Estimation of Asian dust aerosol effect on cloud radiation forcing using Fu-Liou radiative model and CERES measurements

Jing, Su; Huang, Jianping; Fu, Qiang; Minnis, Patrick; Ge, Jinming; Bi, Jun

doi:10.5194/acpd-8-2061-2008

Cited by 43 publications

(53 citation statements)

References 19 publications

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“…These values ranged from 2.6 W m -2 in December to 7.1 W m -2 in August. These absorbing properties of aerosols are also particularly important for energy balance and cloud-aerosol interactions, as shown in the work of Su et al (2008).…”

Section: Aerosol Radiative Forcingmentioning

confidence: 99%

Thirteen Years of Aerosol Radiative Forcing in Southwestern Iberian Peninsula

Muñoz

Costa

Silva

et al. 2017

Aerosol Air Qual. Res.

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Notable uncertainties in the aerosol impact on the Earth's radiative budget still remain, mainly at local scales. This study aims to accurately quantify the shortwave aerosol radiative forcing (ARF) and its efficiency (ARFE) at Évora (Portugal, Southwestern Europe). This is an interesting region affected by different aerosol types and sources. Towards this goal, ARF and ARFE are calculated for Évora during thirteen years (2003)(2004)(2005)(2006)(2007)(2008)(2009)(2010)(2011)(2012)(2013)(2014)(2015), which is the longest period ever analyzed for this region. For this calculation, the most updated AERONET data have been used to simulate irradiance with the libRadtran code. Thus, 1676 daily values were analyzed, obtaining a mean ARF of -7.4 W m -2 at the Earth's surface (SURF) and -1.1 W m -2 at the top of the atmosphere (TOA), indicating a cooling of the Earth-atmosphere system. The difference in ARF between TOA and SURF indicates a mean net gain of 6.3 W m -2 for the atmosphere. While no ARF seasonal pattern is observed at the TOA, a clear seasonal cycle is detected at the SURF with the most negative values occurring in summer. On the other hand, ARFE shows mean values of -62.7 W m -2 τ -1 at the SURF and -14.3 W m -2 τ -1 at the TOA. Results show that ARFE highly depends on the aerosol single scattering albedo, showing opposite behavior at the SURF and at the TOA. The large temporal variability detected in the aerosol properties in the region of study confirms the general need for long time series of measurements to achieve an accurate estimation of the ARF and ARFE.

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Section: Aerosol Radiative Forcingmentioning

confidence: 99%

Thirteen Years of Aerosol Radiative Forcing in Southwestern Iberian Peninsula

Muñoz

Costa

Silva

et al. 2017

Aerosol Air Qual. Res.

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“…Tibetan dust aerosol layers appear most frequently at approximately 4-7 km above the mean sea level, where the plumes likely originate from the nearby Taklimakan Desert and accumulate over the northern slopes of the TP during summer (Huang et al, 2007b). As the dust storm travels toward the TP, the dust aerosols may mix with anthropogenic aerosols and induce new environmental and climatic problems (Jing Su et al, 2008).…”

mentioning

confidence: 99%

Modeling study on the transport of summer dust and anthropogenic aerosols over the Tibetan Plateau

et al. 2015

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Abstract. The Tibetan Plateau (TP) is located at the juncture of several important natural and anthropogenic aerosol sources. Satellites have observed substantial dust and anthropogenic aerosols in the atmosphere during summer over the TP. These aerosols have distinct effects on the earth's energy balance, microphysical cloud properties, and precipitation rates. To investigate the transport of summer dust and anthropogenic aerosols over the TP, we combined the Spectral Radiation-Transport Model for Aerosol Species (SPRINT-ARS) with a non-hydrostatic regional model (NHM). The model simulation shows heavily loaded dust aerosols over the northern slope and anthropogenic aerosols over the southern slope and the east of the TP. The dust aerosols are primarily mobilized around the Taklimakan Desert, where a portion of the aerosols are transported eastward due to the northwesterly current; simultaneously, a portion of the particles are transported southward when a second northwesterly current becomes northeasterly because of the topographic blocking of the northern slope of the TP. Because of the strong upward current, dust plumes can extend upward to approximately 7-8 km a.s.l. over the northern slope of the TP. When a dust event occurs, anthropogenic aerosols that entrained into the southwesterly current via the Indian summer monsoon are transported from India to the southern slope of the TP. Simultaneously, a large amount of anthropogenic aerosol is also transported from eastern China to the east of the TP by easterly winds. An investigation on the transport of dust and anthropogenic aerosols over the plateau may provide the basis for determining aerosol impacts on summer monsoons and climate systems.

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“…We found (Figure 7) a general heating of the entire atmospheric column with a much greater effect near the surface. From Figure 6, one can note that aerosols effect on the heating rate profile [30] shows strong cooling during the day for the lower atmosphere, with slight heating at the upper atmosphere. This SW cooling in aerosol layer is caused by the reflection of solar radiation from the aerosols, which reduces the amount of solar radiation available for absorption.…”

Section: Effect Of Clouds and Aerosols On The Atmospheric Heatingmentioning

confidence: 99%

Shortwave Cloud and Aerosol Radiative Forcings and Their Effects on the Vertical Local Heating/Cooling Rates

Nguimdo¹,

Njomo²

2013

ACS

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An analysis of atmospheric SW-radiative forcing and local heating/cooling rate is made using a one year temporal and vertical profiles of aerosol and cloud over Yaoundé (11.51˚E, 3.83˚N). It appears that the direct influence of aerosols on the surface compared to the TOA can be 3 times larger. Annual mean value obtained at 559 mb altitude is +27.74 W/m 2 with range from 0 to +43 W/m 2 . At 904 mb, we obtained an annual mean of −46.22 W/m 2 with range from −65 to −9 W/m 2 . Frequency distribution indicates that more than 95% of ARF are between +10 and +70 W/m 2 at 559 mb (upper limit of UL), and more than 85% of ARF are between −70 and −10 W/m 2 at 904 mb (upper limit of PBL). This sign change is explained by the fact that the backscattering peaks at the upper limit of the aerosol PBL layer. The maximum CRF is noted at TOA where it reaches −600 W/m 2 based on the time interval and the structure of clouds. The highest values occur between 11.50 and 13.50 LST. Clouds lead to a general heating of the entire atmospheric column with a much greater effect near the surface. Aerosols effect on the heating rate profile show strong cooling during the day for the lower atmosphere, with slight heating at the upper atmosphere. This cooling contribution generally increases from the surface and peacks at the upper boundary of aerosol layer where reflectivity is the most important. Depending on the moment of the day, average heating effect of clouds peacks at surface or within the middle troposphere due to the absorption by clouds particles. Vertical profiles deeply evolve exhibiting differences that exceed −3 K/day according to altitude from one hour to another during a given mean solar day.

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Estimation of Asian dust aerosol effect on cloud radiation forcing using Fu-Liou radiative model and CERES measurements

Cited by 43 publications

References 19 publications

Thirteen Years of Aerosol Radiative Forcing in Southwestern Iberian Peninsula

Thirteen Years of Aerosol Radiative Forcing in Southwestern Iberian Peninsula

Modeling study on the transport of summer dust and anthropogenic aerosols over the Tibetan Plateau

Shortwave Cloud and Aerosol Radiative Forcings and Their Effects on the Vertical Local Heating/Cooling Rates

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