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International Journal of Research in Engineering and Science (IJRES)
ISSN (Online): 2320-9364, ISSN (Print): 2320-9356
www.ijres.org Volume 1 Issue 3 ǁ July. 2013 ǁ PP.34-39
www.ijres.org 34 | Page
Determination of Bright Band in Malaysia through Radar Data
Analysis
Abayomi I. O. Yussuff1, 2
, Nor Hisham Haji Khamis1
2
Lagos State University, Department of Electronic & Computer Engineering, Lagos, Nigeria
1
Universiti Teknologi Malaysia, Department of Communications Engineering, Skudai, Malaysia
Abstract— Restrained usages of X-band and below is mostly due to commercial operations along the slant-
path. In tropical regions, signal degradations are often due to hydrometeors such as rain, hail, cloud, and the
melting layer. In addition, these can cause several problems, such as signal fading, depolarization and co-
channel polarization due to scattering along the satellite link. Inadequate availability of database along the slant-
path in tropical regions for use in rain propagation studies at microwave frequencies required more studies to be
carried out. This work concerns the characterization of bright band in a tropical station. The effects of seasonal
variations on rain height can give the information that are valuable for designing and planning of satellite link in
a tropical region like Malaysia. The meteorological radar data for this work was obtained from the
Meteorological Department of Malaysia. The result of the analysis of the processed radar data and the obtained
parameters for the bright band showed good agreement with works carried out by other researchers in the
tropical region.
Index Terms— Bright band, Stratiform, Convective, freezing height, 00
C isotherm, RAPIC, PPI, RHI.
I. INTRODUCTION
For the study of melting layer characteristics, rainfall types are grouped into stratiform and convective.
In simple terms, stratiform rains comprise light intensity widespread rainfalls within limited vertical extent of
rain height, and are produced by stratus clouds. On the contrary, convective rainfalls are produced by cumulus
clouds; with narrow horizontal area and associated with extensive rainfall rates and height [1]. Rain height is
generally known to be highly correlated with signal attenuation and co-channel interference due to scattering.
The rain height distribution is important because it can be used to investigate the mechanisms responsible for
variations in the attenuation distributions at any station. The prediction methods being used to estimate the
degree of signal attenuation encompasses the various location-specific meteorological factors, and rain height is
one such factor. The rain height, RH is also directly related to the zero degree Celsius isotherm height, 0H .
Rain height information can be indirectly obtained by studying the melting layer height in stratiform rain type.
One major source of slant-path attenuation prediction errors is the complex nature of the rainfall structure along
this path. Another reason is the uncertainty in the estimation of attenuation due to the melting layer. The
difficulties in relating RH to 0H in the tropics had also been attributed to insufficient database and peculiar
rainfall types existing in the tropical regions [2].
The rain height is being employed in ITU-R Rec. P.618-10 (for slant-path attenuation prediction), ITU-
R Rec. P.452-14 (for co-channel interference estimation), ITU-R Rec. P.620-6 (for coordination distances), and
ITU-R Radio Regulations Appendix 7 (for regulatory issues of coordination) [3]. The ITU-R Rec. P.618-10 uses
the rain height as the boundary below which the slant-path attenuation is integrated while the ITU-R Rec. P.452-
10 uses it to discriminate rain scatter from ice scatter, incorporating variability into the mean freezing height. It
uses an effective rain cell model with rain height parameterized vertical dimension, adopting the effective rain
height rather than the melting layer’s height. The rain height can be considered to represent the boundary
between the rain region and the snow region and it often correspond to the 00
C isotherm (mostly during
stratiform rain events). In the vertical dimension, the rainfall rate is assumed to be constant up to the point that
represents the top of the rain height and attenuation beyond the height is considered insignificant, and thus
neglected [3].
However, recent research has shown that the effect of melting layer on signal attenuation is not after all
negligible, especially for weak rain rates [4].
At the 0H , hydrometeors changes from solid to liquid in the melting layer, leading to increase in their
reflectivity; manifesting in the bright band signature seen in radar measurements. This band identification is
made possible because of its sharp peak of reflectivity in high frequency domain [5-7]. Furthermore, if the
Determination of Bright Band in Malaysia through Radar Data Analysis
www.ijres.org 35 | Page
bright-band was not recognized, it can result in serious over-estimation of precipitation reaching the ground by a
factor as high as five [8].
The melting layer is a major factor responsible for the problems being encountered in characterization
and modelling of microwave signal propagation. In the absence of actual attenuation measurement data, System
Designers are usually compel to rely on rain attenuation models, either for terrestrial or slant-path propagation.
This, unquestionably accentuate the importance of modelling in both link budget analysis and equipment
designs.
Radar Meteorologists define the melting layer as the region where melting occurs, and it lie just below
the 00
C isotherm height. The 00
C isotherm is that height at which the ice-to-water transition begins. The
variances in the propagation characteristics of ice and water presents an effective boundary referred to as the
bright band.
The height of the bright band is close to that 00
C isotherm, depending on the season and location of the station
of interest [3, 9-12]. The 00
C isotherm, rain and bright band heights most times lie close to each other (see
Figure 1), although they represent different parameters [3]. The difference between the effective rain height and
the freezing height is taking to be 360 meters according to [13], and is expressed as:
kmHHR 36.00  (1)
Where RH represents the mean rain height above mean sea level and 0H is the mean 00
C isotherm height
above mean sea level.
The frozen hydrometeors were observed to show a typical enhancement of radar bistatic reflectivity
(dBZ) as they fall through the melting layer, followed by a sharper decrease in reflectivity during the following
stages of the melting process [10]. To this effect, several researchers have developed and proposed quite a
handful of models for predicting attenuation in the melting layer [4, 14-17].
Figure 1. Bright band Conceptual Model.
II. METHODOLOGY
The meteorological radar data for this work was obtained from the Meteorological Department of Malaysia.
The analysis undertaken here is for a 62 km range from Kluang radar station (lat. 2.020
N, long. 103.380
E) to
Faculty of Electrical Engineering (FKE), Universiti Teknologi Malaysia (lat. 1.560
N, long. 103.640
E). The
azimuth from Kluang to FKE was evaluated to be 1690
. The data duration spans thirteen months (November
2006 to November 2007). However, this preliminary data analysis is based on data samples from January to
March 2007. The classification of the rain events is evaluated with the minimum amount of the rain rate that the
radar can detect; confirmed by using the widely accepted empirical relationship of the radar reflectivity factor Z,
and rainfall rate R, that is given by
b
aRZ  (mm6
m-3
) (2)
Where the most common values for a and b are 200 and 1.6 respectively, according to Marshall-Palmer
[18]. These are also the values used by the radar operators at the Malaysian Meteorological Department of
Malaysia.
This system uses the 3D RAPIC system and two modes of scans - The plan position indicator (PPI) and range
height indicator (RHI). The specification of the Kluang radar is given in Table I.
Determination of Bright Band in Malaysia through Radar Data Analysis
www.ijres.org 36 | Page
TABLE I. KLUANG RADAR SPECIFICATIONS [11]
For PPI scan there are 15 volumetric elevation angles, 0.5°, 1.2°, 1.9°, 2.7°, 3.5°, 4.6°, 6.0°, 7.5°, 9.2°,
11.0°, 13.0°, 16.0°, 20.0°, 25.0°, and 32.0°. The radar image of each of these selected angles was recorded
through the full RHI's azimuthal scan range of 360°. The elevations angles used in this work are 1.1°, 1.9°, 3.3°,
5.8°, 7.7°, 10.3°, 13.6°, and 18.1°.
The parameters of the melting layer are obtained from the detected bright band signature, after series of
processing that include, but not limited to, various levels of sorting, filtering and decoding to build the vertical
profile of reflectivity of the bright band.
III. RESULTS AND DISCUSSIONS
The vertical profile of reflectivity for the months of January, February and March 2007 are displayed in
Figures 1-3 respectively.
Table II compares the results of measurements with those obtained by other researchers that were also carried
out in other tropical stations and the ITU-Rec. P. 839-3. The ITU-Rec. P. 839-3 largely over-estimated the
measurements for the rain heights.
Significant changes were observed in the month-to-month data for the freezing heights, from 5.815 km, 4.327
km, to 7.742 km for the months of January, February and March respectively.
0 5 10 15 20 25
0
2000
4000
6000
8000
10000
12000
Radar reflectivity ( dBz )
Height(m)
Figure 2. VRP plot for January 2007 for Kluang, Malaysia.
5 10 15 20 25 30 35
0
2000
4000
6000
8000
10000
12000
Radar reflectivity ( dBz )
Height(m)
Figure 3. VRP plot for February 2007 for Kluang, Malaysia.
Determination of Bright Band in Malaysia through Radar Data Analysis
www.ijres.org 37 | Page
0 5 10 15 20 25 30
0
2000
4000
6000
8000
10000
12000
Radar reflectivity ( dBz )
Height(m)
Figure 4. VRP plot for March 2007 for Kluang, Malaysia.
The month-to-month variations in freezing heights, bright band heights, bright band thickness and rain
heights are shown in Figures 6-9 respectively.
Malaysia experiences two monsoon events yearly. These are the North-East (October to March) from the South
China Sea and South-West monsoon (April to September) from the Indian Ocean. This results in two rainy and
two dry seasons.
0 5 10 15 20 25
0
2000
4000
6000
8000
10000
12000
Radar reflectivity ( dBz )
Height(m)
Figure 5. Mean VRP plot for January - March 2007 for Kluang, Malaysia.
January is the end month of the North-East monsoon rain and the start of the dry season, while March is the end
of the North-East monsoon dry season and the beginning of the South-West monsoon rainy season.
January February March
0
1
2
3
4
5
6
7
8
Month of the year ( 2007 )
Zerodeg.celciusheight(km)
Month-to-month variation for freezing height
Figure 6. Month-to-month variation for 0H .
January February March
0
0.5
1
1.5
2
2.5
3
3.5
4
4.5
Month-to-month variation for BB height
Month of the year ( 2007 )
BBHeight(km)
Figure 7. Month-to-month variation for HBB .
Determination of Bright Band in Malaysia through Radar Data Analysis
www.ijres.org 38 | Page
January February March
0
0.5
1
1.5
2
2.5
3
3.5
4
4.5
5
Month-to-month variation for BB thickness
Month of the year ( 2007 )BBthicknessHeight(km)
Figure 8. Month-to-month variation for THBB .
January February March
0
0.5
1
1.5
2
2.5
Month-to-month variation for rain height
Month of the year ( 2007 )
Rainheight(km)
Figure 9. Month-to-month variation for RH .
These values are in contrast to a constant value of 4.50 km as recommended by ITU-Rec. P. 839-3. The melting
layer heights were observed to steadily increase over the months (1.845 km, 3.250 km, and 4.327 km for
January, February and March respectively). Additionally, the rain heights were found to the fixed at 1.062 km
over the three-month period. Results of this work showed good degree of agreement with some other results
obtained in some other tropical regions.
TABLE II. COMPARISON WITH RESULTS OBTAINED FROM SIMILAR WORKS IN THE TROPICS
Freezing
height
(H0) km
BB bot
Height km
BB height
km
BB
thickness
km
Rain
height (HR)
km
ITU-R P.
839-3 [13]
4.50 4.86
TRMM-
PR [9]
5.00 3.75 4.4 1.25 3.75
Singapore
[19]
5.00 2.00 3.50 3.00 2.00
Kluang
2007 [11]
2.952 2.00 3.961 1.827 1.976
Current
work
5.961 1.845 3.789 3.970 1.062
IV. CONCLUSIONS
The results of the comparison of the evaluation of this processed ground radar data with other similar
work showed a good degree of agreement with most of the measured parameters.
However, the ITU-Rec. P. 839-3 seems to over-estimate the measurements for the mean rain height above sea
level, RH . This may be due to the assumed constant value for the mean 00
C isotherm height above mean sea
level, 0H .
REFERENCES
[1] H. Y. Lam, J. Din, C. Capsoni and A. D. Panagopoulos, “Stratiform and Convective rain
Discrimination for Equatorial Region”, Proceedings of 2010 IEEE SCOReD, pp. 112-116, 2010.
[2] G. O. Ajayi and P. A. Odunewu, “Some Characteristics of the Rain Height in a Tropical Environment,”
IEEE Transactions on Antennas and Propagation, pp. 80-82, 1984.
Determination of Bright Band in Malaysia through Radar Data Analysis
www.ijres.org 39 | Page
[3] E. S. M. Thurai, K Okamoto, “Rain Height Variability in the Tropics and Implications for Rain Scatter
Interference,” IEEE Transactions on Antennas and Propagation, pp. 997-1001, 2005.
[4] N. Takahashi, and J. Awaka, “Introduction of a melting layer model to a rain retrieval algorithm for
microwave radiometers,” Geoscience and Remote Sensing Symposium, IGARSS'05
Proceedings, vol. 5, pp. 3404-3409, 2005.
[5] L. Raymond et al , “Improved Modelling of Propagation and Backscattering of Millimeter waves in the
Melting Layer”, IEEE National Conference on Antennae and Propagation, no. 461, pp. 160-163, 1999.
[6] S. Das and A. Maitra, "Some melting layer characteristics at two tropical locations in Indian region."
General Assembly and Scientific Symposium, 2011 XXXth URSI. IEEE, 2011.
[7] K. Pipis, M. Ioannidou, and D. Chrissoulidis, “Comparison of radar reflectivity calculations to satellite
measurements across the melting layer of precipitation” ,General Assembly and Scientific Symposium,
2011 XXXth URSI IEEE, pp. 1-4, 2011.
[8] J. Tan and J. W. F. Goddard, “The use of dual-polarisation techniques for bright-band detection with
PPI-based radars”, In Radar Meteorology, IEE Colloquium, IET (11), pp. 1-6, 1995.
[9] Khalid Mubara, Ali Dawood and Abdulaziz Al Dosary, “Global Mapping of Height of Bright-band”,
IEEE, 2007.
[10] Merhala Thurai, Eri Deguchi, Toshio Iguchi and Ken’ichi Okamoto, “Freezing height distribution in
the tropics”, International Journal of Satellite Communications and Networking. Vol. 21, pp. 533-545,
2003.
[11] N. H. H. Khamis, O. A. R. Sharif, Z. Hanzaz, and A. Baharom, “Month-to-Month variability of the
Melting Layer Boundaries”, Asia pacific Conference on Applied Electromagnetics Proceedings,
Malaysia, 2007.
[12] J. S. Mandeep, “Rain height statistics for satellite communication in Malaysia," Journal of Atmospheric
and Solar-Terrestrial Physics, vol.70, pp.1617-1620, 2008.
[13] Rain Height Model for Prediction Methods, ITU-R P.839-3, 2001.
[14] W. Klaassen, “Radar observations and simulation of the melting layer of precipitation,” Journal of the
atmospheric sciences, vol. 45, no.24, pp. 3741-3753, 1988.
[15] Frederic Fabry and Wanda Szyrmer, “Modeling of the Melting Layer. Part II:
Electromagnetic”, American Meteorological Society, pp. 3593-3600, 1999.
[16] William Olson et al, “A Melting-Layer Model for Passive/Active Microwave Remote Sensing
Applications. Part I: Model Formulation and Comparison with Observations,” Journal of Applied
Meteorology, vol. 40, no. 7, pp. 1145-1163, 2001.
[17] M. Thurai, and H. Hanado, “Melting layer model evaluation using fall velocity spectra at Ku-band,”
Microwaves”, Antennas and Propagation, IEE Proceedings, vol. 151, no. 5, pp. 465-472, 2004.
[18] J. S. Marshall and, W. M. K. Palmer, “The distribution of raindrops with size”, Journal of meteorology,
vol. 5, no. 4, pp. 165-166, 1948.
[19] E. D. M. Thurai, K. Okamoto and E. Salonen, “Rain height variability in the Tropics,” IEE Proc.-
Microwave Antennas Propagation, vol. 152, no. 1, pp. 17-23, 2005.
Abayomi I. O. Yussuff obtained his bachelor and master’s degrees in Electronic and Computer Engineering
from Lagos State University, Nigeria in 1994 and 2003 respectively. He is currently a full-time
PhD research student of Communications Engineering at Faculty of Electrical Engineering
Department Universiti Teknologi Malaysia (UTM), Skudai, Johor, Malaysia. His research area of
interests includes radio propagation and rain attenuation studies in the tropics, computer security,
electronic instrumentation and measurements. Mr. Yussuff is a member of Nigeria Society of
Engineers (NSE) and IEEE. He is licensed by the Council for Regulation of Engineering in
Nigeria (COREN).
Nor Hisham Haji Khamis is a senior lecturer in the Department Communications Engineering, Faculty of
Electrical Engineering Department, Universiti Teknologi Malaysia, Skudai, Johor. He received his
B.Sc.E.E. from the University of Evansville, Indiana, USA in 1988, M.E.Sc.E.E. from the
University of New South Wales, Australia in 1992, and PhD from UTM in 2005. He joined UTM
in 1989 and currently is the Head of Radar Laboratory. He is also the subject coordinator for the
Microwave Engineering, RF Microwave Circuit Design, and Radar courses at the faculty. He also
leads the Sonar and Marine Instrumentation Research Group (STAR). His research interest includes antenna
design especially microstrip antenna, microwave components, wireless transmission, and propagation studies.
Dr. Khamis is a member of Eta Kappa Nu (Electrical Engineering Honor Society, USA) and IEEE.

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D133439

  • 1. International Journal of Research in Engineering and Science (IJRES) ISSN (Online): 2320-9364, ISSN (Print): 2320-9356 www.ijres.org Volume 1 Issue 3 ǁ July. 2013 ǁ PP.34-39 www.ijres.org 34 | Page Determination of Bright Band in Malaysia through Radar Data Analysis Abayomi I. O. Yussuff1, 2 , Nor Hisham Haji Khamis1 2 Lagos State University, Department of Electronic & Computer Engineering, Lagos, Nigeria 1 Universiti Teknologi Malaysia, Department of Communications Engineering, Skudai, Malaysia Abstract— Restrained usages of X-band and below is mostly due to commercial operations along the slant- path. In tropical regions, signal degradations are often due to hydrometeors such as rain, hail, cloud, and the melting layer. In addition, these can cause several problems, such as signal fading, depolarization and co- channel polarization due to scattering along the satellite link. Inadequate availability of database along the slant- path in tropical regions for use in rain propagation studies at microwave frequencies required more studies to be carried out. This work concerns the characterization of bright band in a tropical station. The effects of seasonal variations on rain height can give the information that are valuable for designing and planning of satellite link in a tropical region like Malaysia. The meteorological radar data for this work was obtained from the Meteorological Department of Malaysia. The result of the analysis of the processed radar data and the obtained parameters for the bright band showed good agreement with works carried out by other researchers in the tropical region. Index Terms— Bright band, Stratiform, Convective, freezing height, 00 C isotherm, RAPIC, PPI, RHI. I. INTRODUCTION For the study of melting layer characteristics, rainfall types are grouped into stratiform and convective. In simple terms, stratiform rains comprise light intensity widespread rainfalls within limited vertical extent of rain height, and are produced by stratus clouds. On the contrary, convective rainfalls are produced by cumulus clouds; with narrow horizontal area and associated with extensive rainfall rates and height [1]. Rain height is generally known to be highly correlated with signal attenuation and co-channel interference due to scattering. The rain height distribution is important because it can be used to investigate the mechanisms responsible for variations in the attenuation distributions at any station. The prediction methods being used to estimate the degree of signal attenuation encompasses the various location-specific meteorological factors, and rain height is one such factor. The rain height, RH is also directly related to the zero degree Celsius isotherm height, 0H . Rain height information can be indirectly obtained by studying the melting layer height in stratiform rain type. One major source of slant-path attenuation prediction errors is the complex nature of the rainfall structure along this path. Another reason is the uncertainty in the estimation of attenuation due to the melting layer. The difficulties in relating RH to 0H in the tropics had also been attributed to insufficient database and peculiar rainfall types existing in the tropical regions [2]. The rain height is being employed in ITU-R Rec. P.618-10 (for slant-path attenuation prediction), ITU- R Rec. P.452-14 (for co-channel interference estimation), ITU-R Rec. P.620-6 (for coordination distances), and ITU-R Radio Regulations Appendix 7 (for regulatory issues of coordination) [3]. The ITU-R Rec. P.618-10 uses the rain height as the boundary below which the slant-path attenuation is integrated while the ITU-R Rec. P.452- 10 uses it to discriminate rain scatter from ice scatter, incorporating variability into the mean freezing height. It uses an effective rain cell model with rain height parameterized vertical dimension, adopting the effective rain height rather than the melting layer’s height. The rain height can be considered to represent the boundary between the rain region and the snow region and it often correspond to the 00 C isotherm (mostly during stratiform rain events). In the vertical dimension, the rainfall rate is assumed to be constant up to the point that represents the top of the rain height and attenuation beyond the height is considered insignificant, and thus neglected [3]. However, recent research has shown that the effect of melting layer on signal attenuation is not after all negligible, especially for weak rain rates [4]. At the 0H , hydrometeors changes from solid to liquid in the melting layer, leading to increase in their reflectivity; manifesting in the bright band signature seen in radar measurements. This band identification is made possible because of its sharp peak of reflectivity in high frequency domain [5-7]. Furthermore, if the
  • 2. Determination of Bright Band in Malaysia through Radar Data Analysis www.ijres.org 35 | Page bright-band was not recognized, it can result in serious over-estimation of precipitation reaching the ground by a factor as high as five [8]. The melting layer is a major factor responsible for the problems being encountered in characterization and modelling of microwave signal propagation. In the absence of actual attenuation measurement data, System Designers are usually compel to rely on rain attenuation models, either for terrestrial or slant-path propagation. This, unquestionably accentuate the importance of modelling in both link budget analysis and equipment designs. Radar Meteorologists define the melting layer as the region where melting occurs, and it lie just below the 00 C isotherm height. The 00 C isotherm is that height at which the ice-to-water transition begins. The variances in the propagation characteristics of ice and water presents an effective boundary referred to as the bright band. The height of the bright band is close to that 00 C isotherm, depending on the season and location of the station of interest [3, 9-12]. The 00 C isotherm, rain and bright band heights most times lie close to each other (see Figure 1), although they represent different parameters [3]. The difference between the effective rain height and the freezing height is taking to be 360 meters according to [13], and is expressed as: kmHHR 36.00  (1) Where RH represents the mean rain height above mean sea level and 0H is the mean 00 C isotherm height above mean sea level. The frozen hydrometeors were observed to show a typical enhancement of radar bistatic reflectivity (dBZ) as they fall through the melting layer, followed by a sharper decrease in reflectivity during the following stages of the melting process [10]. To this effect, several researchers have developed and proposed quite a handful of models for predicting attenuation in the melting layer [4, 14-17]. Figure 1. Bright band Conceptual Model. II. METHODOLOGY The meteorological radar data for this work was obtained from the Meteorological Department of Malaysia. The analysis undertaken here is for a 62 km range from Kluang radar station (lat. 2.020 N, long. 103.380 E) to Faculty of Electrical Engineering (FKE), Universiti Teknologi Malaysia (lat. 1.560 N, long. 103.640 E). The azimuth from Kluang to FKE was evaluated to be 1690 . The data duration spans thirteen months (November 2006 to November 2007). However, this preliminary data analysis is based on data samples from January to March 2007. The classification of the rain events is evaluated with the minimum amount of the rain rate that the radar can detect; confirmed by using the widely accepted empirical relationship of the radar reflectivity factor Z, and rainfall rate R, that is given by b aRZ  (mm6 m-3 ) (2) Where the most common values for a and b are 200 and 1.6 respectively, according to Marshall-Palmer [18]. These are also the values used by the radar operators at the Malaysian Meteorological Department of Malaysia. This system uses the 3D RAPIC system and two modes of scans - The plan position indicator (PPI) and range height indicator (RHI). The specification of the Kluang radar is given in Table I.
  • 3. Determination of Bright Band in Malaysia through Radar Data Analysis www.ijres.org 36 | Page TABLE I. KLUANG RADAR SPECIFICATIONS [11] For PPI scan there are 15 volumetric elevation angles, 0.5°, 1.2°, 1.9°, 2.7°, 3.5°, 4.6°, 6.0°, 7.5°, 9.2°, 11.0°, 13.0°, 16.0°, 20.0°, 25.0°, and 32.0°. The radar image of each of these selected angles was recorded through the full RHI's azimuthal scan range of 360°. The elevations angles used in this work are 1.1°, 1.9°, 3.3°, 5.8°, 7.7°, 10.3°, 13.6°, and 18.1°. The parameters of the melting layer are obtained from the detected bright band signature, after series of processing that include, but not limited to, various levels of sorting, filtering and decoding to build the vertical profile of reflectivity of the bright band. III. RESULTS AND DISCUSSIONS The vertical profile of reflectivity for the months of January, February and March 2007 are displayed in Figures 1-3 respectively. Table II compares the results of measurements with those obtained by other researchers that were also carried out in other tropical stations and the ITU-Rec. P. 839-3. The ITU-Rec. P. 839-3 largely over-estimated the measurements for the rain heights. Significant changes were observed in the month-to-month data for the freezing heights, from 5.815 km, 4.327 km, to 7.742 km for the months of January, February and March respectively. 0 5 10 15 20 25 0 2000 4000 6000 8000 10000 12000 Radar reflectivity ( dBz ) Height(m) Figure 2. VRP plot for January 2007 for Kluang, Malaysia. 5 10 15 20 25 30 35 0 2000 4000 6000 8000 10000 12000 Radar reflectivity ( dBz ) Height(m) Figure 3. VRP plot for February 2007 for Kluang, Malaysia.
  • 4. Determination of Bright Band in Malaysia through Radar Data Analysis www.ijres.org 37 | Page 0 5 10 15 20 25 30 0 2000 4000 6000 8000 10000 12000 Radar reflectivity ( dBz ) Height(m) Figure 4. VRP plot for March 2007 for Kluang, Malaysia. The month-to-month variations in freezing heights, bright band heights, bright band thickness and rain heights are shown in Figures 6-9 respectively. Malaysia experiences two monsoon events yearly. These are the North-East (October to March) from the South China Sea and South-West monsoon (April to September) from the Indian Ocean. This results in two rainy and two dry seasons. 0 5 10 15 20 25 0 2000 4000 6000 8000 10000 12000 Radar reflectivity ( dBz ) Height(m) Figure 5. Mean VRP plot for January - March 2007 for Kluang, Malaysia. January is the end month of the North-East monsoon rain and the start of the dry season, while March is the end of the North-East monsoon dry season and the beginning of the South-West monsoon rainy season. January February March 0 1 2 3 4 5 6 7 8 Month of the year ( 2007 ) Zerodeg.celciusheight(km) Month-to-month variation for freezing height Figure 6. Month-to-month variation for 0H . January February March 0 0.5 1 1.5 2 2.5 3 3.5 4 4.5 Month-to-month variation for BB height Month of the year ( 2007 ) BBHeight(km) Figure 7. Month-to-month variation for HBB .
  • 5. Determination of Bright Band in Malaysia through Radar Data Analysis www.ijres.org 38 | Page January February March 0 0.5 1 1.5 2 2.5 3 3.5 4 4.5 5 Month-to-month variation for BB thickness Month of the year ( 2007 )BBthicknessHeight(km) Figure 8. Month-to-month variation for THBB . January February March 0 0.5 1 1.5 2 2.5 Month-to-month variation for rain height Month of the year ( 2007 ) Rainheight(km) Figure 9. Month-to-month variation for RH . These values are in contrast to a constant value of 4.50 km as recommended by ITU-Rec. P. 839-3. The melting layer heights were observed to steadily increase over the months (1.845 km, 3.250 km, and 4.327 km for January, February and March respectively). Additionally, the rain heights were found to the fixed at 1.062 km over the three-month period. Results of this work showed good degree of agreement with some other results obtained in some other tropical regions. TABLE II. COMPARISON WITH RESULTS OBTAINED FROM SIMILAR WORKS IN THE TROPICS Freezing height (H0) km BB bot Height km BB height km BB thickness km Rain height (HR) km ITU-R P. 839-3 [13] 4.50 4.86 TRMM- PR [9] 5.00 3.75 4.4 1.25 3.75 Singapore [19] 5.00 2.00 3.50 3.00 2.00 Kluang 2007 [11] 2.952 2.00 3.961 1.827 1.976 Current work 5.961 1.845 3.789 3.970 1.062 IV. CONCLUSIONS The results of the comparison of the evaluation of this processed ground radar data with other similar work showed a good degree of agreement with most of the measured parameters. However, the ITU-Rec. P. 839-3 seems to over-estimate the measurements for the mean rain height above sea level, RH . This may be due to the assumed constant value for the mean 00 C isotherm height above mean sea level, 0H . REFERENCES [1] H. Y. Lam, J. Din, C. Capsoni and A. D. Panagopoulos, “Stratiform and Convective rain Discrimination for Equatorial Region”, Proceedings of 2010 IEEE SCOReD, pp. 112-116, 2010. [2] G. O. Ajayi and P. A. Odunewu, “Some Characteristics of the Rain Height in a Tropical Environment,” IEEE Transactions on Antennas and Propagation, pp. 80-82, 1984.
  • 6. Determination of Bright Band in Malaysia through Radar Data Analysis www.ijres.org 39 | Page [3] E. S. M. Thurai, K Okamoto, “Rain Height Variability in the Tropics and Implications for Rain Scatter Interference,” IEEE Transactions on Antennas and Propagation, pp. 997-1001, 2005. [4] N. Takahashi, and J. Awaka, “Introduction of a melting layer model to a rain retrieval algorithm for microwave radiometers,” Geoscience and Remote Sensing Symposium, IGARSS'05 Proceedings, vol. 5, pp. 3404-3409, 2005. [5] L. Raymond et al , “Improved Modelling of Propagation and Backscattering of Millimeter waves in the Melting Layer”, IEEE National Conference on Antennae and Propagation, no. 461, pp. 160-163, 1999. [6] S. Das and A. Maitra, "Some melting layer characteristics at two tropical locations in Indian region." General Assembly and Scientific Symposium, 2011 XXXth URSI. IEEE, 2011. [7] K. Pipis, M. Ioannidou, and D. Chrissoulidis, “Comparison of radar reflectivity calculations to satellite measurements across the melting layer of precipitation” ,General Assembly and Scientific Symposium, 2011 XXXth URSI IEEE, pp. 1-4, 2011. [8] J. Tan and J. W. F. Goddard, “The use of dual-polarisation techniques for bright-band detection with PPI-based radars”, In Radar Meteorology, IEE Colloquium, IET (11), pp. 1-6, 1995. [9] Khalid Mubara, Ali Dawood and Abdulaziz Al Dosary, “Global Mapping of Height of Bright-band”, IEEE, 2007. [10] Merhala Thurai, Eri Deguchi, Toshio Iguchi and Ken’ichi Okamoto, “Freezing height distribution in the tropics”, International Journal of Satellite Communications and Networking. Vol. 21, pp. 533-545, 2003. [11] N. H. H. Khamis, O. A. R. Sharif, Z. Hanzaz, and A. Baharom, “Month-to-Month variability of the Melting Layer Boundaries”, Asia pacific Conference on Applied Electromagnetics Proceedings, Malaysia, 2007. [12] J. S. Mandeep, “Rain height statistics for satellite communication in Malaysia," Journal of Atmospheric and Solar-Terrestrial Physics, vol.70, pp.1617-1620, 2008. [13] Rain Height Model for Prediction Methods, ITU-R P.839-3, 2001. [14] W. Klaassen, “Radar observations and simulation of the melting layer of precipitation,” Journal of the atmospheric sciences, vol. 45, no.24, pp. 3741-3753, 1988. [15] Frederic Fabry and Wanda Szyrmer, “Modeling of the Melting Layer. Part II: Electromagnetic”, American Meteorological Society, pp. 3593-3600, 1999. [16] William Olson et al, “A Melting-Layer Model for Passive/Active Microwave Remote Sensing Applications. Part I: Model Formulation and Comparison with Observations,” Journal of Applied Meteorology, vol. 40, no. 7, pp. 1145-1163, 2001. [17] M. Thurai, and H. Hanado, “Melting layer model evaluation using fall velocity spectra at Ku-band,” Microwaves”, Antennas and Propagation, IEE Proceedings, vol. 151, no. 5, pp. 465-472, 2004. [18] J. S. Marshall and, W. M. K. Palmer, “The distribution of raindrops with size”, Journal of meteorology, vol. 5, no. 4, pp. 165-166, 1948. [19] E. D. M. Thurai, K. Okamoto and E. Salonen, “Rain height variability in the Tropics,” IEE Proc.- Microwave Antennas Propagation, vol. 152, no. 1, pp. 17-23, 2005. Abayomi I. O. Yussuff obtained his bachelor and master’s degrees in Electronic and Computer Engineering from Lagos State University, Nigeria in 1994 and 2003 respectively. He is currently a full-time PhD research student of Communications Engineering at Faculty of Electrical Engineering Department Universiti Teknologi Malaysia (UTM), Skudai, Johor, Malaysia. His research area of interests includes radio propagation and rain attenuation studies in the tropics, computer security, electronic instrumentation and measurements. Mr. Yussuff is a member of Nigeria Society of Engineers (NSE) and IEEE. He is licensed by the Council for Regulation of Engineering in Nigeria (COREN). Nor Hisham Haji Khamis is a senior lecturer in the Department Communications Engineering, Faculty of Electrical Engineering Department, Universiti Teknologi Malaysia, Skudai, Johor. He received his B.Sc.E.E. from the University of Evansville, Indiana, USA in 1988, M.E.Sc.E.E. from the University of New South Wales, Australia in 1992, and PhD from UTM in 2005. He joined UTM in 1989 and currently is the Head of Radar Laboratory. He is also the subject coordinator for the Microwave Engineering, RF Microwave Circuit Design, and Radar courses at the faculty. He also leads the Sonar and Marine Instrumentation Research Group (STAR). His research interest includes antenna design especially microstrip antenna, microwave components, wireless transmission, and propagation studies. Dr. Khamis is a member of Eta Kappa Nu (Electrical Engineering Honor Society, USA) and IEEE.