|Researches Studying an effect of salt powder seeding used for precipitation enhancement from convective clouds
| A. S. Drofa1, V. N. Ivanov1, D. Rosenfeld2, and A. G. Shilin1
Atmos. Chem. Phys. Discuss., 10, 10741–10775, 2010
1 Institute of Experimental Meteorology, Research and Production Association “Typhoon”, Obninsk, Russia
2 Institute of Earth Sciences, The Hebrew University of Jerusalem, Israel
Received: 10 February 2010 – Accepted: 13 April 2010 – Published: 23 April 2010
Correspondence to: D. Rosenfeld (email@example.com)
Published by Copernicus Publications on behalf of the European Geosciences Union.
The experimental and theoretical studies of cloud microstructure modification with the ”optimal” salt powder for obtaining additional precipitation amounts from convective
clouds are performed. The results of experiments carried out in the cloud chamber at the conditions corresponding to the formation of convective clouds have shown 5 that the
introduction of the salt powder before a cloud medium is formed in the chamber results in the formation on the large-drop “tail” of additional large drops. In this case seeding
with the salt powder leads to enlargement of the whole population of cloud drops and to a decrease of their total concentration as compared to the background cloud medium.
These results are the positive factors for stimulating coagulation processes in clouds and for subsequent formation of precipitation in them. An overseeding effect, which is
characterized by increased droplet concentration and decreased droplet size, was not observed even at high salt powder concentrations.
The results of numerical simulations have shown that the transformation of cloud drop spectra induced by the introduction of the salt powder results in more intense
coagulation processes in clouds as compared to the case of cloud modification with hygroscopic particles with relatively narrow particle size distributions, the South African
hygroscopic particles from flares being an example of such distributions. The calculation results obtained with a one-dimensional model of a warm convective cloud demonstrated that the effect of salt powder on clouds (total amounts of additional precipitation)
is significantly higher than the effect caused by the use of hygroscopic particles with narrow particle size distributions at comparable consumptions of seeding agents. Here
we show that seeding at rather low consumption rate of the salt powder precipitation can be obtained from otherwise non precipitating warm convective clouds.
Operational hygroscopic cloud seeding aimed at rain enhancement has been conducted extensively in many countries, including India, USA, Saudi-Arabia, China, Thailand
and other countries. The seeding practice with hygroscopic flares became fashionable after the reports of the apparent success of the South African (Mather et al.,
1997) and Mexican (WMO, 2000; Bruintjes et al., 2001) experiments, and the simulations with theoretical support for the efficacy of the flares (Cooper et al., 1997). The operational practice has been to seed the updraft just below cloud base with one to
two 1-kg hygroscopic flares that burn in about 4 minutes. This means a seeding rate of 0.25 to 0.5 kg/min or, with an air speed of 70 m/s, a rate of 0.015–0.03 kg/km of seeding
path. This practice prevails even though demonstration of its efficacy is lacking.
Furthermore, Segal et al. (2004) calculated the particle size distribution of hygroscopic aerosols that would accelerate the conversion of cloud water to rain drops for the least
amount of salt mass, and showed that this was quite different from the particle size distribution that is produced by burning hygroscopic flares. Rosenfeld et al. (2010) followed
this up and manufactured a salt powder that matched the optimal particle size distribution as calculated by Segal et al. (2004), and tested it against hygroscopic flares
in actual cloud seeding experiments. The results of Rosenfeld et al. (2010) support the simulations of Segal et al. (2004) and show that to produce a microphysical seeding
effect on the clouds that is detectable by cloud physics aircraft, a mass concentration greater by an order of magnitude than is presently practiced with hygroscopic flares has to be dispersed.
The paper presents the results of experimental and theoretical studies of cloud modification with the salt powder developed at the Hebrew University, Israel, for obtaining
additional precipitation amounts from convective clouds. Experiments carried out in the cloud chamber of the Research and Production Association “Typhoon”, Russia, under
the conditions corresponding to the formation of convective clouds, as described in Sec. 2. The observed changes of the cloud microstructure at different seeding rates
in the cloud chamber are given in Sect. 3. The conversion of cloud water into rain could not be fully documented even in this big cloud chamber due to sedimentation of
the large cloud drops. The implication with respect to conversion of the cloud water to rainfall had to be assessed by a 1-dimensional cloud model, which replicated the
observed initial spectra and extended the calculations through the formation of rain.
This was done both for the salt powder and for other hygroscopic agents with narrow particles size distributions, as described in Sect. 4. The conclusions, given in Sect. 5,
provide the particle size distribution and seeding rates that would result in the fastest conversion of cloud water to rainfall for a range of seeding rates of the hygroscopic
seeding agents. It should be noted here that the fastest conversion of cloud water to rainfall does not always mean also the greatest amount of precipitation (Rosenfeld
et al., 2008). Establishing the seeding effects on precipitation requires randomized seeding experiments in the natural atmospheric conditions accompanied by detailed
microphysical measurements and model simulations.
2. The Big Cloud Chamber and its usage for measurements in aerosol and cloud media
Experimental studies of a salt powder seeding effect on a cloud medium were performed in the Big Cloud Chamber (BCC) of RPA “Typhoon”. BCC is designed for
modeling convective or stratified clouds and fogs of different origin under the conditions close to those in the real atmosphere.
The chamber is a steel airtight cylinder of 18-m height and 15m diameter. The chamber walls of 6-mm thickness are externally
heat-insulated. The total volume of the chamber is 3200m3. A cloud medium is formed up to a height of 15 m. The technological compartment separated by a metallic grating
is located above. A detailed description of the BCC and the methods of cloud media formation in it are presented in (Romanov and Zhukov, 2000).
The process of convective cloud medium formation in the BCC is made through air expansion. For this external air is pumped into the chamber. As a result the air
pressure in it is increased to a certain level. The air pressure decrease is made by opening holes in the upper part of the chamber. The air discharge from the chamber through
the holes of different cross sections makes it possible to regulate the rate of pressure decrease in the chamber, thus setting a certain velocity of air updraft in the atmosphere
during the formation of a convective cloud. The program 5 controlling pressure decreasing in the BCC makes it possible to realize a preset scenario of air mass updraft
in the atmosphere with equivalent rates of 0.1–10 m/s. Air temperature, pressure, humidity and the chamber wall temperatures are basic parameters for setting thermodynamic
conditions in the BCC. These parameters are continuously measured during the experiments in the BCC. For setting the conditions of cloud medium formation thermodynamic
relationships and the known heat exchange coefficients for the BCC are used (Romanov and Zhukov, 2000).
In the efforts described in this paper the pressure decrease in the BCC was made from the initial value of 1300 hPa with the velocity of air mass updraft in the atmosphere
of 1.2–1.3 m/s. Relative humidity of air in the chamber before the pressure drop is usually 90–96%. The air temperature is 22–25 C. At such values of meteorological
parameters a cloud medium in the BCC is formed in 2–3 min after the beginning of the pressure lowering. The air temperature decreases practically linearly until it becomes equal to that of the chamber walls. It usually makes 18–20 C. This period lasts 12 min
during which the equivalent velocity of air updraft decreases to 0.9 m/s. Just during this period the process of cloud medium formation in the BCC may be considered
adequate to the process of convective cloud formation in the real atmosphere.
As the total heat capacity of the BCC walls is by about 10 times greater than the total heat capacity of air in the chamber, the evolution of the cloud medium is more
strongly affected by the processes of air heat exchange with the chamber walls. When the air temperature becomes lower than that of the wall, the wall heats the air. Despite the continuing lowering of air pressure the rate of air temperature change in the BCC
decreases. The total cooling of the air in the BCC reaches 8 C by this time. During the experiment the wall chamber temperature changes very slowly (no more than by 1 C). By 20 min after the cloud medium began to form the equivalent velocity of updraft drops to zero, the air temperature begins to rise and the cloud begins to evaporate. The
total lifetime of the cloud in the BCC is 40–50 min.
For measurements of aerosol and cloud medium microstructure the BBC is equipped with the photoelectric particle analyzer developed at the RPA “Typhoon”. These devices
are based on measurements of light scattered from particles at an angle of 90. The principle of operation of the analyzers is in the analysis of amplitudes of pulses of
light scattered from single particles at their flight through the measuring volume. Optical formation of the measuring volume not causing changes in the microstructure of measured particle is used in the analyzers.
In the photoelectric meter of cloud drops (Romanov, 1991) an electric filament lamp is used as a light source. The light flux from the lamp is focused by a round lens on
its axis. The light scattered from a drop in the lens focus is collected by the round lens and directed to the photodetector. The angle between the axes of the illuminating
and the positive lenses makes 90. The principle of drop sizes measurements is in the measurement of the intensity of light scattered by a drop and the use of the calculated
dependences of scattered light intensity on a drop size. For this, the operating characteristic of the device is calculated. The operating characteristics of such devices are
calculated with the Mie scattering theory for spherical particles (Heyder and Gebhart, 1979; Singh et al., 1982). The angular apertures of the light source and of the light detector
are taken into consideration. The lamp radiation spectrum and the photodetector spectral sensitivity are also taken into account. The range of measured drop radii with
this meter is within 1–50 μm. The number of drop size measuring channels is 360.
The photoelectric meter is an analog of an airborne instrument used in studying cloud microstructure in the real atmosphere. It allows one to obtain cloud drop spectra at the
time of data accumulation from 1 s at the medium flow rate through the measuring volume over 2.5 cm3/s, which was driven through the probe by a fan located downstream
of the measurement volume. During the measurements in the BCC the photoelectric meter was located near the bottom of the cloud chamber.
The same principle of drop size measurements, as that mentioned in the device described earlier, is used in the laser analyzer of particles (Kolomiets at al., 1989)
for measurements of solid aerosol particles microstructure. A continuously operating laser at the 0.63 μm wavelength serves as a light source in the analyzer. Its main difference
from the device described above is in the peculiarities of the optical formation of the measuring volume. High uniformity of illumination of the measuring volume is
achieved in the laser analyzer because of the use of an annular laser beam and subsequent electronic processing of photoelectric pulses. The annular beam is formed from
the initial laser beam with the help of a special lens (axicon) having one flat surface and the other one is conical in form. The light scattered by particles under study is
collected with the elliptical mirror and sent onto a photodetector in the frames of the annular aperture in the scattering angles of 60 –120 . The operating characteristic of
the laser analyzer is calculated with the account for the geometric peculiarities of its optical scheme. The laser analyzer makes it possible to measure particle size distri15
butions within the particle radii of 0.1–5 μm. The number of particle size measurement channels is 120. The aerosol under study is supplied via a thin capillary into the region
of laser beam focusing. The flow rate of air passing through the analyzer volume is 1 cm3/s.
With the data of photoelectric analyzers calculated also are the integral parameters of size distribution functions such as concentrations and effective radii of the particles.
The particle concentrations are determined from the frequency of pulses of light scattered from every particle. Both photoelectric analyzers are calibrated against round
polysterol latex particles with the known sizes and the known light refraction index.
The experiments in the BCC on cloud medium modification by the salt powder were performed according to the following method. First a cloud medium on natural condensation
nuclei was formed in the BCC, and during about 20 min measurements of the background cloud medium parameters were made. Then the pumping of the chamber
up to the initial high pressure was repeated and salt particles were injected into it. The spraying of the salt powder from an airplane in the cloud was simulated by a pneumatic
atomizing nozzle (like a spraying can). Then via the piping it was introduced into the BCC. With the help of fans the aerosol was uniformly mixed inside the chamber. At the
moment of the beginning of pressure dropping the fans are switched off. The salt particles were introduced into the chamber at a relative humidity of about 96%. By this, the conditions of particles introduction into the subcloud layer of a convective cloud were
simulated. Then, the process of lowering air pressure in the chamber was repeated, and the parameters of the cloud medium formed as a result of aerosol particles impact
were measured. The modification effect was assessed from the results of comparing the parameters of the cloud medium with the corresponding parameters during the
background experiment. During numerous experiments in the BCC it has been found that at repeated lowering of air pressure the parameters of the cloud medium remain
practically the same, so the impact of salt particles with the use of the method developed is made under similar conditions of cloud medium formation as compared to the
Fig. 1. Observed background aerosol particles spectrum in the BCC at a mass concentration of
5×10−4 mg/m3 (1), the spectrum of dry salt particles (2) and the spectrum of the South African
hygroscopic flares particles (3) both at the same mass concentration 0.4 mg/m3. Dashed lines
refer to the approximation made by functions (1, 2).
The agent under study is a specially prepared powder of NaCl with aerosol (SiO2) used as an anticaking admixture (Lahav and Rosenfeld, 2005; Rosenfeld et al., 2010).
The measurements of microstructure of the dry salt particles under this study were made in the BCC at the air relative humidity of about 40% with the laser analyzer of
particles. After the salt powder was introduced into the chamber with the pneumatic atomizing nozzle the aerosol was uniformly mixed inside the chamber and measured
there. The results of measurements of the dry particles size distribution function of the salt powder are shown in Fig. 1. Here also given are the spectra of background aerosol
the mass concentration of which made 5×10−4 mg/m3. The measurements were performed at a salt mass concentration of 0.4 mg/m3. The spectra are obtained during the
time of data accumulation of about 10 min. The spectrum of salt powder particles was obtained by subtraction of background aerosol spectrum from the aerosol spectrum in
the BCC after the introduction of the salt powder. As is seen from the graphs, in the salt powder studied there is a considerable number of particles the sizes of which are
smaller than the lower measurement limit of the laser analyzer (0.15 μm). These may be the particles of the anticaking admixture or the “fragments” of salt. The particles
effective radius in the size range studied is 1.54 μm. As is seen from Fig. 1, there are also particles with the sizes exceeding the upper measurement limit of the laser analyzer
(5 μm). To reveal the structure of these particles, aerosol particles sampling was made by their settling onto a glass substrate during the measurements in 5 the BCC.
Microscopic studies of the samples have shown that in the powder studied there exist large particles with the radii up to 10 μm. In this case, large particles with the sizes over
5 μm are mainly the salt particle conglomerates with finer particles that stuck to them. It should be noted here that the salt powder was tested three years after it was manu10
factured and held in closed plastic bags within cardboard boxes in a storage room, so that some clumping could take place during this long period.
Figure 1 gives the approximation of background aerosol particles spectrum made by the Junge spectrum
where v=5. The spectrum of salt particles, as is seen from Fig. 1, is rather well
approximated by the distribution like
where ro =5 μm.
For comparison, the particle size distribution of the South African hygroscopic flares (Cooper et al., 1997) is given in Fig. 1 at a mass concentration equal to the salt powder
concentration of 0.4 mg/m3. Figure 1 reveals that the South African flares contain a very high number of particles with r<1 μm as compared to the salt powder. At the
same time the particles with r>1 μm are much less in number.
3. BCC measurements of salt seeding effects on cloud microstructure
The evolution of the cloud drop size spectra obtained with the use of a photoelectric meter in the BCC is shown in Fig. 2. Here presented are typical cloud drop spectra determined
at different time steps after the formation of a cloud medium during the background experiments. The time starts from the moment of the cloud medium formation.
Fig. 2. Observed evolution of cloud drop spectrum in the background experiment (numbers at the curves – time (min.) after the cloud medium formation).
At the chosen mode of air pressure lowering a cloud medium with the drop concentration from 1300 to 1550cm−3 is formed. The liquid water content of the medium grows
linearly with time and by 12 min it becomes equal to 0.8 g/m3. The largest drops in the
background experiments reached the radii of 12 μm. Figure 3 gives the results of cloud drop spectrum measurements at different time
steps at the introduction of 3.5 g of the salt powder into the BCC. When distributed over
the BCC volume of 3200 m3 it constitutes a mass concentration of 1.1 mg/m3. The
modal size of the cloud drops that formed in the BCC appear to be nucleated on the background condensation nuclei. The temporal character of variation of this spectrum
range does not practically differ from the behavior of spectra obtained during the background experiment. From the graphs in Fig. 3 it is seen that the introduction of such an
amount of salt particles manifests itself only in the large-drop fraction of the cloud drop spectrum. A “tail” of large drops that formed on the added salt particles appeared on
the drop size distribution that was measured already at the first 2 minutes after cloud formation. In the spectra measured after 4 min of the cloud medium existence the
large-drop “tail” of the distribution appears to be truncated due to gravitation-induced sedimentation of the largest drops onto the BCC floor. Actually, the terminal sedimentation
rate of drops with the radii of, for example, 30 μm, is equal to 11 cm/s. At the height of the BCC working volume of 15 meters all the drops of such sizes formed
at this level fall onto the floor of the BCC during 2.5 min. The duration of the settling process of drops with radii of 20 μm takes about 5 min. It is clear that the life-time of
such drops formed at the lower levels of the BCC is much shorter. This causes a sharp decrease of the observed number of drops with radii larger than 20 μm. The effective
radius of drops calculated over the spectra increased in this case by 5% as compared to the background experiment, and the largest registered drops reached radii of 16 μm.
The evolution of cloud medium spectra at the introduction of 16 g of salt particles with the mass concentration of 5 mg/m3 is shown in Fig. 4. Here the bimodal character
of the cloud drop spectrum is seen distinctly. In this case the cloud droplets formed on the background aerosol particles are smaller in size as compared to the background
experiment. This effect is explained by a decrease of water vapor supersaturation in the cloud medium at the introduction of the given amount of salt particles. As a result, a
slower growth of drops formed on the background aerosol occurs. The fraction of large cloud drops formed on the salt particles is here significantly greater than in the previous
case. The drop effective radius at the introduction of 16 g of salt powder increased as compared to the background experiment by 20%. The largest drops attained radii of
At the introduction into the BCC of a rather great amount of salt particles (31 g, with the mass concentration of 9.7 mg/m3), as is seen from Fig. 5, practically all the cloud
drops are formed on salt particles. The fine-droplet spectrum fraction, that appeared due to the background condensation nuclei, does not manifest itself. The effective
radius of drops increased in this case as compared to the background experiment by 1.35 times, and the largest drops registered reached the radii of 22 μm. The cloud drop
concentration here decreased by 2.5 times. An example of changes in the integral parameters of cloud medium microstructure during the background experiment and in
the experiment in the BCC with the introduction of 3.5 g of salt particles is presented in Fig. 6. The time count begins at the moment of the cloud medium formation. As
one can see from the data presented, the introduction of the salt powder results in the formation of larger cloud drops and their lower concentrations as compared to the
background experiment. The cloud medium liquid water contents are practically the same in both experiments. The experimental results have shown that at an increase of
the mass of the particles introduced, the modification effect becomes stronger.
Fig. 3. Observed evolution of cloud drop spectrum at introduction of salt powder into the
BCC with the mass concentration of 1.1 mg/m3 (numbers at the curves – time (min.) after
the beginning of cloud medium formation).
Fig. 4. Observed evolution of cloud drop spectra at the introduction of salt powder into the
BCC with the mass concentration of 5 mg/m3 (numbers at the curves – time (min.) after the
beginning of cloud medium formation).
The results of measuring the cloud medium integral parameters at different masses of particles introduced are given in Table 1. Table 1 contains the salt particle mass
concentrations at different masses of salt powder introduced, and cloud drop concentrations at the introduction of particles (N) and in the background experiment (NF ).
Fig. 5. Observed evolution of cloud drop spectra at the introduction of salt powder into the
BCC with the mass concentration of 9.7 mg/m3 (numbers at the curves – time (min.) after the
beginning of cloud medium formation.
Fig. 6. Observed changes with time of cloud medium liquid water content (1, g/m3), concentration
(2, 300cm−3) and effective radius of cloud drops (3, μm) in the background experiment
(solid curves) and at the introduction of salt powder with the mass concentration of 1.1mg/m3
Table 1 gives averaged data obtained during the experiment in 4–5 min. after the cloud medium formation in the chamber, i.e. after the process of nuclei activation ended
and the cloud medium parameters are stabilized. It contains also the values of a relative dispersion of cloud drop spectra at the introduction of particles (S) and in the
background experiment (SF ) calculated from the measured spectra with the formula
where r1 and r2 are the mean and mean-root-square radii of drops, respectively. The values of S are calculated for the 12th minute of the cloud medium
|Table 1. Measurement results of cloud medium parameters in the experiments of introduction of salt powder particles into the cloud chamber.
A necessary condition for obtaining a positive effect at modification by hygroscopic
particles (precipitation enhancement) is an increase of cloud drop sizes at the introduction
of particles (Drofa, 2006), as far as the enlargement of cloud drops is the major factor stimulating gravitational coagulation in clouds and subsequent precipitation
formation. Changes of cloud drop sizes were estimated by us during modification experiments over the changes of their concentrations against the drop concentrations
in the background experiment. Under similar conditions of performing these experiments
(the same liquid water contents of cloud media) the relationship NF /N =(r/rF )3
is valid, where r and rF , N and NF are the effective radii of drops, their concentrations
at modification and in the background experiment correspondingly. It means that the
value of NF /N characterizes the changes of cloud drop sizes under modification. It is
easily measured experimentally. In such a way the values of r/rF given in the Table 1
The effect of modification can be considered positive at NF /N>1 (i.e. when the drop
become larger). As one can see from the data given in the Table, the necessary condition
for obtaining a positive effect of modification with the salt powder under study in
our experiments is met – at the introduction of salt particles a decrease of cloud drop
concentration and the drop growth are observed. With increasing weight concentration of salt particles introduced,
this effect of modification increases practically linearly.
The introduction of a great amount of salt particles does not result in “overseeding” at
which the concentration of drops increases and instead of their enlargement the drops
The measurement results of a relative dispersion of drop spectra given in Table 5
show that the introduction of salt particles in the cloud medium causes the spectrum
broadening as compared to the background cloud medium. This effect increases with
increasing the particle mass. The effect is a positive factor at cloud medium modification
for precipitation enhancement as far as the greater the difference in drop sizes
in the cloud medium, the more efficient the coagulation processes of cloud drops and
precipitation formation are. As has been mentioned earlier, the drop spectra obtained
in the BCC are “truncated” in the large-drop-spectrum range because of the settling of
drops onto the BCC floor. It is most probable that in real clouds broadening of cloud
drop spectra may be considerably larger than in the experiment.
The value of NF /N can serve as an estimate of the efficiency of cloud modification with hygroscopic particles having relatively narrow particle size distributions (Drofa,
2006). At the introduction of such particles into the subcloud layer governing in the stimulation of coagulation processes in a cloud is the increase of the whole population
of cloud drops. The more the value of NF /N is realized in the cloud base, the greater
will be the amount of additional precipitation at modification. A characteristic property of modification by particles with narrow drop size distributions is that the positive effect
of modification is realized only at an optimal concentration of such particles. An example of the use of such particles is the modification of convective clouds by pyrotechnic
flares developed in South Africa (Mather et al., 1997). Their particle size distribution is given in Fig. 1. When such flares were used, the positive meaningful modification effect
was obtained in several projects aimed at obtaining additional precipitation amounts from convective clouds. Using the method proposed in (Drofa, 2006) with the known
data on particle size distribution, physical and chemical characteristics of pyrotechnic flares for typical atmospheric conditions, it is possible to obtain a maximum value of
NF /N =1.42. This value is achieved at a certain concentration of particles introduced (300–500 cm−3). The mass concentration of the substance contained in pyrotechnic
flares makes 0.05 mg/m3. At higher or lower concentrations the value of NF /N decreases.
When mass concentrations of particles introduced make over 0.14 mg/m3, an effect of “overseeding” appears, i.e. at the introduction of particles the drop concentration
in the cloud increases and their mean size decreases. This is the cause of decreasing intensity of precipitation formation in the cloud at “overseeding”.
4. Simulations of the seeding effects
To overcome the effect of truncation of the drop size distribution by sedimentation and to assess the efficiency of hygroscopic agents with rather wide particle size distribution
functions (one of them is the salt powder under study), simulation studies are needed.
In this paper we shall theoretically study the efficiency of cloud modification by the salt powder with the use of a one-dimensional convective cloud model developed by
Drofa, (2008, 2010). This numerical model of a warm convective cloud allows one to study a spatiotemporal scheme of cloud formation and development and to analyze
the evolution of cloud microstructure and precipitation in response to the introduction of hygroscopic particles.
The 1-dimensional numerical model describes the evolution of a cloud medium in the central part of an axisymmetric warm convective cloud at a preset variable with
height velocity of an air updraft forming the cloud. The equation system is used for temperature and air pressure changes and for water vapor supersaturation at air mass
lifting. Entrainment of heat and water vapor into a lifting air parcel from the environment is accounted for parametrically (as in Pruppacher and Klett, 1997). The value
of the entrainment coefficient is taken inversely proportional to the altitude above the cloud base. Adjustment of parameters characterizing entrainment gives a possibility
to achieve a complete matching of vertical profiles of cloud parameters obtained in the model with the parameters of continental clouds in the real atmospheric conditions
(Mazin and Shmeter, 1983; Shmeter, 1987).
The vertical profile of vertical air velocity is prescribed in the numerical model and does not change between the stages of cloud development. To describe the air updraft
velocity vertical profile a universal function considering basic regularities of air vertical fluxes in continental convective clouds (Shmeter, 1987) is applied. The velocity 5 of an
air updraft at the cloud base is set to 1.5 m/s. It increases proportionally to altitude in
the lower half of the cloud. Maximum velocity is achieved at the half cloud height. It is proportional to the cloud thickness. At a cloud thickness of 4km it reaches about
5 m/s. In the cloud upper half the updraft velocity drops gradually to zero. The altitude at which the updraft velocity is equal to zero is determined by the cloud thickness.
Limitation of growth of the convective cloud upwards occurs due to the existence in the atmosphere of a barrier layer with isothermality and inversion of air temperatures.
The height of this layer above the cloud base determines the height of maximum liquid water content in the cloud. In the numerical model, the atmospheric barrier layer is
simulated by the introduction at a certain level above the cloud base of water vapor sub-saturation, as far as low air relative humidity has a governing role in the cloud
medium evolution. The altitude of the barrier layer above the cloud base is preset at the level of 0.8 of the cloud thickness. This corresponds to the parameters of moderate
convective clouds observed in real atmospheric conditions. Above this level the cloud top is formed, where fine cloud droplets evaporate and the large drops precipitate into
the lower cloud layers.
In the given numerical model it is assumed that the activation of condensation nuclei takes place in the cloud base. At a further lifting of the cloud medium only the process
of drop condensation growth/evaporation occurs. New cloud drops do not form.
The initial stage of cloud medium microstructure formation is described by the equation of drop condensation growth. With the use of the initial conditions of the air mass
state and the parameters of condensation nuclei (atmospheric and/or additionally introduced), the size distribution function of drops originated at the cloud base is calculated
according to the method used in (Drofa, 2006). Further evolution of the size distribution function is calculated with the use of the kinetic equation. The model contains a
precise description of warm rain microphysics. The processes of drop condensation growth/evaporation, coagulation, breakup of drops and their sedimentation are considered.
For a numeric solution of the kinetic equation a fixed grid of cloud drop sizes in the radius range of 1–2500 μm (396 points) with a non-uniform step in radii was used.
Sedimentation of drops and precipitation are computed from the difference of terminal falling velocities of drops of different radii and the rate of the air mass updraft. For this
determined is the number of drops that fell from the given cloud layer and those that entered this layer from the above level during a certain period of time. With the data obtained during model simulation calculated are the spatiotemporal
structure of meteorological parameters and integral characteristics of the cloud drop size distribution function – the drop number concentration, cloud liquid water content
and the cloud drop effective radius. The liquid water contents of large drops with the radii r>200 μm characterizing precipitation are computed as well. Total amounts of pre15
cipitation are calculated at the level of the lower cloud boundary. It should be said that owing to the fairly simplified description of the dynamic structure of the cloud development,
dynamic responses of the clouds to the modified precipitation are not considered in the model. The results of calculated precipitation in this model should be regarded
as relative estimates. They can be used only for comparison of the efficiencies of the tested hygroscopic cloud seeding methods.
Fig. 7. Evolution of simulated cloud drop spectrum at the introduction of salt powder with the
mass concentration of 1 mg/m3 (the numbers at the curves – time (min.) after the beginning of
the cloud medium formation).
An example of computation of the initial stage of the cloud medium microstructure formation at the introduction of the salt powder into the subcloud layer of the convective
cloud according to the method used in (Drofa, 2006) is shown in Fig. 7. Here presented are the calculation results of cloud drop spectrum evolution with time for the conditions
typical of continental convective clouds. The physical and chemical properties of the aerosol correspond to mean characteristics of atmospheric aerosol of continental origin
(Drofa, 2006). The Junge distribution (1) was used as an initial distribution of aerosol particles being atmospheric condensation nuclei at v=4. The velocity of air mass
updraft is accepted as V =1.5 m/s. The initial temperature of air is 10 C. The pressure is 900 hPa. To describe the salt particles size distribution the function like (2) was used.
It corresponds to experimentally measured spectra of dry salt powder particles. The sizes of salt particles were accounted for within the range of radii from 0.01 to 10 μm.
The mass concentration of the particles introduced was taken equal to 1 mg/m3. At such a concentration, as is seen from Fig. 7, the effect of salt particles reveals 5 itself only
in the large drop “tail” of cloud drop distribution range without changes in the spectrum of drops formed on atmospheric condensation nuclei. The same character of cloud
drop spectrum variations is observed in experimentally obtained spectra measured in the BCC at a very similar concentration of the salt powder introduced (see Fig. 3).
The calculation results of drop spectra in the convective cloud after 120 s at the introduction of different amounts of the salt powder into the subcloud layer are presented
in Fig. 8. The atmospheric conditions are the same as in the case mentioned above. As it is seen from Fig. 8, at a small mass concentration of the powder, the introduction
of such particles results only in the growth of the large-cloud drop fraction. This drop fraction is growing with increasing mass of the powder introduced. The shape of the
drop spectrum formed on the background aerosol particles does not change at their mass concentration of the particles up to 1 mg/m3.
At the concentrations of the salt powder higher than 1 mg/m3 a decrease of the number of drops formed on atmospheric condensation nuclei occurs. This effect is also observed in the experimental data obtained at high concentrations of the salt powder
(see Figs. 4 and 5). The effect is explained, as it has been mentioned earlier, by the fact that the introduction of larger amounts of salt particles decreases the supersaturation of
water vapor. This causes a slower growth of drops formed on the background aerosol
Fig. 8. Simulated drop spectrum in the background cloud (1), at the introduction of salt particles
with the radius of 1 μm with the mass concentrations of 1.1 mg/m3 (2) and at the introduction of
salt powder with the mass concentrations of 0.01, 0.1, 1 and 5 mg/m3 (curves 3–6, correspondingly).
The evolution of the cloud drop size spectrum at the introduction of hygroscopic particles with a very narrow particle size distribution into the convective cloud sublayer
is given as an example in Fig. 8 as well. In this case, the particles of NaCl with an effective radius of 1 μm and a relative dispersion of the drop size spectrum S =0.3 are
introduced. The number concentration of the particles introduced makes 120 cm−3 (an optimal concentration of particles of the given sizes). The particle mass concentration
is 1.1 mg/m3. As is seen from Fig. 8, the result of the introduction of such particles is in the formation of a bimodal cloud drop spectrum. The large drop mode is governed
by the growth of drops formed on salt particles. The small drop mode is formed on the background aerosol particles. Further, the bimodal character of the cloud drop
spectrum is maintained in the quasi-equilibrium state.
The studies of the modification effect induced by such particles have shown (Segal et al., 2004, 2007; Drofa, 2006) that at the introduction of salt particles, due to decreasing
water vapor supersaturation in the cloud, the number of atmospheric nuclei is activated (i.e. they turn into cloud drops) to a lesser degree than in the background
cloud. As a result, the total concentration of cloud drops formed on the background and additional nuclei appears less than in the case when additional condensation nuclei are
absent. Average sizes of cloud drops at the introduction of particles become greater.
Due to this a positive effect of modification by hygroscopic particles with narrow drop size distributions is attained, because the enlargement of cloud drops is the major factor
stimulating gravitation-induced coagulation in clouds and subsequent precipitation formation. One should pay attention to the fact that the cloud drops formed on atmospheric
aerosol particles are smaller in size as compared to those in the background cloud. It means that in this case the impact of salt particles leads to changes in the
conditions of cloud drop formation on atmospheric condensation nuclei.
Modification made by the salt powder does not result in such changes even at rather high mass concentrations of the powder introduced. The number of cloud drops formed
on background aerosol particles changes little here. As the analysis of the results of numerical simulations demonstrate, the modification by the salt powder causes a
higher intensification of coagulation processes in the cloud than at the modification by hygroscopic particles with narrow size distributions. This can be explained by the fact
that at the modification by the salt powder the drop spectrum is broadened only towards the large-drop fraction where coagulation is more efficient.
The data obtained at the initial stage of condensation (Fig. 8) are used as starting data for calculations of evolution of cloud medium microstructure with the onedimensional
numerical model of a convective cloud (Drofa, 2010). The calculation results for precipitation obtained with the model for clouds of different thicknesses at
modification by different amounts of salt particles are shown in Fig. 9. The introduction of particles into the 60, 120 or 240m subcloud layer is made at the 5 10th min. from
the beginning of the cloud formation. The data given in the same figure for clouds without modification demonstrate that the significant precipitation quantities calculated
with this model fall out from convective clouds with thicknesses over 3.5 km. This result is in agreement with the data of experimental studies of clouds in real atmospheric
conditions (Mazin and Shmeter, 1983).
The results of numerical simulations show that the effect of modifying clouds with hygroscopic particles significantly depends on the cloud vertical thickness – the more
the thickness, the greater the precipitation amounts are. The calculation data on the effect of the South African pyrotechnic flares particles show that significant additional
precipitation amounts are observed only at modifying clouds with the thicknesses over 4 km. The calculations are made for the case of particles introduction into the layer
with the thickness of 240m at a mass concentration of particles of 0.05 mg/m3 and the consumption of 12 kg of the agent per 12 of the seeded area. The use of smaller
amounts of such particles does not lead to a discernible positive modification effect.
The result presented is in agreement with the data of field experiments aimed at cloud modification with such particles (Mather et al., 1997; WMO, 2000; Bruintjes et al.,
2001). In these experiments at comparable with the above-mentioned agent consumptions a 10–15% precipitation enhancement from the clouds of 6-km thicknesses was
Fig. 9. Simulated total amount of precipitations, defined as r>200 μm, from clouds of different
thicknesses without the introduction of particles (1), with the 12 kg/km2 particles of the South
African flares consumed (2), with 2.4, 6, 12, 24, 48 kg/km2 of the salt powder (curves 3–7,
respectively). Dashed lines refer to the introduction of 64 kg/km2 of salt particles with the radii
of 1 μm. The precipitation is calculated at the level of cloud base.
Modeling was made for different mass concentrations of the salt powder with 0.01, 0.05, 0.1 and 0.2 mg/m3. The results of numerical simulations demonstrated that the
effect of modification by the salt powder is determined by the total amount of the powder introduced into subcloud layer. This means that at the introduction of the powder
with the concentration of, for example, 0.1 mg/m3 into the 120-m layer the same precipitation amount is observed as at the introduction of the powder with the concentration of
0.2 mg/m3 into the 60-m layer. The amount of the agent at the given mass concentration is determined by the thickness of the layer into which the agent is introduced. So,
at the introduction of the powder with the particle mass concentration of 0.1 mg/m3 into the 120-m layer the consumption of the agent is 12 kg per 12 of the seeding area.
At changing the layer thickness where the agent is introduced the agent consumption changes proportionally with the thickness of the layer.
As is seen from Fig. 9, seeding with salt powders results in a significant increase of precipitation amounts as compared to cloud modification by fine particles of the
South African pyrotechnic flares. At the consumption of 2.4 kg/km2of the salt powder the precipitation amounts falling from the clouds with the thicknesses over 4 km are
greater than at cloud modification with the pyrotechnic flares (at the consumption of pyrotechnic particles of 12 kg/km2).
The modification effect obtained in case of a salt powder is also significantly higher than that achieved with larger salt particles with narrow particle size distributions. Fig. 9
gives the calculation results for precipitation at seeding with salt particles with effective radii of 1 μm at optimal mass concentration 1.1 mg/m3. The cloud drop spectrum at
the initial stage of condensation at seeding by these particles is shown in Fig. 8. The consumption of the agent per 1 2 of the seeding area for such particles, when they
are introduced into the 60-m subcloud layer, makes 64 kg. From Fig. 8 it is seen that at seeding with such particles the modification effect appears almost the same as in
case of using the salt powder with its consumption of 12 kg/km2. It means that the consumption of the salt powder is by 5 times less than that of the salt particles with the
radii of 1 μm.
The calculation results demonstrated that in case of cloud seeding with salt powders at their consumption of 24 kg/km2, additional precipitation amounts may be obtained
from clouds with 2.5<H<3.5 km. Such clouds are not giving significant precipitation under natural conditions. Maximum effect of modification – the greatest precipitation
amounts – is realized at the consumption of 48 kg/km2 of the salt powder (the upper curve in Fig. 9). Here, as the analysis of numerical simulation results shows, when
precipitation falls down, an insignificant number of cloud drops remains in the cloud.
Practically, almost all of the cloud water transforms into rain drops. Therefore, a further
increase in consumption of the agent (over 48 kg/km2) does not lead to a significant additional precipitation enhancement.
The results of experiments carried out in the cloud chamber at the conditions corresponding
to the formation of convective clouds have shown that:
The results of numerical simulations of cloud medium formation at the initial stage of condensation have shown that:
- The introduction of the salt powder before a cloud medium is formed results in the formation on the large-drop “tail” and in the broadening of drop size spectrum.
This result is a positive factor for stimulating coagulation processes in clouds and
for subsequent formation of precipitation in them.
- No impact is observed on the fine-droplet spectrum fraction formed on background condensation nuclei even at moderate amounts of the powder introduced.
- Seeding with the salt powder leads also to enlargement of the whole population of cloud drops and to a decrease of their total concentration as compared to the
background cloud medium. With the introduction of increasing mass concentration
of salt particles, this effect increases practically linearly. This factor also leads
to a positive modification effect for stimulating the conversion of cloud water into rain drops.
- At the introduction of very high concentration of the powder no “overseeding” is
observed, i.e., increase of drop concentration along with reduction of their size is
The calculated rainfall amounts of the numerical simulations with a 1-dimensional numerical model of a warm convective cloud have shown that:
- The introduction of the salt powder into the convective subcloud layer leads to the
appearance of a large-drop “tail” in the cloud drop size distribution. The shape of
the spectrum in the large-drop region is determined by the salt powder particles
- The shape of the spectrum of drops formed on background condensation nuclei
does not change at rather high concentrations of the powder introduced. This
means that the introduction of the salt powder does not change much the conditions
of the formation of cloud drops on the background aerosol particles, except
for at very high mass concentration. This result is confirmed by the experimental
data obtained in the cloud chamber.
- As the analysis of numerical simulation results shows, the transformation of cloud
drop spectra induced by the introduction of the salt powder results in much more
intense coagulation processes in clouds as compared to the case of cloud modification
with particles from hygroscopic flare at the same mass concentration.
- The salt powder results also in much more intense coagulation also with respect
to hygroscopic particles having 1- μm very narrow particle size distribution of the
same mass concentration.
In summary, the experimental data and the results of numerical simulations presented demonstrate the great promises arising from the use of the salt powder studied for
obtaining additional precipitation amounts from convective clouds when accelerating the coagulation results in additional rainfall on the ground. Thus it is proposed to recommend
using this salt powder in the seeding experiments in the natural atmospheric conditions.
- The effect of the salt powder on clouds (total amounts of additional rain) is significantly higher than that caused by the use of hygroscopic flares at comparable
consumptions of seeding agents (of the order of 10 kg/km2).
- At the consumptions of the salt powders over 20 kg/km2 rainfall can be obtained from otherwise no-precipitating clouds with thicknesses of 2.5<H<3.5 km. At the
consumptions of about 50 kg/km2 of the powder the maximum effect of modification
– maximum precipitation amounts – is realized. A further increase of the amounts of the salt powder introduced into a cloud does not result in significant
additional precipitation amounts. Owing to a fairly simplified description of cloud
development in the present 1-dimentional model, the consumptions of the salt
powders indicated above should be regarded as estimates. For more accurate
calculations it is necessary to use more realistic 2 or 3-dimensional cloud model
with full ice microphysics and dynamic feedbacks to the precipitation forming processes.
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