Open access

The Role of DSD and Radio Wave Scattering in Rain Attenuation

Written By

Ondrej Fiser

Published: 01 February 2010

DOI: 10.5772/9110

From the Edited Volume

Geoscience and Remote Sensing New Achievements

Edited by Pasquale Imperatore and Daniele Riccio

Chapter metrics overview

3,457 Chapter Downloads

View Full Metrics

1. Introduction

The (rain) drop size distribution (DSD) plays a very important role in meteorology (determination of radar reflectivity and consequently rain rate, classification of precipitation, flood prediction), in microwave radio-communication (determination of rain attenuation) and also in many other applications like agriculture and insurance business.

1.1. Quick overview of literature

There is a large number of papers devoted to the DSD problems. The classical and very important study by Marshall-Palmer (1948) has to be mentioned. Almost every scientist is using this DSD model for average rain. Rain intensity is a parameter of this DSD.

The most important recent papers concerning the DSD problem are focused on following topics:

Carolin Richter (1995) declared the Gamma function to be an appropriate analytical approximation of DSD. She has studied the dependence of rain rate, median diameter and shape factor (μ-parameter in Gamma approximation) on synoptic events. Clear systematic trends in the drop spectra were found. It was possible to distinguish warm advection from the cold advection according to the numerical value of the shape factor μ. Carolin has also found that the rain intensity does not influence the shape of DSD as no relation between rain rate and shape factor could be found.

Albert Waldvogel (1974) discussed the intercept parameter No in the exponential approximation of DSD. Prof. Waldvogel has found that sudden variations of spectra can be recognised easily as No jump versus the time axis. An empirical model is proposed for the relation between the type of raindrop spectra and the convective activity of the precipitating mass.

Tokay A. and Short D. (1996) have observed dramatic change in the intercept parameter No in the Gamma approximation of DSD occurring during rainfall events with little change in rainfall rate. It can correspond to the transition from rain of convective origin to rain originating from the stratiform portion of tropical systems. The authors have presented an empirical stratiform-convective classification method based on No and rain rate scatterplot. It is worth noting that this study is related only to tropical rains.

J. Joss and E. Gori (1978) have defined an “integral” shape factor of DSD different from the “μ” shape factor, which is a parameter in the Gamma approximation. They discussed the role of sampling time on the shape factor founding that adding many instant distributions from different conditions leads to an exponential distribution such as proposed by Marshall and Palmer (1948).

J. Joss and A. Waldvogel (1968) have modified the Marshal-Palmer DSD for drizzle, continuous rain, shower and thunderstorm for conditions of Switzerland. This modification cannot be accurate because it is based on short term DSD measurement.

O.Fišer and M. Hagen (1998) have discussed the influence of integration time on resulting DSD. For larger integration time the increasing agreement between experimental DSD and its exponential distribution was shown. Also variations of parameters defining DSD (No,λ and μ) with rain rate was illustrated and discussed. Two methods to determine parameters of analytical DSDs were shown and discussed (linear regression, method of moments).

O.Fišer, D.Řezáčová,P.Pešice, Z.Sokol and O.Školoud (1998) realised an attempt to estimate the basic rain type from existing rain rate records using the rain event duration, rain amount, average and standard deviation of rain rate as predictors.

O. Fišer (2002b) discussed the role of particular rain drop size on resulting specific rain attenuation im micro and mm frequency bands.

O. Fišer (2003 a,b) compared existing methods for meteorological rain type identification using Czech DSD data. A lot of work has to be done because existing criterions were devoted for tropical regions only and the mentioned study has an introductory meaning.

O. Fišer (2004) derived the radar reflectivity-rain intensity (Z-R) analytical approximation using the Czech DSD data.

O. Fišer (2006) has published a preliminary study showing DSD variability and its frequency dependence.

O. Fišer (2007) analysed the DSD moments for the estimation of the bilateral relationships between DSD products (outputs).

Jameson, A. R., A. B. Kostinski (2002) have found power law relation between rain rate and radar reflectivity factor. It is found that apparently realistic but spurious nonlinear power-law relations still appear among rainfall parameters even though the rain is not only statistically homogeneous but purely random as well.

Řezáčová D., Kašpar M., Novák P., Setvák M., (2007) have published an overview of published and measured DSDs of of rain (Best,Marhall-Palmer and other distributions).


2. Drop size distribution

The rain drop size distribution (DSD, quantity symbol N) represents the probability density of equivolumetric drop diameter D being in the unity volume. The product N(D) dD gives the number of rain of the diameter between D and D+dD in the unity volume. Only rain drops of diameters below 7 mm can exist for physical reasons. Example of the DSD measured in the Czech Republic is shown in Figure 1

Figure 1.

DSD measured in Czech Republic (one year measurement, rain rate is the parameter of particular curves).


3. DSD measurement

Generally speaking, the measurement of the DSD is relatively rare. The greatest problem is the cost of distrometer. The most developed and user friendly device for the DSD measurement is a videodistrometer (videodistrometers developed at the Graz Technical University, Austria under ESA contract, are well known). Other electromechanical distrometer of the Joss-Waldvogel type, is used at the ETH Zurich and in Bavaria (in the DLR-Oberpfaffenhofen and in the DWD-Hohenpeissenberg). Optical distrometers are or were used in Oberpfaffenofen and in Dubna (Russia). The Rutherford Appleton Laboratory (UK), has performed a DSD measurement in Chilbolton (UK) and in Papua New Guinea. On the other hand, there is a lot of DSD data which is not processed or which is processed only partially.

The DSD measurement is not very simple and it is not performed so often in comparison with the rain rate measurement. Several DSD measurements were performed in the history (e.g. Marshall and Palmer, 1948, Joss and Waldvogel, 1968, Lakomá, 1971, Federer and Waldvogel, 1975, Li and Zhang, 1980) or more recently (e.g. Doelling et al., 1996, Hubert et al., 1999, Tokay et al., 1999, Tokay et al., 2002, Schönhuber et al., 2000, Bringi et al.,2003) using different types of measurement technique (filter or glass catchment, electromechanical distrometer, optical distrometer, videodistrometer and others). Many DSD measurements have been made by the electromechanical distrometer the concept of which was developed by Joss and Waldvogel (e.g. Joss and Waldvogel, 1967).

The results of the Czech DSD measurement (performed in 1998-1999) was published by Fišer et al.,2002, Fišer, 2002b and Fišer, 2004.


4. Analytical approximations of DSD

The exponential and Gamma distribution are the most frequently used analytical approximations of the DSD because of their satisfactory correspondence with the typical drop size distribution shape in the majority of experimental samples. There are also many other DSD models in the literature - for instance the log-normal model (Ajayi, Kozu, 1999). It should be remaindered that also many various factors like the rain type, time of integration and others influence the analytical DSD modelling.

The equation (1) expresses the Gamma model of distribution function (DSD)

N ( D ) = N 0 D μ exp ( λ D ) E1


D [mm] is the rain drop diameter

N(D) [m-3 mm-1-μ] is the number of drops per unit volume per drop diameter interval (dD)

N0 [m-3mm-1-μ] is the intercept parameter of DSD

λ [mm-1] is the slope parameter.

μ [-] is shape of the DSD, to avoid a mismatch it is preferred to call it as “μ parameter”

Examples of numerical values of parameters are shown in Table 1 (Iguchi T., 1999) and plotted in Figure 2.

Gamma N o ( ( Rain type mm-3-(m-3 mm-1 - Convective 6.29E5*R-0.416 8.35R-0.185 3 Stratiform 2.57E4*R0.012 5.5R-0.129 3
Rain type mm-3- m-3 mm-1 -
Convective 6.29E5*R-0.416 8.35R-0.185 3
Stratiform 2.57E4*R0.012 5.5R-0.129 3

Table 1.

Examples of numerical values of the Gamma DSD model parameters (tropical region) where R is the rain rate in [mm/h].

Figure 2.

Gamma DSD model using parameters from Table 1 for certain rain rate value.

The simpler Exponential distribution is used in the form given by the following expression

N ( D ) = N 0 exp ( λ D ) E2

As it is obvious, the exponential DSD model can be considered as a special case of the gamma DSD where the parameter μ equals to zero.

The parameter λ in this model can be also expressed in the dependence on rain rate R:

λ a R b E3

where b=-0,21.

Typical exponential DSD for various rain types (drizzle, thunderstorm and average rain in mild climate) is shown in Figure 3, which is plotted after Table 2. (source: Joss J. and Waldvogel A., 1968).

Rain type N o
mm -1 m -3 mm -1
Thunderstorm or shower 1 400 3 * R -0.21
Continuos rain 7 000 4.1*R -0.21
Drizzle 30 000 5.7*R -0.21
Average rain 8 000 4.1*R -0.21

Table 2.

Typical parameters of Exponential DSD model (Europe) where R is the rain rate in [mm/h].

Figure 3.

Exponential DSD for various rain types (drizzle, thunderstorm and average rain in mild climate).


5. Determination of DSD parameters from measured values

In this part we describe two techniques determining the values of the model parameters N0, λ, and μ. After logarithmic linearization of the N(D) approximation (1) the linear regression can be applied (least square method, Bartsch, 1996). The moment method uses the definition of the DSD moments, which, for the n-th moment, Mn, gives:

M n = 0 D n N ( D ) d D E4

Using the method of moments following formulas for the parameters No and λ in the exponential DSD model (2) were derived:

N o = 98.65 * M 3 * ( M 3 M 6 ) 4 3 E5
λ = 4.93 * ( M 3 M 6 ) 1 3 E6

where M3, and M6 are the 3rd, and 6th DSD moments, respectively. Note that the same formulas were derived by Prof. Waldvogel (Waldvogel, 1974) where the liquid water content W was preferred to the 3rd moment. The third and the sixth moments were chosen to approximate the DSD in order to determine the rain intensity (being approximately proportional to M3) and the radar reflectivity factor (proportional to M6) from the DSD model as accurate as possible.

To determine the parameters of the Gamma approximation (1) the formulas of Tokay and Short (Tokay, Short, 1996) can be used. The expressions using M3, M4, and M6 are as follows:

μ = 11 G 8 + [ ( G ( G + 8 ) ] 1 / 2 2 ( 1 G ) E7
λ = ( μ + 4 ) M 3 M 4 E8
N 0 = λ μ + 4 M 3 Γ ( μ + 4 ) E9

where the auxiliary G factor is given by

G = M 4 3 M 3 2 * M 6 E10

6. Outputs (products) of DSD

The rain drop size distribution (some times it is called “rain drop spectrum”) determines uniquely its outputs (outputs can be called also “products”) as rain rate, radar reflectivity factor, rain attenuation and others (see next parts).

6.1. DSD products of no frequency dependence

a, Rain intensity (rain rate)

R g = 3 . 6 1 0 3 π 0 D 3 v ( D ) N ( D ) d D E11

where Rg [mm/h] is the rain rate (corresponding to the rain rate derived from rain gauge measurement)

v is the terminal falling velocity

N(D) is the drop size distribution

D is the equivolumetric drop radius.

b, Radar reflectivity factor z [mm6m-3]

The radar reflectivity factor z (small letter “z”) is the 6th DSD moment, it can be computed from following expression:

z = 0 D 6 N ( D ) d D E12

while for its logarithmic unit Z [dBZ] (capital letter “Z”) it is used:

Z = 10 log 10 z = 10 log 10 { 0 D 6 N ( D ) d D } E13

If we study electromagnetic energy coming back from rain volume to the radar, we must be aware that the reflected energy is not dependent on frequency only in the “Rayleigh region“ case (drop diameter D is much smaller in comparison with the wave length λ, i.e. D<< λ), more precisely the Rayleigh region is defined

πD/λ <<1 for n =1 (n is the refractive index.) or πnD/λ <<1 for n > 1

If we suppose rain with rain drops having diameter up to 4 mm (typical for mild climate), the Rayleigh region holds for frequencies below 2,5 GHz. But if we consider the existence of maximum rain drop diameter (D=7 mm), the Rayleigh region is met at frequencies lower than 1,36 GHz. In practice, it is not so strict and the Rayleigh region is applicable for frequencies below 5 GHz.

6.2. DSD products dependent on frequency

The specific rain attenuation A is strongly dependent on frequency, but rain attenuation is negligible for frequencies below 4 GHz.

For the specific rain attenuation A in [dB/km] next equation is used:

A = 4 , 343 10 3 λ Im f ( D ) N ( D ) d D E14

where f is the complex forward scattering function (for exact definition see in part 7)

λ is the wave length of the used transmission

Im represents the imaginary part of complex number

The formula (14) is derived in part 9. As one can see, this expression strongly depends on the wave length λ (i.e. frequency) in contrast to the no frequency dependence of the radar reflectivity factor.

Through the numerical simulations it is possible to search for relationships between mentioned quantities (Z, R and A) called “DSD products.” The term frequency means the radio frequency of pertinent technical application in this paragraph.


7. Scattering functions

In literature different definitions of scattering functions are used, see, for instance [Uzunoglu et al., 1977]. One of the most used definition of the scattering function is the following one:
E s = E i f ( K 1 , K 1 ) r 1 e ( j k 0 r ) E15


E s ... electric field of a scattered wave [V/m] E i ... electric field of a wave impressing on the raindrop [V/m] k 0 ... free space propagation constant [m-1]

r.... observation distance from the scattering drop [m]

f ( K 1 , K 2 ) ... scattering function [m], K 1 is the direction of the incident field, K 2 is the direction of the scattered field


if K1=K2, the forward scattering function is considered, orif K1= - K2, the backward scattering function is considered

If the propagating radio wave direction is not parallel with horizontal drop axis, formula (16) can be used (see geometry in Figure 4).

Figure 4.

Geometry of forward propagation direction in the general incidence angle α.

f h,v ( α ) f 0 ( 0 ° ) cos 2 ( α ) + f h,v ( 90 ° ) sin 2 ( α ) E16


α is angle between direction of propagation and zenith axis [ ]

f h,v ( 90 ° ) is the scattering function of horizontally respective vertically polarised wave for direction of propagation parallel with horizontal drop axis (α = 90o) f 0 ( 0 ° ) is scattering function for the “zenith” propagation (α = 0o), it is not dependent on polarisation because of rain drop symmetry

8. Some methods computing scattering functions

8.1. Rayleigh scattering

The Rayleigh scattering theory was developed and published by Strutt (1871a,b) – later Lord Rayleigh. The theory gives an approximation for the scattering of electro-magnetic radiation from spheres. It is valid for sphere diameters significantly smaller than the vacuum wavelength of the radiation., i.e. πD/λ <<1, see part 6.1. Lord Rayleigh derived a scattering function approximation for such case using elementary dipole theory.

The computation of the Rayleigh scattering is very simple (a handy calculator is sufficient) but we must be aware of strict limitations. It was proved that the frequency above about 5 GHz is owing to the usual rain drop diameter out of Rayleigh region.

The Rayleigh scattering helps us to study the frequency and temperature properties of attenuation on lower frequencies. It does not enable to compute depolarisation and angular dependencies.

8.2. Mie scattering

The Mie scattering theory was developed and published by Mie (1908 ). The scattering function f (subscript “f” for forward, “b” for backward scattering) for spherical dielectric particles is given by the next formula:

f f = j λ 3 π 3 D 2 [ n = 1 ( 2 n + 1 ) ( a n + b n ) ] * f b = j λ 3 π 3 D 2 [ n 1 ( 1 ) ( n + 1 ) ( 2 n + 1 ) ( a n b n ) ] * E17

where λ denotes the vacuum wavelength of the electro-magnetic radiation, j is the imaginary unit and D the diameter of the spherical drops, * is symbol for conjugate imaginary numbers. The coefficients an and bn according to Mie depend on the complex relative refractivity εr = ε / ε0 of the material (rain water in our case) and on the diameter D of the scattering sphere.

an, bn are the Mie’s coefficient, its evaluation need not to be very complicated.

The Mie scattering calculation is also possible at this web page:

For the Mie scattering computation a simple programmable computer is needed under the condition that it can work with complex variables. The Mie algorithm can be quite simple if the Bessel and Legandre polynomials were replaced by simple complex goniometric functions. The infinite series (the above printed formula) can be limited to the n being about 10 (or even less) of a perfect accuracy, see (Fiser, O., 1993).

Mie scattering helps us to study the frequency and temperature properties of rain attenuation if we accept that rain drop shape is spherical (for larger rain drops it is not true). Mie scattering does not enable to compute depolarisation and angular dependencies. On the other hand, there is no frequency limitation like in the Rayleigh scattering computation case.

8.3. Other methods computing scattering functions

For full utilisation (angular dependence, polarisation properties), numerical methods computing the scattering functions, are required.

The point matching method is much more complicated and general and it enables to study not only the properties of scattering functions but also the incident angle dependence, the bi-static scattering and depolarization phenomena as well. See, for instance Oguchi, T., 1973.

Some studies to derive the scattering function using numerical methods are used. For instance the MultipleMultiPole (MMP) method was used by Hajny, Mazanek and Fiser at the Czech Technical University Prague, cf. Hajny, M. et al, 1998.


9. Derivation of formula for specific rain attenuation in rain volume

To derive a formula for specific rain attenuation we prepared next collection of formulas related to the Figure 5 (Es is scattered field, Ei is incident field, E0 is “free space” field, z1->0 (infinitesimal length of the rain volume between two parallel slabs), resulting electrical field is summed at the point P(zo) - contributions of the original free space field E0 and scattered field from rain drops in the thin rain volume. Incident wave is of the planar type in our model (a very good approximation of spherical wave being very far from the transmitter). Here are the formulas:

Resulting electrical field E(zo) [V/m] is a sum of free space field and scattered field:

E ( z o ) = E s ( z o ) + E o ( z o ) E18

From the definition of scattering functions we have:

E s ( z o ) = E i ( z ) f ( D ) e j k r r E19

For planar wave it is valid:

E i ( z ) = E i ( 0 ) e j k z E20

Figure 5.

On specific rain attenuation.

After some numerical simplifications

E s ( z o ) ~ E i ( 0 ) f ( D ) e j k r r E21
E s ( z o ) ~ E o ( z o ) f ( D ) e j k ( r z o ) z o E22
E o ( z o ) = E i ( 0 ) e j k z o E23
r = ( ρ 2 + z o 2 ) 0.5 ~ z o ( 1 + 1 2 ρ 2 z o 2 ) E24
r z o ~ ρ 2 2 z o E25

we obtain:

E ( z o ) = E o ( z o ) + E o ( z o ) 0 { 0 z 1 f ( D ) N ( D ) I d z } d D E26


I = 0 π { 0 F ρ e j p ρ 2 d ρ } d ϕ E27

and where F is the radius of the first Fresnel zone. This integral expresses the contributions of all rain drops in the infinite plane perpendicular to the direction of radiowave propagation. In fact, the contribution is considered from ashlar of the infinitesimal length in the direction of propagation (z axis in our picture):

E ( z o ) = E o ( z o ) [ 1 + j 2 π k o z 1 C ] E28


C = 0 f ( D ) N ( D ) d D E29


τ = { lim Δ z 0 ( 1 + j 2 π k o Δ z C ) 1 Δ z } L = e j 2 π k o C L E30


τ is the ratio of the attenuated field strength to the non attenuated one (transmission)

f is the complex scattering function

Transmission τ was computed as a product of a number of (L/Δz) ashlars of infinitesimal lengths arranging in the series of the certain length L. The formula for specific rain attenuation α in the [dB/km] unit is then given as 10 log10(τ):

α = 4.3434 λ 10 3 0 Im f ( D ) N ( D ) d D [ d B / k m ] E31

The next parametrical approximation for the drop size distribution – DSD (symbol N) after Marshall-Palmer is used very frequently for so called “average rain:”

N ( D , R ) = 8000 e 4.1 D R 0.21   [ m m 1 m 3 ] E32

where R is rain rate (or rain intensity) in [mm/h] units and D is equivolumetric rain drop diameter, see Marshall and Palmer, 1948. The same formula (31) was derived through similar way by Van de Hulst (1957).

The mostly used and very simple approximation for specific rain attenuation is this one:

α ~ a R b [ d B / k m ] E33
where a [k alternatively] and b [α alternatively] are constants depending on frequency, polarisation and temperature. An example is shown in next table (ITU-R report):

10. Variability of DSD

The majority of existing models estimating the radar reflectivity or microwave attenuation from rain intensity are rough ones (equations 33 or 34) because they are neglecting the DSD variability. By other words: two various rain events (shower and continuous rain, for instance) of the same rain intensity, say we 5 mm/h, can cause namely different numerical value of rain attenuation through the DSD variability (3 dB/km in shower and 2 dB/km in continuous rain in our example).

The radar reflectivity factor as well as the specific rain attenuation (of the radar signal, or of the microwave and mm wave link) depend on the rain rate only roughly. They both depend on the drop size distribution (DSD) primarily; this fact is frequently neglected (see equations 12, 13 and 14).

The DSD variability is obvious from Figure 6. This figure shows the probability density of the radar reflectivity factors computed through the equations 12 and 13 from measured DSDs corresponding to rain rates between 4.5 and 5.5 mm/h. After the usually used Marshal Palmer relation

Z = 1 0 log ( 3 00  R 1 . 5 )     [ dBZ ]   E34.1

the radar reflectivity factor would be 35,3 dBZ, but one can see, that Z varies from 27 to 42 dBZ (radar would announce rain rate between 1 and 6 mm/h in this case!)

Figure 6.

Radar reflectivity factor histogram corresponding to the rain rate between 4.5 and 5.5 mm/h.

A big dispersion of rain rate values R corresponding to the observed values of the radar reflectivity factor Z is also obvious from scatterplots (Figure 7). Again, it is due to the DSD variability.

Figure 7.

Scatterplot of the R-Z relation (DSD data and equations 11 and 13 were used while integraion time being 1 minute).

Similar scatterplots “attenuation versus rain rate” were done considering frequencies in the 10 - 100 GHz region. A big dispersion is observed, too, but the dispersion depends on the frequency of radio communication link. It was found that the rain attenuation at frequencies close to 40 GHz depends on the rain rate quite uniquely.

In Figure 8 there are shown imaginary parts of forward scattering functions being responsible for the specific rain attenuation (cf. equation 3). It is obvious, that the slope is varying with the frequency.

Figure 8.

Imaginary parts of forward scattering functions being proportional to the rain attenuation.

Through the mathematical regression we have found the exponent “n” in the approximate relationship

Im f  ~   D n                   E34.2

By other words it means that the specific rain attenuation A is approximately proportional to the n-th DSD moment Mn (see equation 4) while “n” varies with the frequency f (unfortunately, there is used the same symbol “f” for both, frequency as well as for scattering function in the technical literature). The found exponent “n” for frequencies between 10 and 100 GHz is shown in Figure 9. Its value is decreasing with the frequency of the radio transmission.

Figure 9.

Exponent “n” in the Im f ~ Dn dependence, where D is rain drop diameter.

After some speculations it could be concluded that the DSD variability courses the measure of the correspondence (uncertainty) between one DSD product (Z,R and A) to another one, for instance the Z –R relation.

It is known that the rain rate is given by the 3.67th DSD moment. As the exponent “n” in equation 34 approximates the 3.67 value in the case of frequencies within the 18 – 42 GHz interval, the A – R relationship is quite unique for this frequency range. On the other hand, the 10 GHz specific rain attenuation approximates the 4.5th DSD moment, which is not very far from the 6th moment, i.e. from the radar reflectivity factor Z (equation 13). That’s why the DSD variation does not very influence the A – Z relation in the 10 GHz case and this relationship is not so ambiguous.

The particular contribution of rain drops of certain diameters to the rain attenuation (after equation 14) is varying considering varying frequency. More concretely: the role of small rain drops is increasing with the frequency. The prevailing contribution is caused by drops of the equivolumetric diameter close to 0.7–1.5 mm (see Figure 10)

Figure 10.

Contribution of rain drops of diameter D to the specific rain attenuation; transmission frequency is a parameter.

All results in this contribution were derived from the actual drop size distributions measurement performed by the videodistrometer of ESA, which was lent to the Institute of Atmospheric Physics Prague through its manufacturer Joaneum Research Graz (Austria) in the period July 1998–July 1999 [Fiser et al., 2002]. The time of integration was chosen to be 1 minute.

11. Conclusion

The applicability, importance and properties of the rain drop size distribution was demonstrated in this chapter. It was also shown that DSD determines rain rate, radar reflectivity and rain attenuation of microwave signal. A part of this chapter describes scattering functions describing radiowave reflection from rain drop.

One of the important results of this study is the following one: the radar reflectivity factor derived from the rain rate through the Z-R relation could be incorrect through the DSD variability. It is due to the fact, that the radar reflectivity is given by the 6th DSD moment while the rain rate depends on 3.67th DSD moment. A bigger rain drop contributes thus much more to the radar reflectivity than to the rain rate.

The rain attenuation at 10 GHz depends on the radar reflectivity factor quite uniquely and similarly the dependence of 42 GHz rain attenuation on the rain rate is unambiguous. For other relationships between DSD products we recommend the utilisation of the dependence of one DSD product on two other DSD products (or DSD moments), for instance to estimate the specific rain attenuation from both rain rate and radar reflectivity factor.


This contribution was thankfully supported by the GACR grant 102/08/0851.


  1. 1. Ajayi G. O. Kozu T. 1999 Rain drop size distribution during convective rainfall in Japan and Nigeria. Proc. of Abstracts, GA URSI, FP37.
  2. 2. Bartsch H. J. 1996 “ Mathematische Formeln,” FINIDR Press.
  3. 3. Bringi V. N. Chandrasekar V. Hubbert J. Gorgucci E. Randeu W. L. Schönhuber M. 2003 "Raindrop Size Distribution in Different Climatic Regimes from Disdrometer and Dual-Polarized Radar Analysis" Journal of Atmospheric Sciences, 60 2003, 2 354 365 .
  4. 4. Bringi V. N. Thurai M. Nakagawa K. Huang G. J. Kobayashi T. Adachi A. Hanado H. Sekizawa S. 2005 “Rainfall Estimation from C-Band Polarimetric Radar in Okinawa, Japan: Comparison with 2-D Video Disdrometer and 400 MHz Wind Profiler" 32nd Conference on Radar Meteorology, 22-29 October 2005, Albuquerque, Mexico, 1 8 .
  5. 5. Doelling I. Joss J. Riedl J. 1996 Systematic variations of raindrop size distributions measured in northern Germany during 7 Years. Proc. 12th International Conference on Clouds and precipitation,2 Zurich, 1310-1313.
  6. 6. Federer B. Waldvogel A. 1975 Hail and raidrop size distribution from a Swiss multicell storm. J.Appl.Meteorol., 14 91-97.
  7. 7. Fiser O. 1993 A simple generator of forward scattering functions on spherical dielectrics. Radioengineering, 2(1), 21-22
  8. 8. Fišer O. Hagen M. 1998 Analysis of distrometer data. COST 75 Final Seminar “Advanced Weather Radar Systems,”. Proc.: “14 papers on Precipitation Estimates by Radar and on Analyses for Weather-Forecasting.” Swiss Meteorological Institute, Locarno, 21 33 .
  9. 9. Fišer O. Řezáčová D. Sokol Z. Školoud O. Pešice P. 1998 An attempt to classify the basic rain types from the rain rate records. COST 255 Workshop “First International Workshop on Radiowave Propagation Modelling for SatCom Services at Ku-band and above”, Noordwijk, the Netherlands, 155 157 .
  10. 10. Fišer O. Schoenhuber M. Pešice P. 2002 First results of DSD measurement by videodistrometer in the Czech Republic in 1998 1999 . Studia Geophysica et Geodetica,46, 3, 2002, 485-506.
  11. 11. Fišer O. 2002b "The role of particular rain drop size classes on specific rain attenuation at various frequencies with Czech data example," ERAD02 series, Delft(NL), 17.-22.November 2002, 1 4 .
  12. 12. Fišer O. 2003a “On Rain (DSD) Types Aimed at Radar Reflectivity and Attenuation Calculation. Proceedings of International Workshop on Precipitation in Urban Areas /6/.- Pontresina,2003., 5
  13. 13. Fišer O. 2003b On methods distinguishing drop size distribution type for improved estimation of radiowave attenuation due to rain.Proc.Conf.COMITE 2003, Pardubice, Czech Rep.,September 23-24,2003,21 24 .
  14. 14. Fišer O. 2004 "Z-R (Radar Reflectivity-Rain Rate) Relationships Derived from Czech Distrometer Data." In Proc. of the ERAD Conference, Visby, Sweden, 2004, 233 236 .
  15. 15. Fišer O. 2006 Improved Rain Attenuation Estimation Based on DSD and Radar Data. In Proc. of CNES Workshop on Earth- Space Propagation 2006, [CD-ROM], Toulouse
  16. 16. Fišer O. 2007 Selected DSD properties for meteo radar applications and microwave link attenuation in rain. In Wave Propagation in Communication, Microwave Systems and Navigation (WFMN07)- A conference of ITG commission 7.5 “Wave Propagation,” 1 4 (CD).
  17. 17. Hajny M. Mazanek M. Fiser O. 1998 Ku-Band Rain Scattering Parameters Calculated by MMP Method, Proc. In First International Workshop on Radiowave Propagation Modelling for SatCom Services at Ku band and above, 28 29 October 1998, ESTEC,The Netherlands
  18. 18. Hubbert J. C. Bringi V. N. Schönhuber M. 1999 "2D-Video Distrometer Measurements: Implications for Rainrate and Attenuation Estimators."Preprints, 29th Conference on Radar Meteorology, Jul 12- 16, 1999, Montreal, Quebec, Canada, American Meteorological Society, 666 669 .
  19. 19. Van De Hulst 1957 Light Scattering by Small Particles, New York, J.Wiley pub.
  20. 20. Iguchi T. 1999 Personal communication, August 1999
  21. 21. Jameson A. R. Kostinski A. B. 2002 "Spurious power-law relations among rainfall and radar parameters" Q. J. R. Meteorol. Soc. (2002), 128, 2045 2058 .
  22. 22. Joss J. Waldvogel A. 1967 Ein Spektrograph fuer Niederschlagstropfen mit automatischer Auswertung, Rev. Pure and Applied Geophysics,68 240 246 .
  23. 23. Joss J. Waldvogel A. 1968 The variation of raindrop size distributions at Locarno. Proc. Int. Conf. Cloud. Phys., 369.
  24. 24. Joss J. Gori E. G. 1978 Shapes of raindrop size distributions. J. Appl. Meteorol, 17 1054 1061 .
  25. 25. Lakomá-Řezáčová D. 1971 Ein Beitrag zur Genauigkeit der Bestimmung der Regenintanistaet aus einem Tropfenspektrum, Meteorologische Rundschau, 24 161 171 .
  26. 26. Li H. J. Zhang Z. W. 1980 A study of raindrop size distributions in central and northwest China and their effects on some propagation parameters for wavelengths from 0.86 cm to 10 cm. Ann.Telec, 35 405 410 .
  27. 27. Marshall and Palmer 1948 The distribution of raindrops with size. J. Meteorol., 5, 165.
  28. 28. Mie G. 1908 „Beiträge zur Optik trüber Medien, speziell kolloidaler Metallösungen“, Annalen der Physik, Vierte Folge, 25(3), 377 445 .
  29. 29. Oguchi T. 1973 “Scattering Properties of Oblate Raindrops And Cross Polarization of Radio Waves Due To Rain: Caculations at 19.3 and 34.8 GHz”, J.Radio Research Labs, 20(102), 79 119 .
  30. 30. Richter C. 1995 On the parametrisation of Drop Size Distributions- Case Studies with Distrometer, internal report of the Rutherford Appleton Laboratory (UK), 14th December, 1995
  31. 31. Řezáčová D. Kašpar M. Novák P. Setvák M. 2007 Fyzika oblaků a srážek (Physics of Clouds and Precipitation), Academia.
  32. 32. Schönhuber M. H. Urban J. P. V. Poiares Baptista. W. L. Randeu W. Riedler W. 1994 Measurements of precipitation characteristics by a new distrometer. Proceedings of "Atmospheric Physics and Dynamics in the Analysis and Prognosis of Precipitation Fields", Rome, Italy, 1 4
  33. 33. Schönhuber M. Urban H. E. Randeu W. L. Poiares Baptista. J. P. V. 2000 Distrometer results obtained in various climates and their application to weather radar data inversion. ESA SP-444 Proceedings, "Millennium Conference on Antennas & Propagation", Davos, Switzerland.
  34. 34. Strutt J. W. 1871 On the Light from Sky, its Polarization and Colour (I). Philosophical Magazine, Series 4, 41(241), 107-120.
  35. 35. Strutt J. W. 1871 On the Light from Sky, its Polarization and Colour (II). Philosophical Magazine, Series 4, 41(243), 274-279.
  36. 36. Tokay A. Short D. 1996 Evidence from tropical raindrop spectra of the origin of rain from stratiform versus convective Clouds. J. Appl. Meteorol., 35 355 371 .
  37. 37. Tokay A. Thiele O. W. Kruger A. Krajewski W. F. 1999 New measurements of drop size distribution and its impact on radar rainfall retrievals. Preprints, 29th Conference on Radar Meteorology (American Meteorological Society), Montreal, Canada, 659 662 .
  38. 38. Tokay A. Kruger A. Krajewski W. F. Kucera P. A. Pereira Filho A. J. 2002 "Measurements of drop size distribution in Southwestern Amazon basin" Journal of Geophysical Research-Atmospheres, 107(D20), LBA 19 1 to LBA 19-15, 2002.
  39. 39. Uzunoglu, Evans, Holt 1977 Scattering of electromagnetic radiation by precipitation particles and propagation characteristics of terrestrial and space communication systems. Proc IEE,124,417
  40. 40. Waldvogel A. 1974 The No jump of raindrop spectra. J.Atmos.Sci., 31 1067 1078 .

Written By

Ondrej Fiser

Published: 01 February 2010