Modeling radiative effects of haze on summer-time convective precipitation over North China: a case study

doi:10.1007/s11783-016-0840-3

Front. Environ. Sci. Eng.

2016, Vol. 10

Issue (4) : 1 https://doi.org/10.1007/s11783-016-0840-3

RESEARCH ARTICLE

Modeling radiative effects of haze on summer-time convective precipitation over North China: a case study

Xuying WANG^1,^2,^*(

),Bin ZHANG^1,³

1. School of Environment, Tsinghua University, Beijing 100084, China
2. Chinese Academy for Environmental Planning, Beijing 100012, China
3. Ministry of Education Key Laboratory for Earth System Modeling, Center for Earth System Science, Institute for Global Change Studies, Tsinghua University, Beijing 100084, China

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Abstract

We modeled the impact of haze radiative effects on precipitation in North China.

Shortwave heating induced by haze radiative effects would reduce heavy rainfalls.

Convection was the key factor that whether precipitation was enhanced or suppressed.

Precipitation was often suppressed where CAPE, RH and updraft velocities were high.

The impact of haze radiative effect on summertime 24-h convective precipitation over North China was investigated using WRF model (version 3.3) through model sensitivity studies between scenarios with and without aerosol radiative effects. The haze radiative effect was represented by incorporating an idealized aerosol optical profile, with AOD values around 1, derived from the aircraft measurement into the WRF shortwave scheme. We found that the shortwave heating induced by aerosol radiative effects would significantly reduce heavy rainfalls, although its effect on the post-frontal localized thunderstorm precipitation was more diverse. To capture the key factors that determine whether precipitation is enhanced or suppressed, model grids with 24-h precipitation difference between the two scenarios exceeding certain threshold (>30 mm or<-30 mm) were separated into two sets. Analyses of key meteorological variables between the enhanced and suppressed regimes suggested that atmospheric convection was the most important factor that determined whether precipitation was enhanced or suppressed during summertime over North China. The convection was stronger over places with precipitation enhancement over 30 mm. Haze weakened the convection over places with precipitation suppression exceeding 30 mm and caused less water vapor to rise to a higher level and thus further suppressed precipitation. The suppression of precipitation was often accompanied with relatively high convective available potential energy (CAPE), relative humidity (RH) and updraft velocities.

Keywords Haze Aerosol radiative effects Convective precipitation

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Corresponding Author(s): Xuying WANG

Issue Date: 20 April 2016

Cite this article:

Xuying WANG,Bin ZHANG. Modeling radiative effects of haze on summer-time convective precipitation over North China: a case study[J]. Front. Environ. Sci. Eng., 2016, 10(4): 1.

URL:

https://academic.hep.com.cn/fese/EN/10.1007/s11783-016-0840-3
https://academic.hep.com.cn/fese/EN/Y2016/V10/I4/1

Fig.1 WRF simulated (a), APHRODITE gridded (b) and TRMM satellite (c) 24-h precipitation of 1 August 2006 over domain 1; the time starts from 0000 UTC August 1 for WRF and APHRODITE and from 2230 UTC July 31 for TRMM

Fig.2 Difference of model simulated precipitation of 2 August 2006 over domain 2 for S_C and S_A (S_A – S_C) (red means precipitation enhancement and blue means precipitation suppression) (a); Domain 2-averaged precipitation intensity for S_C and S_A (b); Correlation of grid precipitation for S_C and that of difference of the two scenarios (S_A – S_C) (c)

Tab.1 Summary of properties for Cluster CE and CS

Fig.3 Time series of latent heat (a) and sensible heat (b) flux for Cluster CE and time series of latent heat (c) and sensible heat (d) flux for Cluster CS

Fig.4 Vertical variation of the atmospheric shortwave heating averaged over 15–24 h for Cluster CE (a) and CS (c), and the difference of the atmospheric temperature (S_A – S_C) for Cluster CE (b) and CS (d)

Fig.5 Vertical and temporal variation of the updraft velocity for Cluster CE in S_C (a) and S_A (b) and for Cluster CS in S_C (c) and S_A (d)

Fig.6 Time series of CAPE and RH averaged over the lower atmosphere (<2 km) under two scenarios for Cluster CE (a) (b) and Cluster CS (c) (d)

Fig.7 Time series of CAPE (a) and RH (b) averaged over the lower atmosphere (<2 km) for Cluster CE and CS in the controlled scenario

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