## 1. Introduction

Knowledge regarding the three-dimensional variability of precipitation is essential in the development of precipitation retrieval algorithms from satellite radiometer observations. This is because satellite radiometer observations cannot be uniquely associated with precipitation, and statistical information is required to determine optimal precipitation estimates. Spaceborne radar observations may be used to derive such information. For example, it is anticipated that in the Global Precipitation Measurement (GPM) era, observations from spaceborne dual-frequency radar will be used to develop algorithms capable of providing consistent precipitation estimates from satellite radiometers featuring various channel frequencies and footprint resolutions (Hou et al. 2008). Consistency among precipitation retrievals from these various radiometers will be achieved through the development of common precipitation–radiance databases derived from combined radar–radiometer precipitation profile estimates (Hou et al. 2008). From this perspective, spaceborne radar profiling algorithms are crucial for the derivation of global satellite precipitation estimates.

Various algorithms for retrieving precipitation from dual-frequency radar observations have been developed. These include, but are not limited to, methods by Meneghini et al. (1992), Mardiana et al. (2004), Grecu and Anagnostou (2004), Liao et al. (2005), and Rose and Chandrasekar (2006). In addition, methodologies for incorporating Ku-band radar observations in combined radar–radiometer retrieval frameworks have been formulated, for example, in Haddad et al. (1997), Grecu et al. (2004), and Masunaga and Kummerow (2005). However, further research must be conducted to develop dual-frequency retrieval algorithms that would perform optimally within the GPM context. The GPM core satellite will feature a Ku-/Ka-band dual-frequency precipitation radar (DPR) (Senbokuya et al. 2004). The dual-frequency radar observations will be available within a 125-km-wide swath, centered within a 245-km-wide swath of single-frequency Ku-band radar observations. From the science perspective, it is desirable to develop a physically consistent radar profiling algorithm that can operate using either single-frequency (Ku band only) or dual-frequency (Ku/Ka band) observations, and one that can make use of path-integrated attenuation (PIA) estimates from the radar surface reference technique (SRT) (Meneghini et al. 2000, 2004) when deemed reliable.

In this study, we formulate a GPM DPR profiling algorithm that can be applied to both the inner and outer swaths and can optimally incorporate SRT information into the retrievals. The algorithm is based on a *generalized* Hitschfeld and Bordan (1954) attenuation correction methodology that yields generic Ku-band radar precipitation profile estimates and an optimization procedure that adjusts the Ku-band estimates to be physically consistent with coincident Ka-band observations and Ku-/Ka-band SRT PIA estimates. The algorithm is computationally efficient and can be used within a combined radar–radiometer framework.

## 2. Method

### a. Overview

The dual-frequency profiling algorithm formulated in this study is based on a computationally efficient methodology to derive generic precipitation profiles from single-frequency Ku-band radar observations. Specifically, assuming that the hydrometeor particle size distributions follow a gamma function (Ulbrich 1983)—that is, *D* is the particle diameter and *N*_{0}, Λ, and *μ* are the intercept, slope, and shape parameters, respectively—and that *N*_{0} and *μ* along with the cloud water and water vapor attenuation are known for every gate, a Ku-band reflectivity profile is inverted to derive profiles of Λ. Various studies (e.g., Testud et al. 2001; Illingworth and Blackman 2002) showed that normalized gamma distributions are preferable to standard gamma distributions in some instances. However, because the number concentration still depends on the shape factor irrespective of whether a normalization is used (Liao et al. 2005), a standard gamma distribution is used in this study. To perform the dual-wavelength inversion, the Λ profiles are optimized as a function of adjustable *N*_{0} profiles to minimize, in a least squares sense, the differences between Ka-band predicted and actual reflectivity observations, as well as the differences between predicted and SRT-derived Ku- and Ka-band PIAs. Additional constraint (background) terms are included in the function to be minimized to prevent the derivation of unrealistic *N*_{0} values.

### b. Single-frequency retrieval

*k*is the specific attenuation,

*Z*is the reflectivity factor, and

*α*and

*β*are known parameters. In addition to the power-law dependence,

*β*has to be constant with range for the HB methodology to apply. A generalization of the HB method can be derived from the radar equation,

*r*is the radar range;

*Z*(

_{m}*r*) and

*Z*(

*r*) are the measured and unattenuated reflectivity factors, respectively; and

*k*[

*Z*(

*s*)] (dB km

^{−1}) is the specific attenuation as a function of

*Z*(

*s*). By raising (2) to power of

*β*and then multiplying the result by

*k*[

*Z*(

*r*)], the following equation can be derived:

*r*yields

*q*≡ 0.2

*β*ln10. From (6), (7), and (2), it follows that the unattenuated reflectivity is related to the measured reflectivity by

Equation (8), together with (6), is a generalization of the attenuation correction formula derived by HB. It is apparent from (6) and (8) that *k* does not have to satisfy (1) for the attenuation correction procedure to work. However, parameter *β* has to be constant in range and for numerical convergence considerations is chosen to minimize the variance of *k*/*Z ^{β}*. However, if (1) holds, then the unattenuated reflectivity values do not need to be known to derive the PIA using (7) and (8). If (1) does not hold, an iterative solution is generally required. Shown in Fig. 1 is a flowchart describing an iterative attenuation correction procedure based on (6) and (8). The procedure starts by reading the observed reflectivity factors

**Z**

*. Because (6) accounts only for attenuation due to solid, liquid, and mixed-phase precipitation, the measured reflectivity factors first need to be corrected for attenuation due to cloud and water vapor. This is done using parameterizations derived from cloud-resolving model simulations, as in Iguchi et al. (2009). Then, the initial estimates of the unattenuated reflectivity factors*

_{m}**Z**are set to

**Z**

*. Because (8) does not have a closed form (i.e.,*

_{m}**Z**occurs on both sides of the equation), iterative improvement of the approximations of

**Z**on the right-hand side of (8) is required.

The next step consists of calculating *S*(*r*) for *r* varying from 0 (radar altitude) to *r _{s}* (range to the surface). When the quantity

*qS*(

*r*) is greater than or equal to 1, (8) cannot be applied. Iguchi and Meneghini (1994) proposed the adjustment of

_{s}*qS*(

*r*) by a factor

_{s}*ε*, while Durden and Haddad (1998) and Ferreira et al. (2001) showed the importance of relating this type of adjustment to changes in the assumptions regarding the particle size distributions. Indeed, if the intercepts in the particle size distributions at all levels are changed by

*δN*, then

*qS*(

*r*) (where

_{s}*r*is the range to the surface) changes

_{s}*δN*

^{(1−β)}, which implies that

*δN*

^{(1−β)}=

*ε*. A simple procedure is implemented to keep the quantity

*qS*(

*r*) below a maximum value

_{s}*ζ*

_{max}(slightly less than 1) that corresponds to a maximum retrievable PIA value of −10/

*β*log

_{10}(1 −

*qζ*

_{max}). That is, if

*qS*(

*r*) becomes greater than

_{s}*ζ*

_{max}, it is set to

*ζ*

_{max}and all particle size distribution (PSD) intercepts are changed by a factor of

The iterative procedure is continued until the root-mean-square difference between the updated and previous reflectivity factors does not change by more than 5 × 10^{−2} dB. Convergence is generally faster than that of the correction procedure of Meneghini (1978). This is because *k*(*Z*)/*Z ^{β}* is a weak function of

*Z*(which may be a constant for certain ranges and drop size distributions, as assumed by HB). Moreover, (7) and (8) provide an effective and physically consistent mechanism of avoiding divergence in the attenuation correction process.

### c. Lookup tables and forward model

To efficiently make use of the generality of formulas (6) and (8), lookup tables of attenuation and associated reflectivity, equivalent precipitation water content, and precipitation rate normalized by *N*_{0} are derived as a function of Λ for constant *μ* at both Ku and Ka bands. Since these bulk radiative properties are normalized by *N*_{0}, properties for different values of *N*_{0} can be easily derived through simple calculations done on the fly. For example, if the attenuation for a given Ku-band reflectivity is desired, a quick search can be used to locate the two consecutive *Z/N*_{0} entries in the lookup table that bound the actual *Z/N*_{0}. The associated Ku-band *k/N*_{0} value is determined through linear interpolation between the corresponding two consecutive *k/N*_{0} values in the lookup table. Finally, *k* is determined by multiplying the interpolated *k/N*_{0} by the actual *N*_{0} value. A bisection method (Press et al. 2007) is used to quickly find the desired entries in the lookup tables.

Five values of *μ* are considered, that is, *μ* ∈ {−2, −1, 0, 1, 2}. The values of Λ are chosen such that the mass-weighted mean diameter, defined as the ratio of the fourth moment of the gamma distribution to the third moment, varies from 0.1 to 5.0 mm with a step of 0.1 mm. That is, given a value of *μ* in the above set and a value of mean diameter, Λ is analytically determined and the normalized reflectivity and attenuation are determined by numerical integration. Multiple hydrometeor phases are considered as well. For stratiform rain exhibiting a clear bright band, the five-node storm structure of Iguchi et al. (2009) is used. That is, the bright band (if it exists) is first identified and used to define the geometry of the melting layer. Then, depending on the altitude of a given range gate relative to the melting layer boundaries, specific lookup tables are used for attenuation correction and PSD estimation. Within the melting layer itself, a brightband model similar to the first model of Bauer et al. (2000) is used to derive the attenuation and reflectivity. That is, snow is assumed to have a constant density at the top of the melting layer and the precipitation flux is assumed to be constant within the melting layer. The first model of Bauer et al. (2000) is integrated downward to derive the amount of melted mass as a function of the distance below the 0.0°C isotherm. The electromagnetic properties of melting snow are calculated using the model proposed by Klaassen (1988). The attenuation, reflectivity, and associated precipitation table for the brightband peak (node C) is constructed by matching the peak reflectivity in the computational melting layer model. A snow lookup table is used at the top of the melting layer (node B). Snow particles are modeled as a spherical mixture of air and ice in this study. The Maxwell-Garnett formula (Maxwell-Garnett 1904) is used to determine the snow refractive index. A water lookup table is used at the bottom of the melting layer (node D). Nodes B and D are set at 500 m above and below the brightband peak. Tables for the top and bottom nodes (A and E) are derived using snow and water properties at temperatures estimated as a function of the distance from the bright band, assuming a 6 K km^{−1} lapse rate. The attenuation versus reflectivity relationships in between these nodes are determined through linear interpolation. It should be mentioned that the lapse rate can also be determined using meteorological analyses. Moreover, nodes B and D might be more accurately determined based on the reflectivity derivative with range. A similar methodology, but based only on four nodes, is used in stratiform rain not exhibiting a bright band and in convective rain. That is, node C is eliminated and the attenuation versus reflectivity relationships within the transition are determined by interpolating between the node B and node D tables.

The lookup tables and multiple-node structures are used not only in the generalized HB retrievals, but also in simulating the measured reflectivity factors at Ka-band. Note that given the Ku-band normalized reflectivity value *Z/N*_{0} and the lookup tables for both Ku- and Ka-band normalized reflectivity and attenuation, the associated Ka reflectivity and attenuation can be readily determined. The Ka-band measured reflectivity factors are simulated using (2). Attenuation due to cloud and water vapor is parameterized as described in Iguchi et al. (2009). The benefit of simulating measured Ka-band reflectivity from Ku-band precipitation profile estimates is that an objective procedure to optimally derive the *N*_{0} values that make the Ku-band estimates most consistent with Ka-band observations can be derived. Such a procedure is described in the next subsection.

### d. Optimal estimation framework

**Z**

_{m}_{,Ka}is the actual Ka-band measured reflectivity vector (dB

*Z*),

**Z**

_{sim,Ka}(

**N**

_{0}) is the Ka-band reflectivity vector simulated from Ku-band retrievals, and

*N*

_{0}(i.e., estimates that are unique and insensitive to small perturbations in the measurements), based on the agreement between simulated and actual measured Ka-band reflectivity factors. A more complete formulation that accounts for the agreement between simulated and SRT-derived PIAs and between estimated

**N**

_{0}and a priori

**N**

_{0}estimates is

**PIA**

_{SRT}is the two-component vector of SRT estimates of Ku- and Ka-band PIA,

**PIA**

_{sim}(

**N**

_{0}) is the vector of Ku- and Ka-band PIA simulated from the Ku retrievals,

**N**

_{0}), and

Function *F* does not depend exclusively on **N**_{0} but on other parameters as well (e.g., the shape factors, cloud water, and relative humidity). However, given that these parameters cannot be reliably retrieved along with **N**_{0} from dual-frequency radar observations, they are specified rather than retrieved. Some information regarding the relative humidity and cloud water distribution can be derived from coincident microwave radiometer observations if available, but this study’s focus is exclusively dual-frequency spaceborne radar retrievals. Combined radar–radiometer retrievals will be investigated in a future study, and so only the *sensitivity* of precipitation estimates to parameters that cannot be retrieved from radar observations alone will be considered here.

*F*in (10) is minimized as a function of ln(

**N**

_{0}) using the Gauss–Newton method (Rodgers 2000). Addressing the minimization problem as a function of ln(

**N**

_{0}), rather than

**N**

_{0}, is advantageous because it requires the linearization of only the first two terms on the right-hand side of (10). The flowchart of the minimization procedure is shown in Fig. 2. The Gauss–Newton method requires the Jacobian of the forward model operator, that is, the operator that, given the vector

**N**

_{0}, produces the simulated observations

**Z**

_{sim},

_{Ka}(

**N**

_{0}) and

**PIA**

_{sim}(

**N**

_{0}). In this study, the derivatives of the forward model operator’s Jacobian, called

**N**

_{0}is varied independently of the other components, and the simulated observations are recalculated and then differenced with respect to the unperturbed simulated observations. The cost of calculating the Jacobian in this way is an order of magnitude higher than calculating the gradient of

*F*through a reverse evaluation technique (Wunsch 2006). However, because the Gauss–Newton method is a second-order method, the minimization process requires a significantly smaller number of iterations than steepest descent techniques based on reverse gradient evaluations, which makes the Gauss–Newton method similar in terms of computational effort to the reverse-gradient-based techniques. The vector

**N**

_{0}is updated using the following formula:

**dY**is the difference between the observations and simulations. Another advantage of the Gauss–Newton method is that

**N**

_{0}) estimates.

Flowchart of the optimal estimation procedure.

Citation: Journal of Applied Meteorology and Climatology 50, 7; 10.1175/2011JAMC2655.1

Flowchart of the optimal estimation procedure.

Citation: Journal of Applied Meteorology and Climatology 50, 7; 10.1175/2011JAMC2655.1

Flowchart of the optimal estimation procedure.

Citation: Journal of Applied Meteorology and Climatology 50, 7; 10.1175/2011JAMC2655.1

The whole process of deriving **Λ** as a function of **N**_{0} from the Ku-band observations, simulating the Ka-band measurements and the PIA vector, and updating the **N**_{0} vector is illustrated in Fig. 2. For the purposes of computational efficiency as well as numerical robustness, it is preferable to retrieve a reduced-order representation of **N**_{0} rather than *N*_{0} at every single radar gate where dual-frequency observations are available; see Hogan (2007). That is, *N*_{0} is retrieved every 500 m, and the intermediate values are determined by spline interpolation of log(*N*_{0}). Although the resulting **N**_{0} is smoother than it would be if it were explicitly retrieved for every gate, the associated estimates of **Λ** and other variables are not necessarily smooth because independent Λ retrievals are carried out for every radar gate using the generalized HB method. It is worth mentioning that Rose and Chandrasekar (2006) also used a parameterized representation of log(*N*_{0}): they assumed that for liquid rain, log(*N*_{0}) varies linearly with height. However, unlike in the current approach, the mass-weighted mean diameter was also parameterized. In subsequent sections, the least squares–based algorithm described in this section will be referred to as LSA.

## 3. Application to synthetic data

To assess the LSA’s ability to yield a well-defined solution, a synthetic data experiment is devised. That is, the algorithm is applied to simulated dual-frequency Ku-/Ka-band observations, and the results are evaluated against the PSD variables used to simulate the observations. Actual Ku-band airborne radar observations collected in the TC4 experiment (Toon et al. 2010) are used to derive vertical profiles of slope profiles (Λ) as a function of randomly generated *N*_{0} profiles. Uncorrelated, lognormally distributed *N*_{0} values with a mean of log(0.08 cm^{−4}) and a standard deviation of 1.0 are generated every 500 m starting from the Ku-band echo top down to surface. The intermediate *N*_{0} values are computed by spline interpolation, as explained in previous section. The shape factor *μ* is assumed constant in the vertical and equal to 0.0. Given the randomly generated *N*_{0} profiles, fixed *μ*, and Ku-band reflectivity profile, a synthesized Λ profile is derived using the generalized HB method. The cloud water and relative humidity profiles are assumed known and set based on the WRF simulations. These profiles are assumed to be representative of tropical precipitation. Finally, Ka-band reflectivities, as well as Ku- and Ka-band PIAs, are then synthesized from the known atmospheric profile and the forward model. Although the vertical distributions of cloud and relative humidity may have a significant impact on both Ku- and Ka-band retrievals, only the mechanics of the algorithm and not the impact of uncertainties in forward models are tested in this section.

Shown in Fig. 3 are the synthetic Ku-band and Ka-band reflectivity observations. Single-frequency (Ku only; left-hand panel) and dual-frequency (Ku/Ka; right-hand panel) estimates of precipitation water content are plotted versus the “true” precipitation water contents in Fig. 4. Data points from all levels are shown in the figure. It is apparent from Fig. 4 that the dual-frequency, Ku-/Ka-band estimates are superior to single-frequency, Ku-band estimates, and that the LSA estimates are reasonably accurate. In applications to actual radar data, the vertical distributions of *μ*, cloud water, and relative humidity are not known, and any reasonable assumption may have a notable impact on retrievals. The electromagnetic properties of the melting layer represent a source of significant uncertainty as well. Therefore, the results described in this section should be regarded only as an evaluation of the LSA’s ability to provide a correct solution to the numerical problem associated with the retrieval process.

Synthetic Ku- and Ka-band reflectivity observations.

Citation: Journal of Applied Meteorology and Climatology 50, 7; 10.1175/2011JAMC2655.1

Synthetic Ku- and Ka-band reflectivity observations.

Citation: Journal of Applied Meteorology and Climatology 50, 7; 10.1175/2011JAMC2655.1

Synthetic Ku- and Ka-band reflectivity observations.

Citation: Journal of Applied Meteorology and Climatology 50, 7; 10.1175/2011JAMC2655.1

True vs estimated equivalent precipitation water content derived from (left) single (Ku band) and (right) dual-frequency synthetic (Ku/Ka band) observations.

Citation: Journal of Applied Meteorology and Climatology 50, 7; 10.1175/2011JAMC2655.1

True vs estimated equivalent precipitation water content derived from (left) single (Ku band) and (right) dual-frequency synthetic (Ku/Ka band) observations.

Citation: Journal of Applied Meteorology and Climatology 50, 7; 10.1175/2011JAMC2655.1

True vs estimated equivalent precipitation water content derived from (left) single (Ku band) and (right) dual-frequency synthetic (Ku/Ka band) observations.

Citation: Journal of Applied Meteorology and Climatology 50, 7; 10.1175/2011JAMC2655.1

Shown in Fig. 5 are single-frequency (Ku band; left-hand panel) and dual-frequency (Ku/Ka band; right-hand panel) retrievals of mass-weighted mean diameters from the semisynthetic observations. Similar to the results in Fig. 4, the dual-frequency retrievals are superior to single-frequency retrievals. However, as previously explained, additional uncertainties are expected to arise in real-life applications.

True vs estimated equivalent mass-weighted mean diameters derived from (left) single (Ku band) and (right) dual-frequency synthetic (Ku/Ka band) observations.

Citation: Journal of Applied Meteorology and Climatology 50, 7; 10.1175/2011JAMC2655.1

True vs estimated equivalent mass-weighted mean diameters derived from (left) single (Ku band) and (right) dual-frequency synthetic (Ku/Ka band) observations.

Citation: Journal of Applied Meteorology and Climatology 50, 7; 10.1175/2011JAMC2655.1

True vs estimated equivalent mass-weighted mean diameters derived from (left) single (Ku band) and (right) dual-frequency synthetic (Ku/Ka band) observations.

Citation: Journal of Applied Meteorology and Climatology 50, 7; 10.1175/2011JAMC2655.1

## 4. Application to airborne data

In this section, the dual-frequency algorithm is applied to actual radar observations collected by the Airborne Second Generation Precipitation Radar (APR-2) during the TC4 experiment. TC4 was based in Costa Rica and Panama during July and August 2007. Its major objective was to better understand the role that the tropical tropospheric layer (TTL) plays in the earth’s climate and atmospheric chemistry (Toon et al. 2010). APR-2 provides collocated beam reflectivity observations at 13.4 and 35.6 GHz in a downward-looking, cross-track-scanning geometry (Sadowy et al. 2003). Given its similarity to the future GPM DPR, APR-2 data represent an excellent opportunity to test DPR algorithms. The real Ku-/Ka-band data used in this section were collected during a flight leg that occurred from 1936 to 1944 UTC 17 July 2007. During this flight leg, the APR-2 sampled both convective (apparent near scan index 40 in Fig. 6) and stratiform precipitation. The dual-frequency retrievals are expected to be more accurate in stratiform precipitation, since the vertical distribution of precipitation phases are better defined in stratiform regions. However, the algorithm developed here is applicable to both convective and stratiform precipitation.

Ku- and Ka-band reflectivity observations from the APR-2 at the TC4 field experiment on 17 Jul 2007.

Citation: Journal of Applied Meteorology and Climatology 50, 7; 10.1175/2011JAMC2655.1

Ku- and Ka-band reflectivity observations from the APR-2 at the TC4 field experiment on 17 Jul 2007.

Citation: Journal of Applied Meteorology and Climatology 50, 7; 10.1175/2011JAMC2655.1

Ku- and Ka-band reflectivity observations from the APR-2 at the TC4 field experiment on 17 Jul 2007.

Citation: Journal of Applied Meteorology and Climatology 50, 7; 10.1175/2011JAMC2655.1

Shown in Fig. 7 are the equivalent mass-weighted mean diameter (top panel) and the equivalent precipitation water content (middle panel) derived by the application of the LSA to the observations shown in Fig. 6. The shape factor *μ* is assumed to be 0.0 in this algorithm application. Generic relative humidity and cloud profiles derived from WRF simulations are assumed, as explained in the previous section. A snow density of 0.1 g cm^{−3} is also assumed. The impact of these assumptions on the retrieved precipitation will be investigated later in this section.

(top) Equivalent mass-weighted mean diameters, (middle) equivalent precipitation water contents, and (bottom) PIAs estimated from the APR-2 data between 1936 and 1944 UTC 17 Jul 2007.

Citation: Journal of Applied Meteorology and Climatology 50, 7; 10.1175/2011JAMC2655.1

(top) Equivalent mass-weighted mean diameters, (middle) equivalent precipitation water contents, and (bottom) PIAs estimated from the APR-2 data between 1936 and 1944 UTC 17 Jul 2007.

Citation: Journal of Applied Meteorology and Climatology 50, 7; 10.1175/2011JAMC2655.1

(top) Equivalent mass-weighted mean diameters, (middle) equivalent precipitation water contents, and (bottom) PIAs estimated from the APR-2 data between 1936 and 1944 UTC 17 Jul 2007.

Citation: Journal of Applied Meteorology and Climatology 50, 7; 10.1175/2011JAMC2655.1

Although some artifacts are apparent, the precipitation estimates appear to be realistic. The reason why the mass-weighted mean diameter tends to be larger in the melting layer than in the immediate neighboring layers is most likely an underestimation of the dual-frequency reflectivity ratio (DFR) in the melting layer due to the relatively simple model of electromagnetic properties of melting ice particles. It should be noted here that not only the model of Klaassen (1988) is deficient in this respect. Several other simple models of similar design (i.e., based on the assumption that melting particles are spherical mixtures of air, ice, and liquid water) have been explored and did not produce better results. Although the more complex approach of Liao and Meneghini (2005) is likely to yield a more continuous transition from the ice to the liquid water phase, tables of electromagnetic scattering properties (e.g., extinction, scattering, phase function) at all GPM frequencies are not yet available. However, such tables will be become available in the near future (L. Liao and R. Meneghini 2010, personal communications), and they will be incorporated into the LSA. Until then, the electromagnetic model of Klaassen (1988) will be used. The consequence of DFR underestimation in the bright band is the underestimation of *N*_{0} in the bright band. Therefore, the Ku-band reflectivity in the bright band is interpreted as being caused by unrealistically few but relatively large particles, leading to an underestimation of precipitation water contents in the bright band.

Shown in the bottom panel of Fig. 7 are the Ka-band SRT PIA and the algorithm-estimated PIA. There is good agreement between the two variables, which indicates that the precipitation estimates are consistent with Ka-band reflectivity observations as well as the SRT PIA at Ka band. The agreement is good even in the convective region, which is characterized by very large Ka-band PIA—an illustration of the algorithm’s ability to make use of all existing information. That is to say, even though the Ka-band reflectivity signal can become completely attenuated (see Fig. 6), the SRT PIA estimate may still provide useful information to the algorithm. Note that formulations that make explicit use of the dual-frequency reflectivity ratio cannot use this type of information in the retrieval process. The Ku-band SRT and retrieved PIAs exhibit similar agreement (not shown).

The retrieved number density *N _{T}*, defined as the total number of precipitation particles per volume unit, is shown in Fig. 8. A trend of increasing

*N*with the distance below the cloud top is apparent above 5-km altitude. Lo and Passarelli (1982) noted a similar trend in airborne data and attributed it to depositional growth of ice nuclei. In the freezing regions close to the 0°C isotherm, a decrease of

_{T}*N*with the distance from cloud top is expected because of aggregation processes. Uncertainties in modeling the electromagnetic scattering properties and size distributions of ice-phase precipitation are likely to significantly affect the

_{T}*N*retrieval in the ice phase. Although progress in modeling the scattering properties using advanced electromagnetic solvers and complex particle shapes (Liu 2008) and better parameterizations of snow distributions (Tian et al. 2010) are likely to reduce uncertainties in the ice-phase estimates of

_{T}*N*, it is expected that ice-phase retrievals will continue to be more uncertain than liquid-phase retrievals simply because of the additional degrees of freedom involved in the characterization of frozen hydrometeors versus raindrops. Similarly,

_{T}*N*estimates in the melting layer are likely to have significant uncertainties due to uncertainties in both electromagnetic properties and particle size distribution parameterizations. Estimates of

_{T}*N*near the ground in clutter-free regions are expected to be most accurate when the SRT estimates of PIA are accurate. This is because, irrespective of forward modeling uncertainties, the algorithm derives a solution that is consistent with Ku- and Ka-band reflectivity observations as well as the associated SRT PIAs. Therefore if the SRT PIAs are reasonably accurate, then precipitation estimates from LSA will be similar to those of Meneghini et al. (1992), which are deemed most accurate near the ground. In sum, the LSA does not require SRT estimates of PIAs, but it does make effective use of them if they are available and accurate.

_{T}Estimated *N _{T}* values from the APR-2 between 1936 and 1944 UTC 17 Jul 2007.

Citation: Journal of Applied Meteorology and Climatology 50, 7; 10.1175/2011JAMC2655.1

Estimated *N _{T}* values from the APR-2 between 1936 and 1944 UTC 17 Jul 2007.

Citation: Journal of Applied Meteorology and Climatology 50, 7; 10.1175/2011JAMC2655.1

Estimated *N _{T}* values from the APR-2 between 1936 and 1944 UTC 17 Jul 2007.

Citation: Journal of Applied Meteorology and Climatology 50, 7; 10.1175/2011JAMC2655.1

To investigate the impact of the SRT PIA estimates, retrievals without the use of these estimates are performed. This is done by setting the elements of

(top) Differences of precipitation water contents estimated using LSA with and without SRT information and (bottom) differences estimated using LSA with dual-frequency (Ku/Ka band) and single-frequency (Ku band) data.

Citation: Journal of Applied Meteorology and Climatology 50, 7; 10.1175/2011JAMC2655.1

(top) Differences of precipitation water contents estimated using LSA with and without SRT information and (bottom) differences estimated using LSA with dual-frequency (Ku/Ka band) and single-frequency (Ku band) data.

Citation: Journal of Applied Meteorology and Climatology 50, 7; 10.1175/2011JAMC2655.1

(top) Differences of precipitation water contents estimated using LSA with and without SRT information and (bottom) differences estimated using LSA with dual-frequency (Ku/Ka band) and single-frequency (Ku band) data.

Citation: Journal of Applied Meteorology and Climatology 50, 7; 10.1175/2011JAMC2655.1

The differences between the SRT-based LSA estimates and single-frequency (Ku only) estimates are shown in the bottom panel of Fig. 9. The differences between the two retrievals are significant both above and below the freezing level. Nevertheless, it is still possible to make the single-frequency radar precipitation estimates more consistent with dual-frequency radar estimates. In the LSA applications shown in Fig. 9, the a priori **N**_{0} estimates derived from the dual-frequency observations. However, in satellite applications, more representative estimates of

To evaluate the sensitivity of precipitation estimates to parameters that cannot be reliably estimated from radar observations alone, retrievals under various assumptions are performed. Shown in the top panel of Fig. 10 is the difference between the LSA retrieval for *μ* = 0 and the LSA retrieval for *μ* = 1. As illustrated by Fig. 10, the PSD shape factor has a significant impact on precipitation water content estimates; the estimates for *μ* = 0 being approximately 15% larger than those for *μ* = 1. Cloud and relative humidity uncertainties may also result in uncertainties up to 10% in estimated water contents (results not shown). It is anticipated that these uncertainties can be reduced by incorporating LSA into a combined radar–radiometer framework, but the performance of such an algorithm will be the subject of a separate study, and so the investigation of combined radar–radiometer retrievals is deferred. Finally, the differences between LSA estimates derived using two different snow densities, namely 0.10 g m^{−3} and 0.15 g m^{−3}, are displayed in the bottom panel of Fig. 7. As discussed previously, retrievals above the freezing level are highly sensitive to assumed snow particle electromagnetic scattering properties, which depend on the snow density. The use of high-frequency radiometer observations may reduce the uncertainties in snow water content estimates if more complex scattering calculations (e.g., Liu 2008) based on realistic snow habits (e.g., Westbrook et al. 2004) are employed.

Differences of estimated precipitation water contents using LSA, assuming different (top) shape factors and (bottom) snow densities. The assumed shape factors in the top panel are *μ* = 0.0 and *μ* = 1.0, while the assumed snow densities in the bottom panel are 0.1 and 0.15 g m^{−3}.

Citation: Journal of Applied Meteorology and Climatology 50, 7; 10.1175/2011JAMC2655.1

Differences of estimated precipitation water contents using LSA, assuming different (top) shape factors and (bottom) snow densities. The assumed shape factors in the top panel are *μ* = 0.0 and *μ* = 1.0, while the assumed snow densities in the bottom panel are 0.1 and 0.15 g m^{−3}.

Citation: Journal of Applied Meteorology and Climatology 50, 7; 10.1175/2011JAMC2655.1

Differences of estimated precipitation water contents using LSA, assuming different (top) shape factors and (bottom) snow densities. The assumed shape factors in the top panel are *μ* = 0.0 and *μ* = 1.0, while the assumed snow densities in the bottom panel are 0.1 and 0.15 g m^{−3}.

Citation: Journal of Applied Meteorology and Climatology 50, 7; 10.1175/2011JAMC2655.1

## 5. Conclusions

In this study, an algorithm to retrieve precipitation vertical profiles from spaceborne dual-frequency (Ku/Ka band) radar observations is formulated and investigated. The algorithm is based on a generalized HB attenuation correction methodology that yields generic PSD profiles from Ku-band radar data and an optimization procedure that adjusts the Ku-band-derived PSDs to make them more consistent with coincident Ka-band reflectivity observations and SRT PIA estimates at both Ku and Ka bands. The consistency between the Ku-band retrievals, the Ka-band reflectivity observations, and SRT PIA estimates at both Ku and Ka bands is quantified using a quadratic cost function that is minimized with respect to parameterized profiles of PSD intercepts using a Gauss–Newton method.

The algorithm is tested using both synthetic and actual airborne data. In the synthetic data evaluation, actual Ku-band radar observations along with assumed profiles of PSD intercepts, cloud water, and relative humidity are used to generate Ka-band observations. Retrievals using the synthetic data show the algorithm’s ability to estimate two-parameter PSD information from dual-frequency observations. Alternatively, if only Ku-band data are available, the same algorithm yields estimates of PSDs with reasonable, but greater, levels of uncertainty.

The algorithm is applied to actual airborne observations from the TC4 field experiment with and without SRT PIA incorporated into the retrieval process. The SRT PIA information is found to have a significant impact on precipitation estimates, especially near the earth’s surface, which is an indication that dual-frequency above-ground reflectivity observations alone may be insufficient for deriving unbiased precipitation estimates, and that SRT PIA information, when reliable, should be utilized in the retrieval process. Retrieved precipitation is also shown to be sensitive to the assumed shape of the particle size distribution, the assumed cloud water and water vapor distributions, and the assumed snow density. The inclusion of the dual-frequency algorithm within a combined radar–radiometer retrieval framework is expected to reduce the sensitivity of precipitation estimates to these factors. Also, valuable insight should be gained from the analysis of dual-frequency radar and in situ observations originating from future field campaigns.

Future work needs to be carried out to assess this algorithm’s performance and robustness within a combined radar–radiometer retrieval framework. Given the sensitivity of radiometer observations to variables that cannot be estimated from radar observations alone (e.g., cloud water, water vapor, snow density) combined radar–radiometer retrievals are likely to be better conditioned and consequently less uncertain than radar-only retrievals. However, because the physical modeling of both radar reflectivities and radiometer-sensitive microwave radiances is subject to uncertainties, the effort to develop combined radar–radiometer retrieval methods should be coupled with rigorous studies to accurately assess the uncertainties in radar and radiometer forward modeling.

## Acknowledgments

This research was supported by NASA’s Precipitation Measurement Missions (PMM) program. The contribution by Dr. Simone Tanelli was performed at the Jet Propulsion Laboratory, California Institute of Technology under contract with the National Aeronautics and Space Administration. The manuscript benefited from the constructive comments of three anonymous reviewers.

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