The effects of attenuation correction in rainfall estimation with X-band dual-polarization radar were investigated with a dense rain gauge network. The calibration bias in reflectivity () was corrected using a self-consistency principle. The attenuation correction of and the differential reflectivity () were performed by a path integration method. After attenuation correction, and were significantly improved, and their scatter plots matched well with the theoretical relationship between and . The comparisons between the radar rainfall estimation and the rain gauge rainfall were investigated using the bulk statistics with different temporal accumulations and spatial averages. The bias significantly improves from 70% to 0% with . However, the improvement with was relatively small, from 3% to 1%. This indicated that rainfall estimation using a polarimetric variable was more robust at attenuation than was a single polarimetric variable method. The bias did not show improvement in comparisons between the temporal accumulations or the spatial averages in either rainfall estimation method. However, the random error improved from 68% to 25% with different temporal accumulations or spatial averages. This result indicates that temporal accumulation or spatial average (aggregation) is important to reduce random error.

1. Introduction

Weather radar has provided useful information about hydrometeors for various meteorological and hydrological applications since its introduction in meteorological observations. Weather radar can observe various parameters of meteorological phenomena with high spatiotemporal resolution over wide observational areas. However, it suffers from many error sources, including radar calibration, beam shielding, attenuation, bright band contamination, beam broadening, and anomalous propagation. Many researchers have studied the characteristics of these error sources and ways to improve the quality of radar data [13].

Recently, X-band dual-polarization radar has received significant attention due to its finer resolution, ease of mobility, and lower cost compared to longer wavelength radars. However, the attenuation is a very important issue in X-band, since it is inversely proportional to radar wavelength. The values of the radar parameters associated with the back-scattered power, such as reflectivity () and differential reflectivity (), can be significantly reduced by attenuation.

The attenuation is caused by absorption and scattering in the medium along the propagation path of the radar beam. The attenuation is severe where the medium is dense and its composition size is large. The attenuation by atmospheric gas molecules is small, being about 1.5 dB per 100 km in the C-band [3]. However, media such as rain drops, hail, and melted snow particles can cause significant attenuation, especially in shorter wavelength radar. The amount of attenuation in the C-band can reach about 12 dB due to strong convective cells as compared to the S-band [3]. Furthermore, the attenuation accumulates over distances as a radar beam propagates. The power is frequently lost completely over far ranges. Therefore, it is not possible to monitor and analyze severe weather, such as heavy rains, typhoons, and heavy snows, without the proper correction of the attenuation in the C- or X-band radars.

The attenuation correction has been investigated by many researchers. Tuttle and Rinehart [4] suggested an attenuation correction method using dual-wavelength (S- and X-band) radar measurements with a relationship between specific attenuation () and . Recently, the specific differential propagation phase shift () has been used widely for attenuation correction because is not affected by radar power calibration, attenuation, and partial beam blocking. In addition, is less sensitive to the natural variability of drop size distributions (DSDs) in rainfall estimation. Bringi et al. [1] showed that both and the specific differential attenuation () are almost linearly related to through scattering simulations, and these relationships have been accepted by many researchers. However, the coefficients of these relationships derived from the scattering simulations vary significantly with temperature, DSD variability, and the drop deformation model. Park et al. [5] showed that the coefficients of - and - relationships vary greatly from 0.139 to 0.335 dB(°)−1 and from 0.114 to 0.174 dB(°)−1 in the X-band, respectively, due to changes in temperatures and the different drop deformation models.

While has many advantages in the attenuation correction as described above, estimating from the measured total differential phase shift () is challenging because of the backscatter differential phase shift () and the measurement errors for [1]. Scarchilli et al. [6] used an iteration method with a - relationship to remove from and corrected the attenuation using estimated in the C-band. Anagnostou et al. [7], Kalogiros et al. [8], and Chang et al. [9] used an iteration method in the X-band. As a different method for removing , Hubbert and Bringi [10] separated and the differential propagation phase () from through an iterative filtering technique (FIR) and calculated the hail signal from . Park et al. [5] also used the same filtering technique to extract for correcting the attenuation and the differential attenuation in the X-band. Recently, Mishra et al. [11] investigated dual-polarimetric products and three types of rainfall estimation results with high spatiotemporal resolution data from X-band radar, S-band radar, and disdrometer data with an intercomparison and T-matrix simulation method [12]. Mishra et al. [11] used a very similar attenuation correction process in their work, where was calculated by an FIR filtered , and was calculated by an - relationship based on a self-consistency method.

Two rainfall estimation methods, and , were used for evaluation of the attenuation correction effect. The self-consistency based correction of the attenuation and the differential attenuation from the FIR filtered were used to improve the accuracy in the rainfall estimation methods by X-band polarimetric radar. The accuracy evaluation of the rainfall estimation methods was performed by comparisons with rain gauge measurements with high spatial resolution. However, there were instrumental uncertainties and errors in the representativeness of the rain gauge measurements. The instrumental error has several sources, including the gauge calibration, wind effects, and wetting/evaporation loss [13, 14]. The representativeness error is linked with the spatial sampling area and the temporal accumulation of the rain gauge [15]. Habib et al. [16] investigated sampling error of the tipping bucket gauge as function of accumulation times in a simulation study. Ciach [17] verified local random errors in the tipping bucket gauge through experimental data. Habib et al. [18] investigated the correlation with separation distances in a rain gauge cluster. In this study, we considered the calibration effects in the instrumental error of the rain gauge. Instrumental error from the calibration effect was removed by laboratory experiments to provide more accurate and reliable references. The representativeness error was investigated by the temporal accumulation and spatial average of rainfall amount.

In Section 2, the radar and rain gauge data used in this study are presented. The methods for the attenuation correction by , the rainfall estimation and its verification, and the analysis of the natural variability of rain fields using rain gauge data are described in Section 3. The analysis results are shown in Section 4. The results are summarized in Section 5.

2. Data

2.1. Radar Data

The radar data from the X-band dual-polarimetric radar (NIMS-XPOL) of the National Institute of Meteorological Sciences (NIMS) was used in this study. The general characteristics of the NIMS-XPOL data are shown in Table 1. The NIMS-XPOL can be installed onto a five-ton truck bed (Figure 1(a)) and mounted on a steel tower bed (Figure 1(b)).

The NIMS-XPOL was operated during June 2010 at Muan-gun, Jeollanam-do, which is on the southwest coast of Korea (latitude = N 35.0940°, longitude = E 126.285°) for the observation of heavy rains during the summer monsoon season. The rain estimation in Section 3.2 was performed with the NIMS-X radar data collected during 5.5 hours, from 1600 UTC to 2130 UTC, on July 10, 2010. During this rain event, the NIMS-X was mounted on a steel tower bed in the Muan-gun observation center to minimize the effect of beam shielding and ground clutter, and a full volume scan with 14 Plan Position Indicators (PPIs) was performed every 2.5 min. The gate spacing was 150 m, and the Pulse Repetition Frequency (PRF) was 999 Hz. And the total rainfall amount was over 50 mm. The evolution of the rain field is shown in Figure 2. The echoes moved toward the northeast, and the small and weak rain cells near the radar site at 1601 UTC were replaced by the strong convective cells approaching from the southwest.

2.2. Rain Gauge Data

The rain gauge data was collected by ten tipping bucket (TB) rain gauges operated by the Kyungpook National University (KNU), Korea. The tip size of all of the gauges was 0.2 mm, and the diameter of the receiving orifice was 15.39 cm. The time resolution was 0.5 s, and the data was recorded based on the event (tipping) time. To compare with the estimated rain rate () from the NIMS-XPOL radar, the rain accumulation from ten gauges was collected during the month of July 2010 near Unnam-myeon, which is located at a distance of about 16 km at 160° azimuth angle from the NIMS-XPOL radar. The area was only slightly affected by beam shielding of the NIMS-XPOL. Considering the geographical situation and the limited locations for the installation, all gauges were installed on the rooftops of buildings. Figure 3 shows the location of the NIMS-XPOL and the deployment of the ten gauges (R is the radar site, and a number represents a gauge location). The total rainfall amount for the month at each gauge site is shown in Table 2. At all gauge sites, the total rainfall accumulation was over 300 mm for the month. The rainfall amount measured during the same period with the NIMS-XPOL radar data used in the rainfall estimation was about 50 mm per 5.5 hours (see Table 2).

The instrumental biases of all gauges were calculated through an ideal experiment using laboratory and field observations for 9 months from October 2009 to June 2010 (except April 2010) at KNU. The rain gauge dataset was corrected for the instrumental bias prior to the detailed analysis.

3. Methodology

3.1. Attenuation Correction Algorithm Using Differential Propagation Phase Shift

The attenuation correction algorithm was performed by the procedure as shown in Figure 4, which included quality control of the radar data, estimation of , calculation of the attenuation amount, and the attenuation correction of and .

As a part of the quality control of the radar data, and were corrected for instrumental biases. calibration bias of about 3.7 dB was obtained by comparison with the reflectivity from the particle size velocity disdrometer (PARSIVEL) and from the NIMS-XPOL radar. The calibration bias of −1.5 dB was calculated from the vertical pointing data [19]. The isolated point echo shows that the values in their surrounding pixels existed by less than 50% of the total pixels to be removed. The threshold of 0.9 was applied to the entire radar measurement field.

After applying the quality control measures, was estimated from measured by eliminating and the observational noise through an iterative filtering technique. In this study, the 20th FIR filter of Hubbert and Bringi [10] was used. This filter preserved a monotonic increasing trend of due to the propagation medium, while it removed the smaller scale fluctuations compared to the filtering window (2.5 km when the gate size is 0.125 m) due to and the observation noise. Hubbert and Bringi [10] also found that repeating the filtering process 10 times produced good results.

The additional problem in the estimation of was the variable offset of . observation can be noisy in near range. Radar, in general, has offset to avoid observing negative value of in near range. Ideally, the offset should not change with the azimuthal angles. However, the offsets of measured of the NIMS-X varied with the azimuthal angles, and values decreased near the radar when rain cells existed above the radar. Therefore, the offset was determined as the minimum value of within 3 km of the radar, and estimated filtered was adjusted accordingly.

The calculation of and was based on the following two relationships [1, 5, 20]:where and are the specific attenuation and the specific differential attenuation at range from the radar, respectively. is the specific differential one-way phase shift calculated using the following equation:where is between and . The coefficients and were derived from , , and obtained by scattering simulations with the DSDs data collected by the Precipitation Occurrence Sensor System (POSS) from March to September of 2001 in Pusan, Korea [21]. The total path integrated attenuation and differential attenuation were calculated with by integrating the following:Number 2 in the equations indicates that the values are two-way values.

Finally, the measured reflectivity  [dBZ] and the differential reflectivity  [dB] at were corrected with the calculated two-way path integrated attenuation and differential attenuation:

3.2. Radar Rain Estimation and Comparison with Rain Gauge Data

A comparison between estimated from the radar parameters and the rain rate () from the rain gauge data was performed to evaluate the attenuation correction algorithm. In addition to the rain attenuation, the difference between and was caused by the errors due to the instrumental uncertainty and representativeness errors of the rain gauge data, the radar observational noise, and the errors in the radar rainfall estimation. The bias due to the instrumental uncertainty in gauge data was removed by properly calibrating the gauges through laboratory tests and a gauge intercomparison. The representativeness errors were due to the mismatch of the sampling area (volume) between the gauge and the radar. The random error in the gauge data could be minimized by time and areal integration. The errors due to the measurement noise in the radar data could be reduced in a similar manner. The time offset between the rain gauge and the radar sampling area was ignored due to the close distance (about 16 km) and the low elevation angle (3°).

Therefore, and were derived with two different radar sampling areas and with increasing accumulation time.

(1) versus . was estimated from the average radar measurement with 9 pixels (0.38 km2 at 16 km range). The gauge rainfall rate was derived from the rainfall accumulation from an individual rain gauge that had a sampling area of 0.07 m2.

(2) versus . was estimated from the areal averaged radar parameters at a 1.6 km × 3.1 km radar measurement resolution. was the average value of from the ten gauges within the same area.

Estimated from radar parameters was calculated with two rain estimators as shown in Table 3. These rain estimators were derived by a least squares fit with the theoretical , , and obtained by scattering simulations with the DSD data collected by POSS from March to September of 2001 in Pusan, Korea [21]. To improve the estimation accuracy, each estimator was derived for two categories. The reflectivity threshold of 35 dBZ was used as a standard stratiform/convective rain classification [22]. The threshold of 0.3 dB was used to minimize the effect of the measurement noise. The PPI data with an elevation angle of 3° was used to suppress the beam shielding and ground clutter. The and fields from the radar were smoothed by the linear average of values at 3 × 3 pixels to reduce the observational noise.

The bias in from the ten rain gauges was corrected by the laboratory test and the intercomparison with field data. The detail is presented in Appendix. To evaluate the attenuation correction algorithm and verify the rainfall retrieval accuracy, the comparisons of and were represented by the general statistics such as normalized bias (NB), normalized standard deviation (NSD), root-mean square error (rmse), relative rms error (r_rmse), and Spearman correlation (corr.) as follows:where is the number of and pairs at a given temporal integration and the overbar indicates the temporal average.

3.3. Spatial Correlation and Variability of the Rain Fields

Rain gauges are widely used to measure rainfall amounts due to many advantages, including easy installation, mobility, low price, and ease of data processing. The rain gauge data is used as a reference for the ground rainfall amount for the evaluation of rain retrieval algorithms, adjustment of other instruments, data assimilation, and other hydrological applications. However, it is affected by instrumental errors and representativeness errors due to the variability of rain fields.

In a TB rain gauge, the instrumental errors are due to improper calibration, the time delay of the tips, leakage due to its measuring principle, and so forth. This error is explored in the Appendix.

The representativeness errors are subdivided into spatial and temporal representativeness. They are mainly caused by having a small sampling area and a limited sampling time due to the gauge measuring principle. The actual rain fields vary with different spatiotemporal scales that are not equivalent to the spatial and temporal resolution of the rain gauge. Therefore, the rain gauge data represent the actual rain fields in a very limited manner.

These errors should be considered and minimized prior to using rain gauge data as ground truth. Furthermore, the degree of these errors has to be understood quantitatively, since there can be other error sources in various applications. In this section, the spatial and temporal variability of the rain fields are investigated using the rain data collected by the ten rain gauges for the month of July 2010 at Muan, Korea.

First, the Spearman correlation coefficient between a pair of values from the th and th individual rain gauge with integration time was calculated from the following equation to obtain the Spearman correlation coefficient of the rain fields:where is the number of gauge data pairs at given and the overbar indicates the temporal average of the rainfall rate. It was derived with to research the spatial and temporal scale of the variation for the rain field.

In addition, the effect of the natural variability of the rain fields within two different areas ( and ) was explored by analyzing the bias and random error between the spatially averaged rainfall rate and from the individual gauge. The NB and NSD of with were calculated as follows:where indicates the th gauge and the overbar indicates the temporal average.

This analysis provided a reasonable spatial average and temporal accumulation resolution for the calculation of more accurate and realistic rainfall amounts from the gauge data and a quantitative guideline regarding the errors in rain estimation due to the variability of the rain fields.

4. Results

4.1. Attenuation Correction of Reflectivity and Differential Reflectivity

The attenuation correction algorithm in Section 3.1 was applied to the NIMS-XPOL radar data. was estimated by eliminating and the observational noise from measured using an iterative FIR filter. The offset of was then adjusted. Figure 5 shows the PPIs of measured and filtered . After applying the FIR filter, the small scale variation due to and observational noise in measured was reduced, and filtered (estimated ) monotonically increased with an increase in range. The maximum value of estimated reached to 140°. In addition, estimated at the azimuth angles of 150° and 200° sharply increased with the loss of signal beyond these sharp gradient areas. This reflected that strong convective cells existed in these directions and that these cells caused the severe signal attenuation. Estimated values between 250° and 360° azimuth angle decreased after filtering since offsets were positive values in these directions. Figure 6 shows the range profile of measured and filtered for estimation of at 71°, 160°, and 334° azimuth angles. The unexpected large values near the radar were removed by the threshold (red line). The small fluctuation in measured due to and the observational noise was effectively removed after filtering. The value of estimated was adjusted to 0 by the offset (blue line).

Estimated was used to calculate the path integrated , and the measured values were corrected as shown in Figure 7. Figure 7(a) represents measured-attenuated and relatively small values of at far ranges. This may indicate that the values at far ranges were affected by the strong attenuation due to strong convective cells near the radar. This spatial pattern of was the typical feature of the attenuated radar signal due to the rain. After correcting the attenuation, the value of the field became larger over the entire area, and the radially attenuated was corrected by showing a typical rain cell pattern in (Figure 7(b)). The largest difference between the uncorrected and the corrected at 2101 UTC was over 50 dB. However, the white area behind the strong echoes was not detected as there was a complete loss of the signal power. These regions could not be corrected by this algorithm. The circle pattern of fields within about a 4 km range from the NIMS-XPOL could not present the actual rain echoes due to the instrumental issues (the same was true for ). These results are also presented in the range profiles in Figure 8.

Similarly, measured were corrected with the path integrated derived from the path integrated using (4) (see Figure 9). Before applying attenuation correction, the attenuation signature in was determined. Ideally, the value for rain should be positive since rain drops are oblate due to aerodynamic force. However, the measured field in Figure 9 showed a negative value over wide areas. After correcting the attenuation, the field was larger than 0 dB and showed a realistic rain pattern. This is also presented in the range profile of Figure 10. The largest difference of between before and after attenuation correction at 2101 UTC was about 8 dB. The values around the 220° azimuth angle beyond 40 km were the largest. They did not match with the area of the largest values (around the 210° azimuth angle with a range of 20 km and 40 km). This was an unexpected result because is proportional to in theory. This mismatch between and at far range may be due to contamination due to beam broadening and accumulated errors due to uncertainty in the attenuation correction with different ranges.

Figures 11 and 12 show the time series of and at the ten gauge sites before and after applying the attenuation correction. The differences between uncorrected and corrected values existed after 1800 UTC and were at a maximum around 2100 UTC. This attenuation correction was evaluated through comparison with the theoretical values of and . In Figure 13, the uncorrected - scatter plots are apart from the theoretical - values [23]. After attenuation correction, the - scatter plots were close to the calculated values. This indicated that and over the gauge sites were corrected with reliable values.

4.2. Variability of the Rain Fields

The Spearman correlation coefficient of the rainfall rate from the 10 spatially distributed rain gauges was calculated with accumulation time and separation distance (Figure 14). The overall Spearman correlation coefficient decreased with increasing separation distance at all accumulation times. This tendency was similar to the result from Habib and Krajewski [24]. However, the correlation value was higher in this study. Note that the gauge tip resolution in Habib and Krajewski [24] was 0.254 mm, while it was 0.2 mm in this study. In addition, the rainfall rates from the gauge data used in this study mainly consisted of moderate rainfall rates, while Habib and Krajewski [24] used data containing heavy rainfall rates.

For accumulation times of less than 10 min, the correlation at the same distance was dramatically increased with increasing accumulation time, and the slope of the correlation function was steep. This was due to the reduction of the instrumental errors of the gauge data by time accumulation. This indicated that rainfall accumulated for less than 10 min from single gauge data cannot represent the rainfall over its surrounding area due to instrumental errors. For accumulation times longer than 10 min, the slope became less steep. This reflected the remaining variability of the rain field. In addition, the accumulated rainfall rate of about 10 min was suitable for minimizing the instrumental uncertainty while preserving the variation in the rain field. The correlation reached about 0.98 at 0.5 km in 10 min of accumulation, and this approached 0.98 at 1.0 km at 60 min accumulation. Therefore, a single rain gauge mostly represented the rainfall rate within 0.5 km and 1.0 km with 10 min and 60 min accumulation, respectively.

The NB between an areal averaged rainfall rate and a single gauge rainfall rate is shown with accumulation time in Figures 15(a) and 16(a). Where the average area was 0.38 km2 (corresponding to 9 pixels of NIMS-XPOL radar at 16 km range), the NB reached a 6–8% maximum. Where the averaged area is 6 km2 (corresponding to the coverage for all of the gauges), the NB reached about a 10% maximum. Furthermore, the NB hardly changed with accumulation time. Note that this statistic was derived after removing instrumental bias. This indicated that the rainfall rate from a single gauge was biased due to the spatial variability of the rain fields, and this bias was maintained with accumulation time.

The NSD of a single gauge for a mean area of 0.38 km2 was over 40%, and it reached about 70–90% for a mean area of 6 km2 at an accumulation time of 1 min (see Figures 15(b) and 16(b)). This statistic included instrumental errors (about 40–60% at 16 mm h−1 and 60–80% at 10 mm h−1 as shown in the Appendix) as well as the spatial variability of the rain fields. This indicated that the variance between the point and area values from the gauge data at short accumulation times was similar to the errors due to the instrumental uncertainty of the rain gauge. The NSD in 60 min accumulation decreased to over 10% and about 15–45% with a mean area of 0.38 km2 and 6 km2, respectively, including the NSD of 6–10% due to instrumental uncertainty. This indicated that the rainfall rate from single gauges may differ significantly from the actual rainfall rate due to the variability of the rain fields and the instrumental uncertainty in short accumulation times.

4.3. Verification of Rainfall Retrieval

The rainfall rate from the NIMS-XPOL radar measurements was retrieved with two rainfall rate estimators: and . The estimated rainfall rate was verified through comparison with the rainfall rate () from the rain gauge data. These two estimators were applied before and after the attenuation correction. First, was compared with at 10 min accumulation (Figure 17). Using , the NB, NSD, rmse, and r_rmse without the attenuation correction were significantly large at 70%, 127%, 12.7 (mm/hr), and 78%, respectively. However, they were reduced to −1%, 52%, 5.21 (mm/hr), and 32%, respectively, after applying the attenuation correction. Using , the NB was just 3%, NSD was 49%, rmse was 4.96 (mm/hr), and r_rmse was 31% before applying attenuation correction. This was similar to the result from after attenuation correction. However, there was no significant change in with attenuation correction. This means that was less sensitive to rain attenuation than was , because is proportional to , and is inversely proportional to in this rain estimator (see Table 3). Furthermore, comparing the analysis of variance results between areal (0.38 km2) and point (0.07 m2) values from the gauge data (Section 4.2), half of the errors after attenuation correction were produced by the small scale variability of the rain fields and the instrumental uncertainty of the rain gauge.

A similar comparison is shown in Figure 18 for a 60 min accumulation. Using , the NB, NSD, rmse, and r_rmse were decreased from −65%, 86%, 7.1 (mm/hr), and 70% to −5%, 34%, 2.8 (mm/hr), and 28% by the attenuation correction, respectively. Using , the NB, NSD, rmse, and r_rmse were only slightly decreased after the attenuation correction. However, the NSD, rmse, and r_rmse were reduced when compared at 10 min accumulation. In the same accumulation time, the errors in the gauge data reached to over 15%.

This comparison was affected by different sampling areas of the gauges and the radar. Therefore, the areal average values were compared (Figure 19). Using with the areal averaged radar measurements, the NB was reduced from −69% to 7%, NSD was reduced from 122% to 42%, rmse was reduced from 3.9 (mm/hr) to 1.3 (mm/hr), and r_rmse was reduced from 77% to 26% at an accumulation time of 10 min. Using , the NB, NSD, rmse, and r_rmse were decreased from −24%, 67%, 2.1 (mm/hr), and 42% to 5%, 39%, 1.2 (mm/hr), and 24%, respectively.

The NB and r_rmse with matched sampling areas between the gauge and the radar are shown in Figures 20 and 21. The reduction of NB due to temporal accumulation was small in both of the rain estimators. The NB was reduced to less than 7% by attenuation correction for all accumulation times with both and . The attenuation correction effect was significantly greater in . Similarly, the r_rmse was reduced significantly in by attenuation correction (from 68% to 25% at a 60 min accumulation). The reduction of the r_rmse due to temporal accumulation was larger in because the significant observational noise of was smoothed. The r_rmse was decreased from 18% to 15% in at a 60 min accumulation time after attenuation correction.

5. Conclusions

In this study, an attenuation correction algorithm based on was developed to improve the accuracy of the rainfall estimation using X-band radar. This algorithm was evaluated with radar measurements from NIMS-XPOL. However, measured contained and observation noise as well as . Furthermore, the offset varied with azimuth angles and decreased near the radar when rain cells were above the radar. In this study, was estimated by an iterative filtering technique and by adjusting with an offset determined as the minimum value of within 3 km of the radar. As a result, estimated monotonically increased. The path integrated value of and was calculated from estimated using and relationships derived from the DSDs data. Measured and were corrected with the calculated path integrated and by each gate. The attenuated signal patterns of and were restored to a typical rain echo pattern. However, the attenuation corrected and fields were not matched at distant ranges. This was likely because of contamination due to beam broadening and the accumulation of errors with increasing range. Comparing the - scatter plots over the 10 rain gauge sites with the results obtained from a scattering simulation with the DSD data, the attenuation corrected - scatter plots are in good agreement with the - scatter plots from the DSDs.

The validation for the improvement of accuracy in the rainfall estimation through attenuation correction was performed by comparing with dense rain gauge network data. from the attenuated (observed) produced a severe underestimation with an NB, NSD, rmse, and r_rmse of 70%, 127%, 12.7 (mm/hr), and 78% at 10 min accumulation, respectively, while from the attenuation corrected showed better agreement with the gauge measurements, with an NB, NSD, rmse, and r_rmse of −1%, 52%, 5.21 (mm/hr), and 32% at 10 min accumulation, respectively. At 60 min accumulation, the NB, NSD, rmse, and r_rmse were decreased from −65%, 86%, 7.1 (mm/hr), and 70% to −5%, 34%, 2.8 (mm/hr), and 28%, respectively. Using , the NB, NSD, rmse, and r_rmse were only slightly reduced even if attenuation was corrected but were smaller than when using . This indicated that was less sensitive to the attenuation than . In addition, half of the errors that remained after attenuation correction were caused by the small scale variability of the rain fields and the instrumental uncertainty of the rain gauges. Using an areal averaged value, the NB was reduced to less than 7% with attenuation correction using either rainfall estimator, regardless of accumulation time. The r_rmse were significantly reduced by attenuation correction in , and the reduction of r_rmse with was even more dramatic.

As summarized above, the rain attenuation for and in the X-band was corrected by , and the results showed a good agreement with the value obtained by scattering simulations with the DSD datasets. The results of comparison with rain gauge data also showed a significant improvement in the accuracy of rainfall estimation by attenuation correction, which supports the quantitative use of the X-band radar in rain data retrieval.


A. Instrumental Uncertainty of the Rain Gauge

The instrumental uncertainty of the TB rain gauge is associated with improper calibration, leakage and precipitation missing the gauge due to the measurement principle, and wetting and evaporation losses. In addition, external sources, such as wind, turbulence, and installed position, also contribute to the instrumental uncertainty. Ciach [17] reported that the TB gauge data suffers a significant uncertainty associated with random differences between closely collocated TB gauges through the analysis of the error as a function of the rainfall intensity for three timescales. In addition, the improper calibration induces a bias in the rainfall measurement, and this bias cannot be removed by increasing accumulation time. Therefore, the proper correction or processing of TB gauge data is necessary to obtain accurate and reliable reading of the rainfall amount.

In this appendix, instrumental biases were calculated to reduce the instrumental uncertainty through an ideal experiment in the laboratory and a field intercomparison with 10 TB rain gauges. In addition, the random errors were quantitatively calculated as a function of rainfall rate and accumulation time.

A.1. Correction of Instrumental Bias

The instrumental bias of the th gauge was defined as a combination of the absolute bias of the reference gauge and the relative bias of the th gauge according to the following equation:

signified the ratio of the calculated value from the instrumental resolution of the reference gauge to the true value measured by other instruments:

In this study, was derived by an ideal experiment using an electronic scale. First, the reference gauge was put on the scale, and the scale was initialized. The water drops flowed out into the receiving orifice of the reference gauge until the tipping number became 60. The measured weight of 60 tips was 214.4 g, while the theoretical (or expected) value was 224.4 g for the reference gauge (receiving orifice size of 15.45 cm, 60 tips, and 0.2 mm tip resolution). Therefore, the absolute bias of the reference gauge from (A.2) was about 0.955. This indicates that the rainfall amount measured by this reference gauge was overestimated by about 4.5%, and this bias should be corrected prior to any interpretation.

represented the ratio of the observed (recorded) value from the th gauge to the observed (recorded) value from the reference gauge:

was calculated from ten collocated rain gauges including the reference gauge, located at an observation field at KNU, Korea. The observational period for intercomparison was from October 2009 to June 2010 (14 rainy days), and the total accumulated rainfall for this period was about 300 mm. The results are presented in Table 4. All relative biases were mainly larger than 1.0. This indicated that the most of gauges underestimated the rainfall amount compared to the reference rain gauge. The relative bias of the reference gauge () was 1.0.

Finally, was calculated from (A.1) (see Table 4). All instrumental biases were between 0.90 and 1.1, and the mean value of the biases was nearly 1.0. This indicated that the rainfall rate from a single gauge data had a maximum 10% bias. These biases were corrected for each gauge to remove existing instrumental errors.

A.2. Quantification of Random Errors

To quantify the random error due to instrumental uncertainty, the NSD of the ten gauges was calculated with accumulation time and rain rate using data from an intercomparison. The NSD of the th gauge compared to the reference gauge was derived for 20 rain rate classes () and 17 accumulation time classes () as follows:where and indicate the reference and individual gauges, respectively. The overbar means the temporal average of the rainfall rate. The NSDs of nine different gauges (except the reference gauge) were averaged to obtain the two-dimensional average NSD (Figure 22). The average NSD tended to decrease with increasing accumulation time and with increasing rain rate. The NSD was about 10–15% when accumulation time was 10 min and the rain rate was 10 mm h−1. The instrumental errors were quite significant for longer accumulation times and higher rainfall rates. These errors should be used as a guideline when a single gauge is used as a reference for any validation study.

Competing Interests

The authors declare that they have no competing interests.


This paper has been revised and extended from Ms. Young-A Oh’s M.S. thesis [25] of Kyungpook National University. This research is supported by Development and Application of Cross Governmental Dual-Pol Radar Harmonization (WRC-2013-A-1) project of the Weather Radar Center, Korea Meteorological Administration. This work was funded by the Korea Meteorological Administration Research and Development Program under Grant KMIPA2015-1010.