Diurnal phase of late-night against late-afternoon of stratiform and convective precipitation in summer southern contiguous China
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- Yu, R., Yuan, W., Li, J. et al. Clim Dyn (2010) 35: 567. doi:10.1007/s00382-009-0568-x
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Using the tropical rainfall measuring mission (TRMM) Precipitation Radar (PR) observations combined with the surface rain gauge data during 1998–2006, the robust diurnal features of summer stratiform and convective precipitation over the southern contiguous China are revealed by exploring the diurnal variations of rain rate and precipitation profile. The precipitation over the southern contiguous China exhibits two distinguishing diurnal phases: late-night (2200–0600 LST) and late-afternoon (1400–2200 LST), dependent on the location, precipitation type and duration time. Generally, the maximum rain rate and the highest profile of stratiform precipitation occur in the late-afternoon (late-night) over the southeastern (southwestern) China, while most of the stratiform short-duration rain rate tends to present late-afternoon peaks over the southern China. For convective precipitation, the maximum rain rate and the highest profile occur in the late-afternoon over most of the southern contiguous China, while the convective long-duration rain rate exhibits late-night peaks over the southwestern China. Without regional dependence, the convective precipitation exhibits much larger amplitude of diurnal variations in both near surface rain rate and vertical extension compared with stratiform precipitation and the convective rain top rises most rapidly between noon and afternoon. However, there are two distinctive sub-regions. The diurnal phases of precipitation there are very weakly dependent on precipitation type and duration time. Over the eastern periphery of the Tibetan Plateau, the maximum rain rate and the highest profile of either convective or stratiform precipitation occur in the late-night. Over the southeastern coastal regions, both the near surface rain rate and rain top of convective and stratiform precipitation peak in the late-afternoon.
KeywordsDiurnal cycle Stratiform precipitation Convective precipitation Rainfall duration
Due to its significant influences on Earth’s weather and climate, the diurnal cycle of precipitation has been widely studied using both ground based rain gauge records and satellite observations (Wallace 1975; Dai et al. 1999; Dai 2001; Yang and Slingo 2001; Sorooshian et al. 2002; Nesbitt and Zipser 2003). Large differences exist in the diurnal variations between the open oceans and the continents. The diurnal amplitude is usually larger over the continents than open oceans. Oceanic deep convection tends to reach its maximum in the early morning and continental convection generally peaks in the late afternoon. Moreover, affected by the complex land–sea and mountain–valley breezes, there are interesting regional variations over the continents (Yang and Slingo 2001). The mainland of China not only occupies the largest continental area over East Asia Monsoon region, but also is characterized by complex land-sea contrast and irregular mountain-valley distributions. Therefore, the contiguous China exhibits unique climatic characteristics. Using rain gauge records, Yu et al. (2007a) pointed out that summer precipitation over the contiguous China has distinct diurnal variations with considerable regional features. Over the southern inland China and northeastern China, summer precipitation peaks in the late afternoon, while over the eastern periphery of the Tibetan Plateau it peaks around midnight. To further understand the diurnal variation of rainfall over the central eastern China, Yu et al. (2007b) classified the precipitation into different categories based on the duration time. The results suggest that the duration of a rainfall event is a critical factor to determine the diurnal phase. Their results show that long-duration rainfall events tend to have their maximum hourly rainfall around the early morning, while short-duration rainfall events tend to peak around the late afternoon. The seasonal variation of rainfall diurnal cycle in the southern contiguous China was also examined by Li et al. (2008) and it is both regional and durational dependent.
Based on rain gauge data, analyses of diurnal cycle are mainly focused on the rainfall amount and frequency of all kinds of precipitation. Nevertheless, the total rainfall is constituted of the stratiform precipitation associated with relative stable stratification and convective precipitation related to vigorous overturning. Analysis of the components modulated by different mechanisms would be helpful to understand the characteristics of total rainfalls. Meanwhile, differences exist in the vertical distributions of latent heating and horizontal mass divergence between stratiform and convective precipitation regions. Investigating them separately would be useful to better measure the feedback of total rainfalls to the atmosphere (Houze 1997). Previous researches have been mostly focused on the diurnal phase and amplitude of precipitation amount, frequency, intensity and the like, but the diurnal variation of the precipitation vertical structure is rarely revealed. Tao et al. (1993) pointed out that the precipitation profile reflects both microphysical and thermal-dynamical processes associated with precipitation formation. For example, the mean profile patterns of convective and stratiform precipitation are different. The former usually has three (or four) layers from rain top to near surface: crystal, mixed ice and water, and droplet collision (evaporation) layer. In contrast, the latter commonly has three layers: crystal, mixed ice and water, and water layer (Liu and Fu 2001; Fu et al. 2003, 2006).
TRMM 2A25 products can offer both the precipitation types and three dimensional rainfall structures (Iguchi et al. 2000). Moreover, as a non-sun-synchronous satellite, during its precession period it samples rainfall at different times throughout the diurnal cycle. To be noted, the reflectivity-rain-rate algorithm used to produce the TRMM 2A25 products can provide a more physically direct measurement of near surface rainfall than other remote sensing proxies like IR cloud-top temperatures and low-frequency microwave brightness temperatures (Nesbitt and Zipser 2003). In this paper, 2A25 products derived from the TRMM PR measurements are used to explore the fundamental diurnal property of two kinds of rainfall events in the southern contiguous China, and the data sets are compared with hourly rain gauge records to investigate the diurnal variations of rainfall events with different duration. It will reinforce the knowledge about regional features of diurnal variations and the corresponding mechanisms.
The rest of this paper is organized as follows: Section 2 describes the datasets and analysis method; the diurnal features of stratiform and convective precipitation are presented in Sect. 3; the diurnal features of stratiform and convective precipitation with long and short duration are discussed in Sect. 4. Section 5 describes the rainfall diurnal variations of two distinctive sub-regions. A summary and discussion are given in Sect. 6.
2 Data and methodology
The data used in this study is the TRMM standard 2A25 products measured by TRMM PR in summer (June, July and August) from 1998 to 2006. TRMM PR is an electric scanning radar operating at 13.8 GHz. It scans ±17° from nadir with 49 positions, resulting in a 215 km swath width and a horizontal resolution of 4.3 km at nadir. The resolution along the radar beam is 250 m. The 2A25 products contains rain rate profiles (R), which are calculated from the radar reflectivity (Z) profiles using a Z-R relation based on a hybrid of the Hitschfeld-Bordan method and the surface reference method (Iguchi et al. 2000). Errors in a given PR 2A25 near surface rainfall estimate may be introduced due to uncertainties in the attenuation correction, drop size distribution, and nonuniform beamfilling assumptions. However, it is unlikely that these errors are large, or would significantly affect the results portraying the phase and amplitude of the diurnal cycle (Nesbitt and Zipser 2003). Furthermore, PR pixels are classified into three types: convective, stratiform, and “other”, according to the vertical pattern of the profile (i.e. V-method) and the horizontal variability of the echo (i.e. H-method (Steiner et al. 1995)). Simply, a stratiform profile is classified if PR detects a brightband near the freezing level in the profile. If no brightband exists and any value of radar reflectivity in the beam exceeds a predetermined value of 39 dBZ, the profile is named as convective. Exception for both convective and stratiform, profile is labeled as “other”. Stratiform and convective precipitation will be the focus in this article. When total precipitation is referred, it concludes all three kinds of precipitation: stratiform, convective, and “other”.
The TRMM satellite with an orbit inclination of roughly 35° provides data between approximately ±36° latitude. However, the narrow swath of the PR data (215 km) leads to geographic undersampling on a daily basis. The orbital pattern of the satellite allows sampling between 0.5 times per day at the equator and nearly 2 times per day at 35° latitude (Nesbitt and Zipser 2003). Therefore, the swath data is inhomogeneous both spatially and temporally. As analyses were applied in 0.5° × 0.5° grid cells, correction is applied to the samples, according to the weights between the observation number of the whole region (22–32°N, 100–122°E) and that of each grid cell, as well as the weights between the observation number of each hour and the total number in the same grid cell. Because the sensitivity of PR is about 17 dBZ, which corresponds to about 0.7 mm/h in rain rate, only records with near surface rain rate no less than 1 mm/h are kept in this study.
To effectively describe the diurnal cycle, statistics on precipitation peaks and profiles are made in 6 local solar time (LST) periods defined as the midnight (from 2200 LST to 0200 LST), early morning (from 0200 LST to 0600 LST), morning (from 0600 LST to 1000 LST), noon (from 1000 LST to 1400 LST), afternoon (from 1400 LST to 1800 LST), and evening (from 1800 LST to 2200 LST).
3 Precipitation type dependent diurnal features
The diurnal phase of total precipitation is more similar to that of stratiform (convective) precipitation in Region A (B). For precipitation in Region A, the percentage contribution of stratiform precipitation is about 52.8% and convective precipitation of 46.5%. For precipitation in Region B, the proportion of stratiform precipitation is 44.1%, contrast to the convective composition of 54.5%. The stratiform (convective) precipitation occupies a large part of the total precipitation in Region A (B). While over the southern contiguous China, both the stratiform and convective precipitation have almost equally contribution to total precipitation. The convective precipitation occupies about 47.3% of total precipitation, compared to stratiform precipitation of 51.0%. Previous studies (Yu et al. 2004; Li et al. 2008) mentioned that large cloud and cloud thickness are found in the southwestern China, producing extremely strong negative short wave cloud radiative forcing. As a result, the surface air temperature is relatively low in the afternoon over the southwestern China. Therefore it is unfavorable for the occurrence of the afternoon convection. This might be a reason why the composition of convective precipitation is relatively lower in the southwestern China.
4 Duration related diurnal features
Diurnal cycle of regional averaged stratiform and convective precipitation with different duration is shown in Fig. 4b, c. As shown in Fig. 4b, both the long- and short-duration stratiform rainfalls show a late-night (0400 LST) peak over Region A and tend to peak in the late-afternoon (1600 LST) over Region B. To be noted, the diurnal amplitude of long-duration rainfall is larger than that of short-duration precipitation over Region A and a secondary peak at 0500 LST exits in rainfalls over Region B. For convective precipitation (Fig. 4c), the long-duration rainfalls peak at 0300 LST and short duration rainfall has the maximum hourly rainfall at 1500 LST over Region A. Over the southeastern China, both the long- and short-duration rainfalls peak in the late-afternoon. Similar to the stratiform long-duration precipitation, the convective long-duration precipitation also has a secondary peak in the late-night over Region B.
5 Diurnal features of two sub-regions
6 Summary and discussion
The maximum rain rate and the highest profile of stratiform precipitation occur in the late-afternoon (late-night) over the southeastern (southwestern) China. For convective precipitation, the maximum rain rate and the highest profile occur in the late-afternoon over most of the southern contiguous China.
The diurnal phase of stratiform and convective precipitation also relates to the rainfall duration. For long-duration rainfall events, most of the stratiform and convective precipitation exhibit late-night peaks except for the rainfall in the southeastern coastal regions. For short-duration rainfall events, most of two types of precipitation tend to present late-afternoon peaks, apart from the rainfall over the eastern periphery of the Tibetan Plateau.
There are two distinct sub-regions where the diurnal phases are very weakly dependent on precipitation type and duration time. Over the eastern periphery of the Tibetan Plateau, the maximum rain rate and the highest profile of either convective or stratiform precipitation occur in the late-night and the peak time of convective rain rate leads that of the stratiform rain rate by about 4 h. Over some southeastern coastal and inland mountain regions, the near surface rain rate and rain top of both convective and stratiform precipitation peak in the late-afternoon.
Without regional dependence, the convective precipitation exhibits much larger diurnal amplitude in both near surface rain rate and vertical extension compared with stratiform precipitation. The convective rain top rises most rapidly between noon and afternoon.
Using station rain gauge data, Li et al. (2008) has discussed the differences in rainfall diurnal cycle between the southwestern and southeastern China. In this study, the diurnal phase of stratiform rain rate derived from TRMM PR measurements shows similar pattern with that of the total rainfall derived from the rain gauge data over the southwestern China. This similarity indicates that the stratiform precipitation plays an important role in modulating the late-night peak in the southwestern China.
The late-afternoon peaks of the stratiform and convective short-duration rainfalls occupy a large part of the southern China. Previous studies (Yu et al. 2007b; Li et al. 2008) mentioned that the highest surface air temperature and strongest instability in the lower troposphere in the afternoon are benefit to the trigger of the convection. However, it is generally unfavorable for the formation and maintain of stratiform clouds in the afternoon (Li et al. 2003). With the development of the convection, under certain conditions the cumulonimbus capillatus quickly degrades and dissipates, then altostratus opacus or nimbostratus may form. Although the total amount of these stratiform clouds is relatively small, the stratiform clouds can produce considerable rainfall. Even if there were no stratiform cloud, stratiform precipitation can also exist in the old convection (Houze 1997). Stratiform precipitation and convection may be not absolutely exclusive. Therefore, with the high frequency of convection, precipitating stratiform clouds and stratiform precipitation may be generated from the decaying convective cloud. The processes may contribute to the peak of stratiform rainfall in the afternoon. For long-duration rainfalls, the consistent late-night maximum for the stratiform and convective precipitation over a large part of the southwestern contiguous China may be related to mesoscale convective systems (MCSs) (Yu et al. 2007b). The MCSs are strongest after midnight and a long duration may be necessary for the moisture accumulation and isolated convection cells growing into well organized MCSs before the rainfall peaks.
An interesting feature of the precipitation diurnal cycle over the southern China is the solid diurnal phase of the two sub-regions. Over the eastern periphery of the Tibetan Plateau, precipitation has a solid late-night peak. The largest rise of stratiform profile also occurs between the evening and midnight. Besides, the convective rain top has a comparable rise (about 2 km) between evening and midnight with that (about 2.5 km) between the noon and afternoon. With large cloud optical depth and small diurnal amplitude (Yu et al. 2004; Li et al. 2003, 2008), the lower troposphere is more stable in the afternoon over the southwestern China than the southeastern China and the probability of precipitation is relatively low. Because of both the nighttime middle-level cold advection originated from the plateau cold surface and the long-wave radiative cooling at the top of cloud, the instability may be triggered and reach the maximum around the late-night. Areas of sub-Region B mostly locate in either the coastal or inland mountain regions (as shown in Fig. 7). The consistent late-afternoon maximum over sub-Region B might be affected by the complex land–sea and mountain-valley breezes (Yu et al. 2008). The strongest solar heating in the afternoon may also contribute to the consistent late-afternoon peak.
This research offers a more comprehensive cognition about the characteristics of the precipitation diurnal cycle over the southern contiguous China and provides a standard for the test of parameterizations in numerical models. To further verify above processes and mechanisms, it is necessary to grasp both the categorization of rainfall types and the whole evolution processes of rainfall events. Therefore, in the following studies, the TRMM PR data and the station rain gauge data will be further synthesized to investigate these questions.
Satellite radar data was provided by NASA Goddard Space Flight Center and JAXA/EORC through the TRMM project. This research was jointly supported by the Major State Basic Research Development Program of China (973 Program) under grant No. 2004CB418304, the National Natural Science Foundation of China under grants No. 40625014, 40675027, and 40730950.
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