JOURNAL OF GEOPHYSICAL RESEARCH, VOL. 107, NO. D19, 4367, doi:10.1029/2001JD001269, 2002

Physical properties of maritime low clouds as retrieved by combined
use of Tropical Rainfall Measuring Mission (TRMM) Microwave
Imager and Visible/Infrared Scanner
2. Climatology of warm clouds and rain
Hirohiko Masunaga,1,2 Takashi Y. Nakajima,1 Teruyuki Nakajima,3 Misako Kachi,1and Kentaroh Suzuki3
Received 4 September 2001; revised 28 February 2002; accepted 25 March 2002; published 2 October 2002.

[1] In this paper, we investigate characteristics of low clouds and warm-rain production interms of droplet growth based on the effective droplet radii retrieved by a combined use ofvisible, infrared, and microwave satellite remote sensing. We propose to categorize low
clouds into the following groups: (1) nondrizzling, nonraining clouds; (2) nonraining
clouds with drizzling near the cloud top; (3) raining clouds; and (4) clouds with no clear
interpretation in terms of the effective radii derived using two different schemes. This
categorization is supported by examination of the correlation between static stability andthe retrieved results in the three ‘‘precipitating regions’’ (the Middle Pacific, South PacificConvergence Zone [SPCZ], and Intertropical Convergence Zone [ITCZ] cumulus regions)and in the four ‘‘nonprecipitating regions’’ (the Californian, Peruvian, Namibian, andeastern Asian stratus regions). The rain rate derived by Precipitation Radar (PR) provides
global characteristics consistent with our results. Californian and Peruvian stratus clouds
are found to frequently have the drizzle mode near the cloud top, whereas Namibian strati
have fewer chances to drizzle. The drizzle mode almost completely disappears in theeastern Asian region in the winter. The cloud–aerosol interaction is a promising candidate
INDEX TERMS:
for suppressing the drizzle mode formation in nonprecipitating clouds.
0320 Atmospheric Composition and Structure: Cloud physics and chemistry; 1610 Global Change:
Atmosphere (0315, 0325); 1640 Global Change: Remote sensing; 1655 Global Change: Water cycles (1836)
Citation: Masunaga, H., T. Y. Nakajima, T. Nakajima, M. Kachi, and K. Suzuki, Physical properties of maritime low clouds as retrievedby combined use of Tropical Rainfall Measuring Mission (TRMM) Microwave Imager and Visible/Infrared Scanner, 2. Climatology
of warm clouds and rain, J. Geophys. Res., 107(D19), 4367, doi:10.1029/2001JD001269, 2002.

1. Introduction[2] A major climatological importance of clouds is theirimpact on the Earth’s radiation budget. However, quantitative evaluation of the clouds’ radiative effects on the Earth’s
climate involves numerous unknown factors. Clouds thus
provide the largest uncertainty in predicting the futureclimate change such as global warming. Some of the
difficulties lie in the geometrical complexity of clouds suchas spatial inhomogeneity, brokenness, and overlapping.
Possibly more essentially, problems arise from the lack of
our knowledge of the response and sensitivity of the cloudphysical properties to possible climate changes.

1
Earth Observation Research Center, National Space Development
Agency, Tokyo, Japan.
2
Now at Department of Atmospheric Science, Colorado State
University, Fort Collins, Colorado, USA.
3
Center for Climate System Research, University of Tokyo, Tokyo,
Japan.

Copyright 2002 by the American Geophysical Union.
0148-0227/02/2001JD001269$09.00

AAC[3] Low stratiform clouds are known to play importantroles as effective coolers of the Earth by reflecting solar
radiation back to space, we hereafter designate low stratiform clouds containing stratus, stratocumulus, and fog
simply as ‘‘stratus,’’ after the notation by Zuidema andHartmann [1995]. One may categorize low clouds into a
few different types, depending on the formation mechanismand on the related environmental factors. Klein and Hartmann [1993] investigated the seasonal cycle of stratus andfound that the appearance of low clouds is closely relatedwith lower-tropospheric static stability. They identified ten
regions of active stratocumulus convection, five of which
are located off the west coasts of continents in the marine
subtropics. In these areas, stratus clouds form over relatively
cold sea surfaces where the trade inversion caps the boundary layer. One of the areas chosen by Klein and Hartmann[1993] is off the coast of California, where many marine
stratus studies have been conducted both by in situ observations and by satellite remote sensing.
[4] Stratus clouds frequently also appear over the warm
western boundary current in winter. Cold continental air
blowing over the warm sea surface produces convective
clouds triggered by the surface fluxes of heat and mois-

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MASUNAGA ET AL.: PHYSICAL PROPERTIES OF MARITIME LOW CLOUDS 2

ture, where the inversion prevents the clouds from developing beyond the boundary layer. Stratocumuli in winterover the Sea of Japan, the East China Sea, and off the east
coast of North America provide typical examples for thiscategory.
[5] In contrast to nonprecipitating low clouds such as
stratus, some maritime convective clouds at temperatures
above freezing are capable of producing warm rain.
Tropical clouds are known to constitute a broad spectrumof the cloud types. They consist of nonprecipitating
shallow cumuli or trade wind cumuli, which dominate
the cloud population, and by cumulonimbi, which dominate the convective rainfall [Johnson et al., 1999, andreferences therein]. Johnson et al. [1999] suggested thatcumulus congestus should be considered as the third
component of the convective cloud spectrum in thetropics, based on statistics of radar-echo heights from theTropical Ocean Global Atmosphere Coupled OceanAtmosphere Response Experiment (TOGA COARE) as
well as other preceding studies. They pointed out thatcumulus congestus, with detrainment through the cloud
top near the 0C stable layer, often forms precipitation by
the warm-rain process.
[6] Maritime clouds are widely known to have relatively
larger droplets with wider size spectra than continental
clouds [Squires, 1958]. This is supported by more recent
studies on the satellite-derived effective radius of liquidwater clouds [Han et al., 1994; Kawamoto et al., 2001].
This tendency implies that maritime low clouds havehigher potential to produce rainfall than continental clouds
since the presence of large droplets enables collisional
droplet growth, which is a necessary process following the
diffusional-growth phase to form raindrops through thewarm-rain process [Rogers and Yau, 1989]. Indeed, using
satellite data, Rosenfeld and Lensky [1998] demonstrated
that the collisional droplet growth takes place even near
the cloud base for maritime clouds, while growth beyond
the diffusional growth is rarely identified before glaciation
starts for continental clouds. The cloud– aerosol interaction(see section 4.2) is believed to partly account for thedifference in the cloud microphysical properties between
maritime and continental clouds. A recent theory, however,showed that static stability (or updraft velocity at the cloudbase) as well as the aerosol concentration is crucial topromote or suppress collisional growth [Pinsky and Khain,2002].
[7] Impacts of clouds on the climate system involve
various processes including radiative transfer, interactions
with aerosols, and global hydrological cycles. To reveal
cloud – climate interactions, we must therefore comprehensively understand the dynamic and microphysical processesof clouds as well as the radiative effects and complicatedfeedbacks among them. Our strategy is to clarify theclimatological characteristics of low clouds and theirdependence on environmental factors, in terms of the evolutionary status of droplet growth implied by satellite-derived
effective radii. The purpose of the present paper is to makean overall examination of possible factors determining thephysical state of low clouds. We leave future studies to go
into more detail for responding to specific interests.
[8] Masunaga et al. [2002, hereafter referred to as Paper I]
proposed a combined use of visible/infrared and micro-

wave radiometers to derive the effective droplet radii by
two different schemes. They found the results imply thatthe difference in those effective radii reflects a microphysical mechanism that expedites or suppresses the conversion of cloud water into rainfall. This paper is dedicatedto a closer examination of the effective radii to identify thepresence or absence of drizzle droplets and/or raindrops inlow clouds.
[9] Section 2 outlines the retrieval algorithm and data
adopted in this work. The results are presented in section 3.
We discuss relations of our retrievals with the geographicalfeatures of rain rate and aerosols in section 4, and give thesummary and conclusions in section 5.

2. Algorithm and Data
[10] This section briefly describes the retrieval schemeand data used in the present analysis. The major interest of
this paper is to study the effective droplet radii (defined byequation (1) below) retrieved from satellite remote sensing
over a wide spectral range from the visible to microwave.
Similar strategies were employed by Greenwald et al.
[1995] and Zuidema and Hartmann [1995], who used
Special Sensor Microwave/Imager (SSM/I), International
Satellite Cloud Climatology Project (ISCCP), and Earth
Radiation Budget Experiment (ERBE) data to obtain liquidwater path, cloudiness, and effective radius, respectively.
Lin et al. [1998a, 1998b] studied the statistics of multilayered clouds and the effective radii in the use of SSM/I
and Meteosat data.
[11] In Paper I, we proposed a new retrieval algorithm tosimultaneously derive the effective radius, optical thickness,cloud top temperature, and liquid water path by a combined
use of Visible and Infrared Scanner (VIRS) and TRMM
Microwave Imager (TMI) aboard the Tropical Rainfall
Measuring Mission (TRMM) satellite. This algorithm isoutlined as follows. First, level 1 data of VIRS and TMI
are assigned to the common global grid of 0.25 square
degrees over oceans. Combining visible, near-infrared, andthermal infrared radiances (ch1, ch3, and ch4 of VIRS,
respectively) yields the optical thickness, effective radius,and cloud top temperature [cf. Nakajima and Nakajima,
1995; Kawamoto et al., 2001]. TMI brightness temperaturesat 10.65GHz, 19.35GHz, and 37.0GHz are employed forevaluating the columnar water vapor (CWV) and liquidwater path (LWP) on the grid points identified as cloudy
by the VIRS analysis. The cloud top temperature obtained by
the VIRS analysis is used in the TMI analysis to improve theaccuracy in estimating LWP. Moreover, a cloud fraction
correction is applied to reduce errors in LWP caused bydifference in the spatial resolution between VIRS and TMI.
The microwave-retrieved LWP with the optical thickness
provides a different estimate of the effective radius from the
VIRS analysis (section 3.1).
[12] As a minor technical change in the retrieval algorithm, we modified the way of incorporating the verticalprofile of atmospheric water vapor in forward simulations
for making a lookup table. Water vapor was assumed todecrease exponentially with increasing altitude under aconstant scale height of 2.3 km in Paper I. In the present
work, the water vapor is assumed to be mixed well, i.e.,
vertically homogeneous, below the cloud base and toAAC

MASUNAGA ET AL.: PHYSICAL PROPERTIES OF MARITIME LOW CLOUDS 2

decrease linearly with increasing height toward the cloud
top, above which water vapor content decays exponentially.
The updated version is considered to represent the water
vapor profile in cloudy atmospheres better than a fixed
exponential profile as assumed before, although resultant
retrievals were found to show no substantial changes due tothe modification.
[13] Cold clouds with top temperatures below 273 K areomitted since the present analysis is focused on warm
clouds. This criterion may be too strict to define warm
clouds because very few ice crystals are detected in supercooled clouds considerably colder than 273 K. Dependence
on the threshold temperature is discussed in section 4.3.
[14] As ancillary data required for the analysis, we adopt
daily mean data of TMI-retrieved sea surface temperature(TMISST), provided by the Earth Observation ResearchCenter of the National Space Development Agency ofJapan (EORC NASDA). We also employ the global
analysis (GANAL) data, which are six-hourly objective
analysis archives provided by the Japan Meteorological
Agency. A more detailed description of the retrieval
scheme is given in Paper I. All the results in the present
paper are based on two sets of three-monthly data, i.e.,
January, February, and March (JFM) 2000 and July,
August, and September (JAS) 2000. We use the whole
global data in section 3.2, as well as local-area data for theseven sites listed in Table 1 for the regional analysis in
section 3.4. Note that we define ‘‘global’’ as the entire
scene observable from the TRMM satellite, which covers±38 in latitude.
[15] In addition to the satellite-derived cloud properties
described above, global characteristics used to describe
static stability are illustrated in section 3.2 below, where
the temperature and humidity profiles are taken from
National Center of Environmental Prediction (NCEP) Reanalysis data. The global distributions of rain rate near thesurface and of the storm height shown in section 4.1 aretaken from TRMM 3A25 products based on Precipitation
Radar (PR) data.

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Table 1. Area Definitions of the Seven Representative Sites for
Regional Analysis
Sites
Middle Pacific
ITCZ
SPCZ
Californian
Peruvian
Namibian
Eastern Asian

Coverage
160E – 180E
120W – 100W
120W – 100W
130W – 120W
90W – 80W
0E – 10E
120E – 140E

10N – 25N
5N – 15N
20S – 10S
20N – 30N
20S – 10S
20S – 10S
25N – 35N

Kawamoto et al., 2001], which is hereafter denoted by Re(NV).
The second type effective radius is derived from the relationReðMVÞ 

3LWPmicr
;
2tc

ð2Þ

ð1Þ

where LWPmicr denotes the microwave-retrieved LWP, andtc, the optical thickness at a wavelength of 0.5 mm retrieved
from shortwave analysis.
[18] The beam-filling efficiency should be considered toremove the cloud-inhomogeneity effect when microwave
estimation of LWP is linked with the shortwave retrieval.
In our scheme, the beam-filling efficiency is evaluated using
the cloud fraction, which is defined by the number ratio ofcloudy pixels to the total pixels derived from VIRS data. We
performed the cloud-fraction correction before estimating
LWPmicr to derive Re(MV) through equation (2). Paper I
pointed out that the difference in those two effective radii
could reflect a microphysical mechanism that expedites or
suppresses the conversion of cloud water into rainfall. Thisimplication is based on the intrinsic bias between Re(NV) andRe(MV), which arises from the spectral variation in the opticalproperties of water. Specifically, Re(NV) tends to be biased
toward a value near the cloud top due to strong absorption ofnear-infrared radiation by water, while Re(MV) is expected to
be close to the average in the whole cloud layer because
microwave and visible radiation do not suffer from saturation
within any cloud thickness of interest in the present work.
The difference between Re(NV) and Re(MV) should therefore
reflect the vertical inhomogeneity of droplet size inside thecloud, which is closely related with the microphysicalprocess of droplet growth. Droplet size generally increases
with increasing height and reaches a maximum near the top
in a nonprecipitating cloud layer. In contrast, a precipitating
cloud contains raindrops below or near the cloud base, andthus is detectable only by microwave measurement. In otherwords, Re(MV) should be smaller than Re(NV) for nonprecipitating low clouds, but the relation would be reversed once
cloud drops grow large enough to precipitate.
[19] A major purpose of this paper is to closely examine
Re(MV) and Re(NV) and give an overview of their dependence
on the environmental factors and the microphysical properties of low clouds. In the next section, we discuss relationsin global characteristics between static stability and thepresent retrievals.

where n(r) is the droplet size distribution. The first-type
effective radius is retrieved by using a pair of shortwave
channels in visible and near-infrared bands [Nakajima andKing, 1990; Han et al., 1994; Nakajima and Nakajima, 1995;

3.2. Low Clouds and Static Stability[20] The low cloud amount is positively correlated withlower-tropospheric static stability [Klein and Hartmann,
1993]. In this section, we present global trends of the low

3. Results[16] The cloud physical properties retrieved by combined
analysis of VIRS and TMI data are shown in this section.
We first briefly summarize the results in Paper I (section
3.1). We then illustrate global features of low cloud properties retrieved by the present analysis and static stability
calculated from NCEP Reanalysis data (section 3.2). We
introduce our working hypothesis in section 3.3 to identify
drizzle and rain in warm clouds, then examine regionalfeatures for seven representative sites (section 3.4).
3.1. A Brief Summary of Paper I[17] Paper I introduced two different ways to derive theeffective radius of cloud droplets,
R1 3r nðrÞdr
R
Re  01 2;
0 r nðrÞdr

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MASUNAGA ET AL.: PHYSICAL PROPERTIES OF MARITIME LOW CLOUDS 2

Figure 1. Cloud optical thickness (for clouds warmer than 273 K) retrieved by the VIRS analysis inthree-monthly mean in JFM (upper) and in JAS (lower) 2000. Boxes shown in the figure indicate the sites
listed in Table 1.
cloud distribution and demonstrate the relation with static
stability based on a brief theory for cumulus convection
described as follows.
[21] An adiabatic air parcel lifted by external force
reaches the lifting condensation level (LCL) when water
vapor inside the parcel is saturated and condensed into
liquid water droplets. The base of a convective cloudtherefore corresponds to LCL. In a conditionally unstable
atmosphere, the cloud air parcel lifted further along the
moist adiabat arrives at the level of free convection (LFC),
beyond which the air parcel ascends by its own buoyancy
without the help of an external force. The ascent of the airparcel is eventually halted when it looses its buoyancy at thelevel of neutral buoyancy (LNB), which roughly gives thecloud top height. LNB is expected to be low in altitude
where the boundary layer is capped by the strong inversion.
In contrast, LNB could be much higher near the tropopause
in the tropical convergence zones. Furthermore, an LFC
significantly lower in height than the freezing level may
imply that cumulus convection would allow considerable
droplet growth even for warm clouds, although warm rain isunlikely to form if LFC is so high close to LNB that strong
updrafts of air promoting droplet growth are not expected.
[22] As an indicator of static stability or inversion
strength, we calculated the atmospheric temperatures at

LFC and LNB (hereafter denoted by the LFC temperatureand the LNB temperature) from the NCEP Reanalysis data.
The dry adiabatic lapse-rate is integrated to obtain thetemperature within the air parcel, Tp(z), from the surface
to LCL, above which the integration is performed along the
moist adiabat until it is equal to the ambient atmospherictemperature, Ta(z). The altitude where Tp(z) meets Ta(z) firstafter the air parcel leaves the surface is defined as LFC.
Further integration along the moist adiabat is performed
until Tp(z) reaches Ta(z) again, where LNB is defined.
[23] Figure 1(2) shows the cloud optical thickness
retrieved by our VIRS analysis (the LNB temperature) inthree-monthly averages in JFM and JAS 2000. Note that the
optical thickness in Figure 1 is that of low clouds because of
the warm-cloud criterion, i.e., the cloud top temperature
should exceed 273 K. Boxes in the figures represent thesites that we chose for regional analysis (summarized inTable 1), which is discussed in section 3.4. As mentioned in
section 1, strong inversions, and thus low altitudes of LNB,
are observed off the west coasts of continents in thesubtropics, e.g., Californian, Peruvian, and Namibian areas.
In these areas, the LNB temperature exceeds 0C, and thus
clouds are not allowed to develop beyond the freezing level.
The optical thickness of low clouds (Figure 1) is relatively
large, typically larger than 10, in those areas. This result isMASUNAGA ET AL.: PHYSICAL PROPERTIES OF MARITIME LOW CLOUDS 2

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Figure 2. Temperature at the level of neutral buoyancy (LNB) calculated from NCEP Reanalysis data inthree-monthly mean in JFM (upper) and in JAS (lower) 2000. Boxes shown in the figure indicate the sites
listed in Table 1.
fully consistent with Klein and Hartmann [1993], whodemonstrated that appearance of low clouds positively
correlates with the inversion strength, although they usedcloud amount and the potential temperature difference
instead of optical thickness and the LNB temperature.
[24] The most prominent feature in Figure 1 is the hornlike structure with large optical thickness extending fromthe east coast of China to the midlatitude Pacific in JFM. As
also mentioned in section 1, stratus clouds frequently appear
in the East China Sea in winter, partly contributing to thisstructure. These low clouds, however, develop as blown
eastward to deeper clouds capable of yielding heavy precipitation, and are eventually merged into the midlatitude
storm track. The horn-like feature, especially near its tip,
traces the southern edge of the storm track, where higher
and thicker clouds typical of the storm track have been
omitted from Figure 1 by the warm-cloud criterion.
[25] Figure 2 shows that the LNB temperatures over thetropical oceans are so low that convective clouds could be
developed up to the tropopause. While deep convective
clouds extending beyond the freezing level have been
excluded from our analysis, shallower cumulus clouds
warmer than 0C, which are also major components of thetropical convective cloud spectrum (section 1), are within
the scope of the present study. In contrast to stratus clouds

that appear over the cold boundary currents, cumulus clouds
over the tropical oceans are formed in a less stable atmosphere by virtue of a higher sea surface temperature and ahigher humidity resulting in a higher LFC temperature.
Figure 3 illustrates the LFC temperature calculated fromthe NCEP Reanalysis data. The LFC temperature is significantly higher than 0C in the tropical oceans, which
potentially allows rapid droplet growth in clouds evenbelow the freezing level, which would enhance the probability of producing warm rain. On the other hand, the LFC
temperature decreases almost to 0C off the coasts ofCalifornia, Peru, and Namibia. Recalling that these areas
are subjected to a strong inversion, one can deduce that afree convection layer between LFC and LNB is so thin inthese areas that droplet growth in a cloud layer would beless effective than in precipitating shallow clouds over thetropical oceans. A difference in the LFC temperature would
therefore account for the regional variation in the capabilityof warm-rain production.
[26] Paper I inferred that precipitating clouds might bediscriminated from nonprecipitating clouds by examining
Re(MV) and Re(NV); clouds are expected not to be associatedwith significant precipitation if Re(NV) exceeds Re(MV),otherwise they are raining (section 3.1). Figure 4 draws
the ratio of Re(MV) to Re(NV) retrieved from TRMM data.

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MASUNAGA ET AL.: PHYSICAL PROPERTIES OF MARITIME LOW CLOUDS 2

Figure 3. Same as Figure 2 but temperature at the level of free convection (LFC).
The global pattern in Figure 4 shows that precipitating
regions such as the Intertropical and South Pacific Convergence Zones (ITCZ and SPCZ, respectively) are clearlytraced by Re(MV)/Re(NV) larger than unity. In contrast,
Re(MV)/Re(NV) is smaller than unity over the eastern boundary
current, where the rain rate is much lower. The remarkable
resemblance in patterns between Figures 3 and 4 supports
the idea for correlation between Re(MV)/Re(NV) and thepresence of rainfall.
[27] Close examination of the Peruvian area in Figures 2
and 3 reveals that the domain having the maximum LNB
temperature is detached from the coastline, with a narrow
area between them showing the lowest LFC temperature.
This narrow area shows the local maximum in cloud optical
thickness (Figure 1) with the minimum in Re(MV)/Re(NV)(Figure 4); these trends are more prominent in JAS. These
facts suggest that clouds covering the area should containvery small droplets and be incapable of ascending from thesea surface, and thus they are probably fogs. Similar trends
are also found in the Californian and Namibian areas, butthey are not as evident as in the Peruvian area.
3.3. Detection of Drizzle and Rain[28] In the previous section we showed that low clouds
can be categorized to be precipitating or nonprecipitating interms of the ratio of Re(MV) to Re(NV). We extend this idea inthis section to include a category for drizzling clouds.

[29] The formation of warm rain begins with the onset ofcollisional droplet growth, which triggers generation of aseparate peak at 100 mm in the droplet size spectrum, i.e., thedrizzle mode [Rogers and Yau, 1989]. Rosenfeld and Gutman[1994] showed that 14 mm in Re(NV) is a threshold value above
which clouds contain precipitation size hydrometeors using asatellite imager and weather radars. Gerber [1996] concluded
that the threshold discriminating heavy-drizzle stratocumuli
from light-drizzle ones is an effective radius of 16 mm using
airborne probes. A detailed microphysical simulation for
droplet growth illustrated that strong collisions start wheneffective radius attains about 15 mm [Pinsky and Khain,2002]. These studies independently reached almost the sameconclusion that the threshold for occurrence of drizzle is aneffective radius of 15 mm.
[30] Compiling all the implications given in the present
and previous sections, we propose the following categorization in terms of Re(NV) and Re(MV)/Re(NV), or the inverse ofg  Re(NV)/Re(MV) by the definition in Paper I, to identify
nonprecipitating, drizzling, and precipitating clouds fromsatellite data. Figure 5 is a schematic illustration for thefollowing categorization, where any given set of Re(NV) andRe(MV)/Re(NV) specifies the category to which the cloudshould belong.
1. The first category (domain 1 in Figure 5) is defined byRe(NV) < 15 mm and Re(MV)/Re(NV) < 1. This type of cloud is
not associated with drizzle mode or with precipitation.

MASUNAGA ET AL.: PHYSICAL PROPERTIES OF MARITIME LOW CLOUDS 2

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Figure 4. Ratio of Re(MV) to Re(NV) in three-monthly mean in JFM (upper) and in JAS (lower) 2000.
Boxes shown in the figure indicate the sites listed in Table 1.

3.4. Regional Characteristics[32] Figures 6 (JFM) and 7 (JAS) show scatter diagramsfor Re(MV)/Re(NV) versus Re(NV) (cf. Figure 5). Each panel in
Figure 6 gives statistics for each of the seven representative

sites listed in Table 1 along with global statistics. We haveomitted very tenuous clouds with optical thickness smaller
than 4 in Figures 6 and 7 to reduce contamination of
uncertainties in the surface emission seen through the cloud.

Re(MV) / Re(NV)2. Clouds with Re(NV) > 15 mm and Re(MV)/Re(NV) < 1(domain 2) belong to the second category. The criterion ofRe(MV) > 15 mm implies that the clouds are probablydrizzling, but the drizzle mode is confined to near the cloud
top as long as Re(MV)/Re(NV) remains below unity. Those
clouds are unlikely to develop enough to produce considerable amounts of precipitation, although formation of thedrizzle mode has begun near the cloud top through cumulus
convection.
3. The third category consists of clouds with Re(NV) > 15mm and Re(MV)/Re(NV) > 1 (domain 3), which are expected tocontain raindrops in appreciable numbers.
4. We do not have a convincing interpretation of theremaining category of Re(NV) < 15 mm and Re(MV)/Re(NV) > 1(domain 4). As a possible explanation, low precipitating
clouds overlaid by nonprecipitating midlevel clouds may befallen into this category [Lensky and Rosenfeld, 1997].
Validation studies, however, are necessary to confirm or
reject this speculation.
[31] We apply our retrievals to this categorization in thesubsequent section to figure out climatological characteristics on the microphysical states of low clouds.

4.

3.

1.

2.

1

15 micronRe(NV)

Figure 5. A schematic illustration to categorize themicrophysical status of low clouds (see section 3.3 fordetails).

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MASUNAGA ET AL.: PHYSICAL PROPERTIES OF MARITIME LOW CLOUDS 2
Middle Pacific
Re(MV)/Re(NV)

Re(MV)/Re(NV)Global
5
4
3
2
1
0
-1
0

5

5
4
3
2
1
0
-1

10 15 20 25 30
Re(NV) [micron]

0

5

SPCZ
Re(MV)/Re(NV)

Re(MV)/Re(NV)

ITCZ
5
4
3
2
1
0
-1
0

5

5
4
3
2
1
0
-1

10 15 20 25 30

05Re(NV) [micron]

Peruvian
Re(MV)/Re(NV)

Re(MV)/Re(NV)

0

5

5
4
3
2
1
0
-1

10 15 20 25 30
Re(NV) [micron]

0

5

0

5

10 15 20 25 30
Re(NV) [micron]10 15 20 25 30
Re(NV) [micron]
Eastern Asian

Re(MV)/Re(NV)

Re(MV)/Re(NV)Namibian
5
4
3
2
1
0
-1

10 15 20 25 30
Re(NV) [micron]

Californian
5
4
3
2
1
0
-1

10 15 20 25 30
Re(NV) [micron]

5
4
3
2
1
0
-1
0

5

10 15 20 25 30
Re(NV) [micron]Figure 6. Ratio of Re(MV) to Re(NV) versus Re (NV) in JFM 2000. Location of each site is listed in Table 1.
Averages of Re(MV), Re(NV), and Re(MV)/Re(NV) for each site
are listed in Table 2.
[33] A common tendency identified throughout Figure 6
is that the density of scattered points appears to be largest
where Re(MV)/Re(NV) is equal to or slightly less than unity.
However, the upper four panels (the Middle Pacific, ITCZ,
SPCZ, and the global scene) contain many points dispersed
far beyond the Re(MV)/Re(NV) = 1 line, whereas many fewer
points surpass it in the lower four (the Californian, Peruvian, Namibian, and eastern Asian regions). This contrast ismore clearly demonstrated in Table 2, where Re(MV)/Re(NV)exceeds or nearly equals unity for the Middle Pacific, ITCZ,
and SPCZ, but is slightly smaller than unity for the global
mean and much smaller for the other four. This result, whichis comparable to that in Figure 4, is fully consistent with theidea that Re(MV)/Re(NV) reflects the probability of rain
formation in low clouds.
[34] Figures 6 and 7 and Table 2 contain some negativevalues of Re(MV) and Re(MV)/Re(NV) since microwave estima-tion of LWP could produce negative values because of
uncertainties in the surface emissivity. Negative effective
radii are physically meaningless, but we did not exclude thembecause LWP could be seriously overestimated if negative
LWPs were excluded from statistics [Lin and Rossow, 1994].
[35] For convenience, we hereafter designate the Middle
Pacific, ITCZ, and SPCZ as ‘‘precipitating regions’’ and theCalifornian, Peruvian, Namibian, and eastern Asian sites as‘‘nonprecipitating regions.’’ This classification is clearly
defined depending on whether the average value ofRe(MV) /Re(NV) for each site is larger than the global meanor not (Table 2), and is supported as well by the global
distribution of rain rate obtained from Precipitation Radar
data (section 4.1). Figures 6 and 7 are examined below inmore detail for each of the precipitating and nonprecipitating regions.
3.4.1. Precipitating Regions[36] Table 2 shows that both Re(MV) and Re(NV) tend tohave larger values in the precipitating regions than in the

MASUNAGA ET AL.: PHYSICAL PROPERTIES OF MARITIME LOW CLOUDS 2

0

5

5
4
3
2
1
0
-1

10 15 20 25 30
Re(NV) [micron]

0

5

0

5

5
4
3
2
1
0
-1

10 15 20 25 30

05Re(NV) [micron]

Peruvian
Re(MV)/Re(NV)

Re(MV)/Re(NV)

0

5

5
4
3
2
1
0
-1

10 15 20 25 30
Re(NV) [micron]

0

5

0

5

10 15 20 25 30
Re(NV) [micron]10 15 20 25 30
Re(NV) [micron]
Eastern Asian

Re(MV)/Re(NV)

Re(MV)/Re(NV)Namibian
5
4
3
2
1
0
-1

10 15 20 25 30
Re(NV) [micron]

Californian
5
4
3
2
1
0
-1

10 15 20 25 30
Re(NV) [micron]
SPCZ

Re(MV)/Re(NV)

Re(MV)/Re(NV)

ITCZ
5
4
3
2
1
0
-1

3-9

Middle Pacific
Re(MV)/Re(NV)

Re(MV)/Re(NV)Global
5
4
3
2
1
0
-1

AAC

5
4
3
2
1
0
-1
0

5

10 15 20 25 30
Re(NV) [micron]Figure 7. Same as Figure 6 but in JAS 2000.

nonprecipitating regions. The contrast between these tworegions is more pronounced in Re(MV) than in Re(NV), whichis responsible for the difference in variation of Re(MV)/Re(NV).
Large excess of Re(MV) over Re(NV) in the precipitating
regions is considered to be attributed to the presence ofraindrops (section 3.1).
[37] Among the precipitating regions, the smallest values
are found in ITCZ for any of Re(MV), Re(NV), or their ratio
both in JFM and in JAS in Table 2. This seemingly implies
that ITCZ has the lowest probability of rain formation in low
clouds among those three sites. However, it does not indicatethat ITCZ provides less precipitation than SPCZ and the
Middle Pacific because heavy precipitation over the tropicaloceans is contributed mainly by deep convective clouds
through the cold-rain process, which were excluded from
our analysis by the warm-cloud criterion. Actually, theMiddle Pacific and SPCZ by our definition are not theregions with heaviest precipitation in the tropics. (Note thatthe region defined as SPCZ in Table 1 is eastwardly offcentered from the usual notation.) Considerable seasonalvariation is observed in the Middle Pacific, where data points
are heavily dispersed (Figure 7) and Re(MV) is found even
Table 2. Three-Monthly Means of Re(MV) and Re(NV), and the
Ratio of Re(MV) to Re(NV) for Each Site Listed in Table 1
Sites

GlobalMiddle Pacific
ITCZ
SPCZ
Californian
Peruvian
Namibian
East Asian

JFM

JAS

Re(MV),mm

Re(NV),mm

Ratio

Re(MV),mm

Re(NV),
mm

Ratio

13.57
25.06
13.65
23.42
8.15
10.29
3.86
6.11

14.83
16.74
13.27
17.79
15.06
14.88
12.83
9.41

0.86371.51811.07661.32270.51550.65770.21720.6292

12.40
30.85
13.63
21.24
3.32
6.78
5.17
1.34

14.90
17.86
15.38
17.31
12.55
14.04
10.87
12.11

0.7547
1.74780.87141.20380.17350.44190.4354
0.0491

AAC

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MASUNAGA ET AL.: PHYSICAL PROPERTIES OF MARITIME LOW CLOUDS 2

larger (Table 2) for JAS, implying that precipitating clouds
appear more frequently in summer than in winter in this area.
Further interpretation of the Re(MV)/Re(NV) versus Re(NV)diagram for the precipitating regions will be discussed in
section 4.1.
3.4.2. Nonprecipitating Regions[38] Table 2 illustrates that the nonprecipitating regions
are separated from the precipitating regions by an averageRe(NV) of 15 mm, which accords with the drizzle formationthreshold (section 3.3). Closer examination of Figures 6 and7 reveals that individual clouds frequently surpass 15 mm
in Re(NV) in the Californian and Peruvian regions, indicatingthat low clouds often include the drizzle mode there.
Drizzle droplets, however, are unlikely to grow into largeraindrops because Re(MV)/Re(NV) remains below unity inmost cases even when the drizzle mode is identified near
the cloud top. Compared to the Californian and Peruvian
regions, the drizzle mode is less frequently identified in the
Namibian region and it almost completely disappears in
the eastern Asian region in JFM. The drizzle mode in
those regions may be quenched by the cloud – aerosolinteraction. We will revisit this subject in section 4.2.
There could be other meteorological factors that suppress
the drizzle mode, but we consider that the cloud– aerosolinteraction is the most plausible candidate for thefollowing reasons.
[39] First, the Californian, Peruvian, and Namibian stratus regions are under similar meteorological conditions,
i.e., over cold boundary currents off the west coasts of thecontinents, while only eastern Asian stratus is formed over
the warm current off the east coast. This difference in themeteorological conditions could not account for the contrast between Californian/Peruvian regions and the Namibian/eastern Asian regions. Second, if the suppression of
the drizzle mode as seen in the eastern Asian and Namibian regions is not due to large CCN concentrations, adifference in static stability should be responsible forsuppressing the droplet growth. Figures 2 and 3, however,show no notable evidence for a difference in static stability, or in LNB and LFC temperatures, between the Namibian/eastern Asian regions and the other two stratus
regions.
[40] Extremely small values of Re(MV) seen in Namibianand eastern Asian regions (Table 2) are observed in broken
clouds with low LWP and small cloud fractions, e.g., fairweather cumulus. In such cases, microwave estimation of
LWP is liable to suffer from relatively large errors becauseof uncertainties in the surface emissivity. Therefore, reliability of Re(MV) may not be ensured when it shows an
exceptionally small value, but this does not seriously
damage our conclusive remarks.

4. Discussions
4.1. Rain Rate Near Surface Rain Rate[41] The previous section was devoted to illustrating that
an idea proposed in section 3.3 is supported by the
retrievals from satellite observations shown in Figures 6
and 7, which is consistent with the geographical characteristics in lower-tropospheric static stability. In this section,
we investigate the correlation between raining and/or
drizzling clouds identified by our classification and rainfall

observed by Precipitation Radar (PR) aboard the TRMM
satellite.
[42] PR data should have been omitted when the cloud
top temperature is lower than 273 K for comparing our
results directly with the PR rain rate. However, we present
the total rainfall without screening in Figure 8 because thepurpose of this section is not only validating our results but
also showing the climatological characteristics of warm rainin the context of the total rainfall. The rain type (cold orwarm) is indicated in terms of the storm height, which isdefined by the altitude of the highest radar echo detected byPR.
[43] Figure 8 shows the three-monthly mean rain rate near
the surface derived from PR along with the atmospherictemperature at the storm height (hereafter called stormheight temperature). We calculated the storm-height temperature assuming a temperature lapse-rate of 6.5 K/km fromsea surface temperature (and hence the storm-height temperature is drawn only over oceans in Figure 8). Storm-heighttemperatures substantially above 0C indicate that warm
rain dominates the precipitation processes in that region,
whereas cold rain is likely if the storm-height temperature isfar below 0C. Although this latter statement is not always
true because liquid water hydrometeors often exist below
temperatures of 15C, the storm-height temperature provides a tentative guideline to roughly illustrate regional
trends of precipitation processes. Note that PR is notsensitive to ice particles unless they have grown very large,
and therefore the storm height for cold rain only gives thelower limit for the actual height at which precipitation
begins.
[44] Among the nonprecipitating regions identified in
section 3.4 above, the Californian, Peruvian, and Namibianareas are confirmed to have rain rates of less than 1 mm/hr,
which is comparable to the lower detection limit of rainfall
by PR. California in JFM appears to have slightly higher
rain rates than in JAS since the midlatitude storm track isshifted southward (closer to this site) in JFM as seen in
Figure 8. Peru does also under the influence of doubled
ITCZ in JFM. This seasonal variation is consistent with
Table 2, where the ratio of effective radii is larger in JFM
than in JAS for both of the Californian and Peruvian sites.
The eastern Asian area is found to have considerable rainfallwith rain rates of 2 – 5 mm/hr, even though it is categorized
as a nonprecipitating region. This seems to be a contradiction, but it actually is not, because rainfall in the
midlatitude is mainly due to the cold-rain process and mostwarm clouds found there are nonprecipitating. Figure 8
shows that the storm-height temperature in eastern Asia is
indeed lower than 0C.
[45] The precipitating regions can be divided into two
categories by average rain rates, heavily precipitating areas
with typical rain rates exceeding 2 mm/hr (Middle Pacific in
JAS and ITCZ) and moderately precipitating areas (Middle
Pacific in JFM and SPCZ). We again notice that the region‘‘SPCZ’’ by our definition (Table 1) is off-center from thearea with heaviest precipitation in the South Pacific. The
moderately precipitating regions have storm-height temperatures above 10C, strongly indicating that rainfall in thoseregions is dominated by the warm-rain process from precipitating shallow clouds. In contrast, correlation between
the classification proposed in Figure 5 and rain rate is less

MASUNAGA ET AL.: PHYSICAL PROPERTIES OF MARITIME LOW CLOUDS 2

AAC

3 - 11Figure 8. Three-monthly-mean rain rate near the surface derived from PR in JFM (upper) and JAS(lower) 2000. Contours delineate the atmospheric temperature at the storm height, which is calculated
from the PR storm height on the assumption of a temperature lapse-rate of 6.5 K/km from sea surface
temperature given by TMISST. Red-colored and purple-colored contours denote the storm-heighttemperatures beyond and below 0C, respectively. Boxes shown in the figure indicate the sites listed inTable 1.

clear in heavily precipitating regions since deep convective
clouds play significant roles in the total rainfall throughthe cold-rain process. In fact, it is curious that ITCZ
shows only a weak sign of rainfall in Table 2, comparedto less precipitating regions such as SPCZ and the Middle
Pacific. A possible explanation for this tendency is thatsubsidence from coexisting deep convection may tend to
suppress growth of neighboring shallow clouds. However,further examination of the dynamical interaction among
tropical cumulus clouds is outside the scope of the present
study.
[46] We avoided choosing the rainiest region in thetropics, e.g., the western Pacific warm pool, as a representative site because low clouds over the warm pool were very
infrequently detected. This is the same reason why we haveshifted our ‘‘SPCZ’’ eastward from the usual definition.
This is presumed to be attributed to frequent appearance ofhigh clouds obscuring lower clouds in those areas where
active deep convection moistens the upper troposphere. We

have indeed confirmed that frequency of low-cloud detection increases with decreasing threshold temperature for the
warm-cloud criterion over the warm pool (not shown). Moredetailed investigation involved with the cloud overlapping,
however, is also beyond the scope of this work and is thus
left for future studies.
4.2. Interaction With Aerosols[47] We showed in section 3.4.2 that the drizzle mode issuppressed for stratus clouds in the Namibian and eastern
Asian regions, in contrast to the Californian and Peruvian
stratus regions. It was also implied there that the cloud–aerosol interaction is a candidate for suppressing thedrizzle mode. The cloud – aerosol interaction is increasing
in climatological importance because it plays importantroles both in the cloud microphysics and in influencing
the Earth’s radiation budget, i.e., the aerosol indirect
effect, as described below. This section is devoted to
introducing the cloud– aerosol interaction and to discus-

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MASUNAGA ET AL.: PHYSICAL PROPERTIES OF MARITIME LOW CLOUDS 2

sing the relation between past studies and the results of thispaper.
[48] Hydrophilic aerosols activated as cloud condensation
nuclei (CCN) affect the cloud physical properties. Twomey[1977] showed that an increase of the aerosol concentration
enhances the cloud reflectivity in the global average.
Coakley et al. [1987] and Radke et al. [1989] confirmed
enhancement of the cloud reflectivity due to the ship trackeffluence, and Kaufman and Fraser [1997] found the same
trend caused by carbonaceous aerosols generated by biomass burning. Nakajima et al. [2001] investigated thecorrelation between the cloud and aerosol concentrations
by means of global analysis of satellite data. Bréon et al.
[2002] also found that the effect of aerosols on cloud
microphysics occurs on a global scale using satellite databy means of a different retrieval scheme from that of
Nakajima et al. [2001].
[49] In addition to changes in the cloud reflectivity, theshrinking of cloud droplets in response to an increase in theaerosol concentration would suppress the formation ofdrizzle, and hence would extend the cloud lifetime[Albrecht, 1989]. By a combined use of the radiometers
and radars aboard the TRMM satellite, Rosenfeld [2000]
demonstrated that urban and industrial air pollution can
suppress rainfall. Enhanced cloud reflectivity and extended
cloud lifetime as a result of interaction with aerosols isknown as the aerosol indirect effect, which has become tobe recognized as one of the major cooling sources of the
Earth. The aerosol indirect effect, however, introduces alarge uncertainty in predicting global warming [IPCC01,
2001].
[50] It is interesting to compare the findings by Nakajima
et al. [2001] with occurrence or disappearance of thedrizzle mode in the nonprecipitating regions as discussed
in section 3.4, although their analysis is based on annualmean retrievals in 1990. According to Nakajima et al.
[2001], the strongest positive correlation between the number concentrations of cloud droplets and aerosols was foundover the East China Sea, which infers that numerous anthropogenic aerosols emitted from China cause cloud droplets toshrink in the surrounding areas. Evidence of the cloud –aerosol interaction was also identified off the west coast of
Namibia, and less clearly over the ocean near Peru, but nosign of such interactions was found in the Californian area.
Recalling the findings in section 3.4, where drizzling clouds
are frequently found in the Californian and Peruvian regions
but less frequently in the Namibian and completely disappear in the eastern Asian, one finds that the cloud– aerosolinteraction is a promising candidate for dominating droplet
growth in nonprecipitating clouds, for which a high aerosol
concentration suppresses the drizzle mode.

Yau, 1989]. There is a wide variety in actual clouds attemperatures between 0C and 40C, depending onwhether cloud particles are in the purely liquid phase, purely
ice phase, or a mixed phase. Our threshold of 273 K assuresa sufficient condition for clouds to be in the liquid phase andmay be overly strict in some cases. To estimate dependenceof the threshold temperature on the statistics of the retrieved
effective radius, we performed another analysis in the same
way as presented in section 3.4 except for a threshold
temperature at 258 K instead of 273 K.
[52] Table 3 lists averages of Re(MV) and Re(NV), and theirratio for the threshold temperature of 258 K. In comparison
with Table 2, the decreased threshold temperature at everysite both in JFM and in JAS produces no significant
changes in Re(NV), although a slightly increasing tendency
of about 1 mm with decreasing threshold temperature isobserved in the eastern Asian region. In contrast, Re(MV) is
considerably decreased by the decreased threshold temperature. This correlation of Re(MV) with the threshold temperature is accounted for by the increasing contribution of ice
crystals as the cloud temperature decreases. For clouds
containing an ice-water mixture, the estimate of Re(MV)using equation (2) should be rewritten as

4.3. Dependence on the Warm-Cloud Criterion[51] Clouds with top temperatures below 273 K havebeen omitted from our analysis since the present study is
focused on liquid water clouds. Clouds, however, often
contain supercooled water droplets even if the water temperature is considerably lower than 0C. Cloud droplets are
known to freeze spontaneously at temperatures as low as40C, whereas ice crystals usually appear in a cloud inappreciable numbers when the temperature drops below
15C through heterogeneous nucleation [Rogers and[53] In this paper, we investigate the characteristics oflow clouds and warm-rain production in terms of droplet
growth in warm clouds, based on the effective droplet radii
retrieved by a combined use of visible, infrared, and microwave satellite remote sensing. The present study is focusedon an overall examination, and thus more detailed investigations of specific factors such as the cloud – aerosolinteraction are left to future work.
[54] The retrieval algorithm, described in detail in Paper I,
is designed to be applied to VIRS and TMI aboard theTable 3. Same as Table 2 Except for the Threshold Temperatureof 258 K for the Warm-Cloud Criterion Instead of 273 K
Sites

JFM

JAS

Re(MV),mm

Re(NV),mm

Ratio

Re(MV),mm

Re(NV),
mm

Global10.50
Middle Pacific 19.73
ITCZ
8.61
SPCZ
19.89
Californian
7.32
Peruvian
8.78
Namibian
1.77
Eastern Asian
5.65

15.07
16.50
14.06
17.88
15.08
14.92
12.87
10.16

0.6602
1.19040.65891.12230.45870.5456
0.04180.5518

9.16
11.28
7.90
20.03
2.36
6.30
4.60
5.25

15.34
0.534717.73
0.610815.80
0.463617.31
1.130812.57
0.093014.05
0.404610.84
0.378113.84 0.4875

ReðMVÞ 

3TWP
;
2tc

Ratio

ð3Þ

where TWP stands for the total water path including both
liquid and ice water. However, microwave sensors would
miss the ice water component because of their insensitivity
to ice crystals, which results in underestimation of Re(MV) inequation (3). As a consequence, we prefer the threshold
temperature of 273 K as the warm-cloud criterion in order toavoid underestimating Re(MV) due to contamination of ice
crystals.

5. Summary and Conclusions

MASUNAGA ET AL.: PHYSICAL PROPERTIES OF MARITIME LOW CLOUDS 2

TRMM satellite to evaluate the cloud optical thickness,cloud top temperature, LWP, and the cloud effective radii.
In particular, LWP and the effective radius are derived in thetwo different ways using visible and infrared radiances andthe combination of visible radiance and microwave brightness temperatures. These two effective radii, Re(NV) andRe(MV), do not accord with each other in general because
Re(NV) tends to be biased toward the value near cloud top
while Re(MV) is close to the average within the whole cloudlayer. The ratio of those two effective radii, Re(MV)/Re(NV), is
therefore expected to represent the vertical inhomogeneity ofthe effective radius in a cloud layer. For nonprecipitating
cumulus, the mean droplet size is known to increase withincreasing height due to droplet growth and coalescence inan ascending air parcel, and hence Re(MV) would be slightly
smaller than Re(NV). In contrast, Re(MV)/Re(NV) should exceed
unity if clouds produce raindrops that fall below the cloudbase. These considerations, along with observational andtheoretical implications by past studies, lead us to categorize
low clouds into the following four groups: (1) nondrizzling,
nonraining clouds (Re(NV) < 15 mm, Re(MV)/Re(NV) < 1), (2)nonraining clouds with drizzling near the cloud top (Re(NV) >15 mm, Re(MV)/Re(NV) < 1), (3) raining clouds (Re(NV) > 15mm, Re(MV)/Re(NV) >1) (section 3.3), and (4) other clouds(Re(NV) < 15 mm and Re(MV)/Re(NV) > 1) with no clear
interpretation. Low raining clouds with overlying nonprecipitating clouds might belong to this final category, but wehave no verification.
[55] We chose seven representative sites for the regional
analysis (Table 1). The Californian, Peruvian, and Namibiansites are characterized by optically thick stratus clouds(Figure 1), which are capped by a strong inversion as
indicated by calculated LNB (level of neutral buoyancy,
Figure 2). This is consistent with the findings by Klein andHartmann [1993]. All of those sites exhibit values of Re(MV)/
Re(NV) less than unity in average (Figure 4 and Table 2),
which supports our categorization. Californian and Peruvian
stratus clouds are found to often surpass 15 mm in Re (NV) or,in other words, to frequently have the drizzle mode near the
cloud top, whereas Namibian strati have fewer chances todrizzle. Stratus clouds are abundant also in the eastern Asian
region in winter, but occurrence of the drizzle mode is rarely
identified there in contrast to the other three stratus regions.
The cloud– aerosol interaction is a promising candidate forsuppressing formation of the drizzle mode in nonprecipitating clouds (section 4.2).
[56] The Californian, Peruvian, Namibian and eastern
Asian stratus regions, designated as ‘‘nonprecipitating
regions’’ for convenience, are distinguished from ‘‘precipitating regions’’, comprised of the Middle Pacific, ITCZ,
and SPCZ cumulus regions, depending on whether the
average value of Re(MV)/Re(NV) is smaller or larger than
the global mean (Table 2).
[57] Warm-rain production requires an unstable layer
below the freezing level so thick as to allow the collisional droplet growth to yield raindrops. The rain rate near
the surface obtained by PR shows that the Middle Pacificin JFM and SPCZ (at its eastern edge by our definition)
have moderate rainfall. In these regions, deep convective
clouds that form heavy precipitation through the cold-rain
process do not appear frequently because of the trade
inversion, and warm rain is the only source to provide

AAC

3 - 13

precipitation. Precipitating shallow cumuli such as congestus clouds that do not develop far beyond the 0Clayer probably contribute to warm rain in the tropics[Johnson et al., 1999]. Further studies are necessary fortropical regions with heavier precipitation, e.g., the western Pacific warm pool (not shown in this work) and ITCZ,
since the present work is focused on low clouds and thewarm-rain process.
[58] The above findings all lead us to the following
general conclusions on the mechanism determining the
microphysical state of low clouds.
1. Based on combined analysis of shortwave andmicrowave measurements, nondrizzling clouds, drizzling
clouds, and raining clouds are discriminated on the twodimensional plane constructed by Re(NV) and Re(MV)/Re(NV).
2. Nonprecipitating clouds are composed of drizzling(but not raining) clouds and nondrizzling clouds. Althoughboth types of nonprecipitating clouds are formed under thestrong inversion over the boundary current, the drizzle
mode is suppressed if any external forcing is exerted toprevent droplet growth, probably by the presence ofabundant aerosols.
3. The drizzle mode can be converted into warm rainover the tropical and subtropical oceans having high sea
surface temperature and high humidity.
[59] There remain many unresolved issues. Detailed
investigation of the cloud – aerosol interaction for nonprecipitating stratus clouds was beyond the scope of the present
study. Moreover, the conversion efficiency from the drizzle
mode to warm rain would be affected by the aerosol
concentration as well as the surface temperature and humidity for continental and coastal clouds [Rosenfeld, 2000]. To
investigate the radiative effects of clouds on climate, cloud
lifetime as well as droplet size should be estimated from theefficiency of conversion from clouds into rainfall. Middle
and high clouds, as well as low clouds, should be included
inside the scope to discuss the Earth’s energy budget in
total, which involves studying the cold-rain process inaddition to the warm-rain process. These are formidable
issues to resolve, but some of them will be subjects in our
subsequent work.
[60] Acknowledgments. VIRS(1B01), TMI(1B11) and PR(3A25)
data were provided by NASA Goddard Space Flight Center, and GANAL
data by the Japan Meteorological Agency. TMISST (Version 2.0) was
produced and supplied by NASDA Earth Observation Research Center.
NCEP Reanalysis data were provided by the NOAA-CIRES Climate
Diagnostics Center, Boulder, Colorado, USA.

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M. Kachi and T. Y. Nakajima, Earth Observation Research Center,
National Space Development Agency, Tokyo 104-6023, Japan.
H. Masunaga, Department of Atmospheric Science, Colorado State
University, Fort Collins, CO 80523, USA. (masunaga@atmos.colostate.edu)
T. Nakajima and K. Suzuki, Center for Climate System Research,
University of Tokyo, 4-6-1 Komaba, Meguro-ku, Tokyo 153-8904, Japan.