Intuitively, Capon's method only maintains unity gain in the beamformer direction defined by k. The algorithm has freedom in the choice of the gain for other directions. As a result, Capon's method may produce higher gain in directions where there is little backscatter energy. Of course, this higher gain has little adverse effect given that the backscattered energy is low.
 This constrained minimization problem can be solved using Lagrangian methods, resulting in the well-known solution for the weight vector
In general, it was found that higher resolution is achieved in generating the output power map using Capon's method compared to the Fourier method [Palmer et al., 1998]. It should be emphasized that the Capon weight vector was derived based on the idea of minimizing output power. No attempt was made to mitigate any effects on the estimated radial velocity. It will be shown later that the reflectivity field does have a significant effect on the imaged wind field map.
3. Simulation Results
3.1. Simulation Technique Overview
 The simulation model developed by Holdsworth and Reid  has proven to be invaluable for diverse studies of atmospheric radar applications [e.g., Yu, 2000]. However, the computational complexity of the required spatial filter becomes limiting for a large number of scatterers. This method was applied to a simulation of the TEP system at 915 MHz. Owing to the large number of receivers and the high resolving capacity of the TEP array, however, the limited number of scatterers proved to be ineffective in emulating volume scattering. Therefore the modified scheme proposed by Cheong et al.  is used for the current study. This method is similar to that of Holdsworth and Reid  but uses a table look-up method and linear interpolation. A set of pregenerated tables for a turbulent field are stored in a standardized manner that consists of velocity samples over a uniform three-dimensional grid within the enclosing volume. For each scatterer position, the turbulent velocity is extracted from the table and linearly interpolated among the eight surrounding points within a cubical region. As time evolves, the tabulated turbulent values are updated reflecting the time change behavior of the turbulent field.
 The tabulated values of the turbulent field can be generated in any number of ways. For example, the previous method of Holdsworth and Reid  could be used to generate the sequence of turbulent look-up tables. Since the turbulent fields are not updated at each instance in time and only linear interpolation is used, the computational efficiency gain is tremendous. Other physical-based methods of generating the turbulent fields could be used without increasing the complexity of the method. A interesting example was provided by Muschinski et al. , who used the resulting fields from a large eddy simulation to generated Doppler radar data.
3.2. Turbulent Eddy Profiler Configuration
 For this simulation, the TEP array is configured to have up to 61 sensors arranged in a hexagonal lattice. Each sensor is separated by approximately 0.5412 m, which is based on the actual TEP system. The range resolution is set to 30 m. A vertically directed transmit beam is used with a one-way, half-power beamwidth of 25°. Including coherent integration, the backscattered signal is sampled at a period of 0.007143 s. Figure 1 shows the simulated configuration of TEP array.
3.3. Consistency of Pulse Pair Beamforming
 Using the method of Cheong et al. , time series data were generated for the simulated TEP array. The general parameters of the simulation are provided in Table 1.
Table 1. List of Simulation Parameters
Transmitter pointing direction
Sampling time, Ts
Number of scatterers
Horizontal wind magnitude
Turbulent RMS velocity
 As a consistency check of the simulation method, Figure 2 provides several examples of Doppler spectra for five distinct pointing directions using both the Fourier and Capon beamformers. For this simple example, a symmetric, two-dimensional Gaussian reflectivity field with half-power width of 10° was used. The top panels provide the simulated radial velocity field within ±12.5° of zenith. For each pointing direction, the expected first moment of the Doppler spectrum will change. As we can see, the Doppler spectra are consistent with the radial velocity map. Since the wind is flowing at 25 ms−1 with 45° azimuth angle without vertical velocity (u = −17.67, v = −17.67 and w = 0 ms−1), one would expect negative radial velocity in the upper right region and positive radial velocity in the lower left region. Direction (1) is pointing vertically and shows the expected small radial velocity since the simulated vertical velocity is zero, in this case. The other four points also yield reasonable radial velocities and Doppler spectra. The actual values of radial velocity at each of these five points is indicated in the figure next to the panels for each of the five points. Note that the 0.3 ms−1 RMS turbulent velocities result in small but non-zero vertical radial velocities.
3.4. Simulated Experimental Setup
 An example reflectivity model used in the simulation is shown in Figure 3. It is composed of two elongated Gaussian blobs, each with the following form:
 The two scattering centers are located at (2°, 4°) and (−6°, −4°) with σx = 2°, σy = 4°, ρ = −0.75, and σx = 2°, σy = 4°, ρ = −0.5, respectively. For this simulation a northeasterly wind is used with an azimuth angle of 45° and mean velocity of 25 ms−1. Isotropic turbulence was introduced to the wind field model with an RMS value of 0.3 ms−1. A white noise sequence is added to each receiver signal to give an SNR of 3 dB for each sensor. The new simulation method allowed the use of 10,000 scattering points and the results are presented in the following section.
3.4.1. Moment Maps
 In this section, results using the new PPB method are provided. In Figure 4 the top panel shows echo power obtained by CRI using both Fourier and Capon based methods.
 The middle panel shows the corresponding radial velocity estimate using the new PPB method. The weight vectors used in equation (6) are both obtained from the Fourier and Capon procedures. As expected, the radial velocity contour lines derived from the PPB method are generally perpendicular to the wind direction. The bottom panel shows the spectral width estimate using equation (7). As stated previously, these maps were obtained using 10,000 scatterers in the volume. Note that radial velocity and spectral width maps are shown for regions with SNR > 3 dB.
 Given a wind magnitude of 25 ms−1, radial velocities of −6.45 ms−1 and +6.45 ms−1 should be observed at the edge of the circle (12.5°) at northeast and southwest, respectively. The estimates are shown in the middle panel of Figure 4 where visually accurate results are obtained. A more thorough statistical comparison will be provided when the radial velocity estimates are subsequently used to calculate the three-dimensional wind field.
 Spectral width estimates are shown in the bottom panel of Figure 4. The estimates have been normalized by 2va where va = 11.47 ms−1 for this simulated TEP configuration. Although a direct comparison to simulated values is difficult due to beam broadening effects, the spectral width estimates using the Fourier method show consistent results in regions of high reflectivity. Since the RMS value of the simulated turbulence is constant across the map, an approximately constant spectral width estimate should be expected. In contrast, the spectral width estimates from the Capon method are erratic and not comparable to the Fourier results. This is due to the adaptive nature the Capon algorithm which changes the shape of the beam pattern for each pointing direction. Of course, the adaptation is a result of the constrained minimization problem stated in equation (8). As will be seen in the next section, the adaptive nature of the Capon algorithm has a positive effect on the estimation of the reflectivity and velocity fields. However, the spectral width estimates are profoundly affected by the beam broadening effect which will change for each pointing direction using the Capon method. Therefore it is recommended to use the Fourier or other fixed beamforming methods for spectral width estimates.
3.4.2. Wind Field Maps
 Similar to the standard Doppler Beam Swinging (DBS) method, an estimate of the three-dimensional wind field map can be obtained by solving the following set of linear equations for each pixel in the map [e.g., Pollard et al., 2000].
where θi and ϕi are the azimuth and zenith angles for pixel i, respectively. For this study, a 3 × 3 sliding window is used providing nine equations for the estimate of the wind field. This sliding window may progress across the map in an overlapped or non-overlapped manner. Figure 5 illustrates the 3 × 3 sliding window for extracting 9 pixels used in computing the wind field for the middle pixel. As in the standard DBS method, it is assumed that the wind field is constant across the scanned area, which is reasonable given the limited area covered by the nine beams.
 The well known minimum norm least squares solution for equation (11) is given by
 Results obtained using equation (12) for estimates of the three-dimensional wind field are shown in Figure 6. These results are generated for a situation in which there is a constant horizontal wind of 25 ms−1, no vertical velocity, and a turbulent RMS velocity of ±1 ms−1 is added to the mean velocity. The corresponding wind field maps are obtained by computing the least square solutions for the nine linear equations in the 3 × 3 sliding window. A window distance of 3 pixels (from one middle pixel to the middle pixel in the adjacent 3 × 3 window) is used in this map. In a general sense, the estimates do give a reasonable indication of the horizontal winds. The overall direction and approximate magnitudes are similar to the underlying known wind field. The actual horizontal wind vector is provided in the upper-right corner, for reference. Visually, the wind field estimates using the Fourier method seem to display a larger error than the Capon results. The RMS error for the Capon results (5.427 ms−1) appears to be significantly lower than that of the Fourier results (8.131 ms−1) at an SNR of 3 dB. A set of experiments were run under the same conditions over a range of SNRs. These results are illustrated in Figure 7. Note the consistently lower RMS errors in the velocity estimates for the Capon technique. As SNR increases, the Fourier error does not change significantly, indicating that the source of the error is not predominantly noise.
 In Figure 8 the effect of angular variations in the underlying reflectivity pattern along the horizontal wind direction on the estimated radial velocity is illustrated. Assuming that the desired pointing direction is given by θo, the observed signal extends over the range in which the receive beam pattern magnitude is significant. An ideal delta function beam pattern would sample the received signal from only the direction θo and yield a good estimate of the radial velocity in that direction. A finite width beam will observe radial velocities over a range of angles. The variation of reflectivity along the direction of the horizontal wind will result in uneven weighting of velocities that are too low on one side of θo and too high on the other side of θo. The shaded regions in the figure illustrate the extent to which the reflectivity variation contributes to a systematic bias in radial velocities.
 We can investigate the effects of reflectivity changes along the direction of the horizontal wind using Fourier beamforming. Following a development similar to that used in May et al.  for thin scattering layers, the biased estimated radial velocity can be written as
where T(θ, ϕ) is the transmit beam magnitude, R(ro, θ, ϕ) is the true atmospheric reflectivity magnitude at range ro, F(θ, ϕ) is the Fourier based receive beam magnitude, H is the true horizontal wind velocity, and (θ, ϕ) is the unit direction vector toward direction (θ, ϕ). The integration is taken over the small range of angles in which the receive beam is significant (i.e., the mainlobe region). The estimate r,bias can be used to generate an approximation to the error radial velocity estimate observed with the Fourier based simulation. These estimates are, to a first order approximation, equivalent to the errors observed in several different cases.
 Given the rather controlled nature of the conditions used in the experiment (constant, known horizontal velocity with weak turbulence), it is interesting to look at the horizontal wind estimates superimposed over the estimated reflectivity. Figure 9 presents these horizontal wind field estimates over the reflectivity estimates for both the Fourier and Capon based estimators. An interesting feature is observed near the valley between the two reflectivity peaks. Note the systematic over and under estimation compared to the known actual horizontal velocity indicated by the single arrow in the upper right corner of each frame. Variations in the reflectivity pattern along the direction of the wind are accompanied by either systematic increases, decreases, or rotations in horizontal wind vector estimates. It appears that the variation is more significant in the case of the Fourier estimators than it is for the Capon estimators. Such errors have been known from some time in standard Doppler measurements [May et al., 1988]. Through the use adaptive array processing (Capon), however, it is now possible to mitigate these adverse effects for imaging applications.
3.5. Quantitative Wind Field Results for Reflectivity Variations
 The reflectivity pattern used in Figure 3 suggests the impact on the wind field estimates produced by reflectivity patterns. To investigate this possibility, another set of experiments with six different reflectivity fields were tested to assess the statistical performance of different reflectivity patterns. Figure 10 shows the six different reflectivity patterns that were used in this experiment. A uniform horizontal wind of 25 ms−1 with 45° azimuth angle was used for all six patterns. Turbulent field of 0.3 ms−1 RMS velocity was added. Figure 11 shows the wind field estimates superimposed on the power distribution maps obtained from Fourier and Capon PPB methods. Note the poorer wind estimates from the Fourier PPB method especially around the regions with significant reflectivity variations. The images obtained from Capon PPB method do not show such poor results over much of the field. By varying the SNR from 0 to 15 dB, a statistical test was conducted for these six patterns. Figure 12 shows the RMS error of the wind field estimates for these six patterns as SNR is varied. Results from the Fourier PPB method do not improve with SNR but results from the Capon PPB method are initially better and continue to improve with increasing SNR. This motivates the use of Capon PPB method for imaging applications that require wind field maps as well as simply reflectivity maps.
 The primary contributions of this paper include a combination of pulse pair processing and beamforming techniques referred to as pulse pair beamforming (PPB) for estimating velocity and spectral width using beamforming techniques and a statistical investigation into the applicability of Capon and Fourier PPB techniques for high-resolution estimation of the wind and reflectivity field maps. The concept of pulse pair processing has been extended to beamformed imaging systems by using reflectivity derived weight vectors to estimate the pulse pair parameters necessary for both velocity and spectral width estimates. This PPB approach has been applied with both Fourier and Capon techniques. The validity of the PPB technique has been demonstrated by comparison to standard Doppler spectral techniques.
 While the Capon PPB technique has been shown to be superior in estimating velocities using simulated data, the varying nature of the adaptive beamformer beam pattern results in poor performance for spectral width applications. The fixed pattern Fourier technique appeared to be superior for the spectral width application. In addition, Capon PPB tends to consistently outperform Fourier PPB in statistical tests for three-dimensional wind field maps. A significant source of the errors that are mitigated by Capon PPB are reflectivity field variation induced errors in the wind field maps. These are visually apparent when the Fourier wind field maps are superimposed on the reflectivity maps. In addition, the constancy of the Fourier errors with increasing SNR are consistent with a signal induced (as opposed to noise induced) effect. Similar effects have been observed previously for the case of standard Doppler wind measurements [May et al., 1988].
 As pointed out earlier, existing MST radar systems and newly developed systems are beginning to routinely use CRI as a means of high-resolution studies of the atmosphere [Luce et al., 2001]. Even commercial systems are available with multiple receiver capabilities allowing CRI implementation. Given this interest in imaging technologies, statistical studies using realistic numerical simulations are becoming important. In fact, it is now apparent that the future of MST radar studies of the atmosphere will include developments in imaging techniques.
 B.L.C., R.D.P., and M.W.H. were supported by the Army Research Office through grant DDAD19-01-1-0407. S.J.F. and F.J.L.-D. were supported by the Army Research Office (Atmospheric Sciences) through grant DAAG55-98-1-0480.