MozartV1, PascalFrancis, Corpus, bibRecord, 000168

Direct radiative forcing of anthropogenic organic aerosol

Identifieur interne : 000168 ( PascalFrancis/Corpus ); précédent : 000167; suivant : 000169

Direct radiative forcing of anthropogenic organic aerosol

Auteurs : YI MING ; V. Ramaswamy ; Paul A. Ginoux ; Larry H. Horowitz

Source :

Journal of geophysical research [ 0148-0227 ] ; 2005.

RBID : Pascal:06-0013167

Descripteurs français

Pascal (Inist)
- Transfert radiatif, Forçage, Aérosol, Modèle circulation générale, Climatologie, Transport, Propriété optique, Humidité relative, Croissance, Fonctionnelle, Modèle thermodynamique, Distribution dimension, Monde, Carbone organique, Ciel serein, Atmosphère, Refroidissement, Amérique du Sud, Amérique Centrale, Europe, Asie, Analyse sensibilité, Captation, Particule, Echantillon référence, Afrique Centrale.

English descriptors

KwdEn :
- Asia, Central Africa, Central America, Clear sky, Climatology, Europe, Forcing, Functional, General circulation models, Radiative transfer, Relative humidity, South America, Thermodynamic model, Uptake, aerosols, atmosphere, cooling, global, growth, optical properties, organic carbon, particles, sensitivity analysis, size distribution, standard samples, transport.

Abstract

This study simulates the direct radiative forcing of organic aerosol using the GFDL AM2 GCM. The aerosol climatology is provided by the MOZART chemical transport model (CTM). The approach to calculating aerosol optical properties explicitly considers relative humidity-dependent hygroscopic growth by employing a functional group-based thermodynamic model, and makes use of the size distribution derived from AERONET measurements. The preindustrial (PI) and present-day (PD) global burdens of organic carbon are 0.17 and 1.36 Tg OC, respectively. The annual global mean total-sky and clear-sky top-of-the atmosphere (TOA) forcings (PI to PD) are estimated as -0.34 and -0.71 W m^-2, respectively. Geographically the radiative cooling largely lies over the source regions, namely part of South America, Central Africa, Europe and South and East Asia. The annual global mean total-sky and clear-sky surface forcings are -0.63 and -0.98 W m^-2, respectively. A series of sensitivity analyses shows that the treatments of hygroscopic growth and optical properties of organic aerosol are intertwined in the determination of the global organic aerosol forcing. For example, complete deprivation of water uptake by hydrophilic organic particles reduces the standard (total-sky) and clear-sky TOA forcing estimates by 18% and 20%, respectively, while the uptake by a highly soluble organic compound (malonic acid) enhances them by 18% and 32%, respectively. Treating particles as non-absorbing enhances aerosol reflection and increases the total-sky and clear-sky TOA forcing by 47% and 18%, respectively, while neglecting the scattering brought about by the water associated with particles reduces them by 24% and 7%, respectively.

Notice en format standard (ISO 2709)

Pour connaître la documentation sur le format Inist Standard.

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Format Inist (serveur)

NO :	PASCAL 06-0013167 INIST
ET :	Direct radiative forcing of anthropogenic organic aerosol
AU :	YI MING; RAMASWAMY (V.); GINOUX (Paul A.); HOROWITZ (Larry H.)
AF :	Visiting Scientist Program, University Corporation for Atmospheric Research, Geophysical Fluid Dynamics Laboratory/Princeton, New Jersey/Etats-Unis (1 aut.); Geophysical Fluid Dynamics Laboratory/Princeton, New Jersey/Etats-Unis (2 aut., 3 aut., 4 aut.)
DT :	Publication en série; Niveau analytique
SO :	Journal of geophysical research; ISSN 0148-0227; Etats-Unis; Da. 2005; Vol. 110; No. D20; D20208.1-D20208.12; Bibl. 32 ref.
LA :	Anglais
EA :	This study simulates the direct radiative forcing of organic aerosol using the GFDL AM2 GCM. The aerosol climatology is provided by the MOZART chemical transport model (CTM). The approach to calculating aerosol optical properties explicitly considers relative humidity-dependent hygroscopic growth by employing a functional group-based thermodynamic model, and makes use of the size distribution derived from AERONET measurements. The preindustrial (PI) and present-day (PD) global burdens of organic carbon are 0.17 and 1.36 Tg OC, respectively. The annual global mean total-sky and clear-sky top-of-the atmosphere (TOA) forcings (PI to PD) are estimated as -0.34 and -0.71 W m^-2, respectively. Geographically the radiative cooling largely lies over the source regions, namely part of South America, Central Africa, Europe and South and East Asia. The annual global mean total-sky and clear-sky surface forcings are -0.63 and -0.98 W m^-2, respectively. A series of sensitivity analyses shows that the treatments of hygroscopic growth and optical properties of organic aerosol are intertwined in the determination of the global organic aerosol forcing. For example, complete deprivation of water uptake by hydrophilic organic particles reduces the standard (total-sky) and clear-sky TOA forcing estimates by 18% and 20%, respectively, while the uptake by a highly soluble organic compound (malonic acid) enhances them by 18% and 32%, respectively. Treating particles as non-absorbing enhances aerosol reflection and increases the total-sky and clear-sky TOA forcing by 47% and 18%, respectively, while neglecting the scattering brought about by the water associated with particles reduces them by 24% and 7%, respectively.
CC :	220; 001E; 001E01
FD :	Transfert radiatif; Forçage; Aérosol; Modèle circulation générale; Climatologie; Transport; Propriété optique; Humidité relative; Croissance; Fonctionnelle; Modèle thermodynamique; Distribution dimension; Monde; Carbone organique; Ciel serein; Atmosphère; Refroidissement; Amérique du Sud; Amérique Centrale; Europe; Asie; Analyse sensibilité; Captation; Particule; Echantillon référence; Afrique Centrale
FG :	Afrique
ED :	Radiative transfer; Forcing; aerosols; General circulation models; Climatology; transport; optical properties; Relative humidity; growth; Functional; Thermodynamic model; size distribution; global; organic carbon; Clear sky; atmosphere; cooling; South America; Central America; Europe; Asia; sensitivity analysis; Uptake; particles; standard samples; Central Africa
EG :	Africa
SD :	Transferencia radiativa; Forzamiento; Aerosol; Climatología; Transporte; Propiedad óptica; Humedad relativa; Funciónal; Modelo termodinámico; Mundo; Carbono orgánico; Cielo sereno; Atmósfera; Enfriamiento; America del sur; America central; Europa; Asia; Captación; Roca patrón
LO :	INIST-3144.354000135086770130
ID :	06-0013167

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Pascal:06-0013167

Le document en format XML

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<front><div type="abstract" xml:lang="en">This study simulates the direct radiative forcing of organic aerosol using the GFDL AM2 GCM. The aerosol climatology is provided by the MOZART chemical transport model (CTM). The approach to calculating aerosol optical properties explicitly considers relative humidity-dependent hygroscopic growth by employing a functional group-based thermodynamic model, and makes use of the size distribution derived from AERONET measurements. The preindustrial (PI) and present-day (PD) global burdens of organic carbon are 0.17 and 1.36 Tg OC, respectively. The annual global mean total-sky and clear-sky top-of-the atmosphere (TOA) forcings (PI to PD) are estimated as -0.34 and -0.71 W m<sup>-2</sup>
, respectively. Geographically the radiative cooling largely lies over the source regions, namely part of South America, Central Africa, Europe and South and East Asia. The annual global mean total-sky and clear-sky surface forcings are -0.63 and -0.98 W m<sup>-2</sup>
, respectively. A series of sensitivity analyses shows that the treatments of hygroscopic growth and optical properties of organic aerosol are intertwined in the determination of the global organic aerosol forcing. For example, complete deprivation of water uptake by hydrophilic organic particles reduces the standard (total-sky) and clear-sky TOA forcing estimates by 18% and 20%, respectively, while the uptake by a highly soluble organic compound (malonic acid) enhances them by 18% and 32%, respectively. Treating particles as non-absorbing enhances aerosol reflection and increases the total-sky and clear-sky TOA forcing by 47% and 18%, respectively, while neglecting the scattering brought about by the water associated with particles reduces them by 24% and 7%, respectively.</div>
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<fA44><s0>0000</s0>
<s1>© 2006 INIST-CNRS. All rights reserved.</s1>
</fA44>
<fA45><s0>32 ref.</s0>
</fA45>
<fA47 i1="01" i2="1"><s0>06-0013167</s0>
</fA47>
<fA60><s1>P</s1>
</fA60>
<fA61><s0>A</s0>
</fA61>
<fA64 i1="01" i2="1"><s0>Journal of geophysical research</s0>
</fA64>
<fA66 i1="01"><s0>USA</s0>
</fA66>
<fC01 i1="01" l="ENG"><s0>This study simulates the direct radiative forcing of organic aerosol using the GFDL AM2 GCM. The aerosol climatology is provided by the MOZART chemical transport model (CTM). The approach to calculating aerosol optical properties explicitly considers relative humidity-dependent hygroscopic growth by employing a functional group-based thermodynamic model, and makes use of the size distribution derived from AERONET measurements. The preindustrial (PI) and present-day (PD) global burdens of organic carbon are 0.17 and 1.36 Tg OC, respectively. The annual global mean total-sky and clear-sky top-of-the atmosphere (TOA) forcings (PI to PD) are estimated as -0.34 and -0.71 W m<sup>-2</sup>
, respectively. Geographically the radiative cooling largely lies over the source regions, namely part of South America, Central Africa, Europe and South and East Asia. The annual global mean total-sky and clear-sky surface forcings are -0.63 and -0.98 W m<sup>-2</sup>
, respectively. A series of sensitivity analyses shows that the treatments of hygroscopic growth and optical properties of organic aerosol are intertwined in the determination of the global organic aerosol forcing. For example, complete deprivation of water uptake by hydrophilic organic particles reduces the standard (total-sky) and clear-sky TOA forcing estimates by 18% and 20%, respectively, while the uptake by a highly soluble organic compound (malonic acid) enhances them by 18% and 32%, respectively. Treating particles as non-absorbing enhances aerosol reflection and increases the total-sky and clear-sky TOA forcing by 47% and 18%, respectively, while neglecting the scattering brought about by the water associated with particles reduces them by 24% and 7%, respectively.</s0>
</fC01>
<fC02 i1="01" i2="2"><s0>220</s0>
</fC02>
<fC02 i1="02" i2="3"><s0>001E</s0>
</fC02>
<fC02 i1="03" i2="2"><s0>001E01</s0>
</fC02>
<fC03 i1="01" i2="X" l="FRE"><s0>Transfert radiatif</s0>
<s5>01</s5>
</fC03>
<fC03 i1="01" i2="X" l="ENG"><s0>Radiative transfer</s0>
<s5>01</s5>
</fC03>
<fC03 i1="01" i2="X" l="SPA"><s0>Transferencia radiativa</s0>
<s5>01</s5>
</fC03>
<fC03 i1="02" i2="X" l="FRE"><s0>Forçage</s0>
<s5>02</s5>
</fC03>
<fC03 i1="02" i2="X" l="ENG"><s0>Forcing</s0>
<s5>02</s5>
</fC03>
<fC03 i1="02" i2="X" l="SPA"><s0>Forzamiento</s0>
<s5>02</s5>
</fC03>
<fC03 i1="03" i2="2" l="FRE"><s0>Aérosol</s0>
<s5>03</s5>
</fC03>
<fC03 i1="03" i2="2" l="ENG"><s0>aerosols</s0>
<s5>03</s5>
</fC03>
<fC03 i1="03" i2="2" l="SPA"><s0>Aerosol</s0>
<s5>03</s5>
</fC03>
<fC03 i1="04" i2="3" l="FRE"><s0>Modèle circulation générale</s0>
<s5>04</s5>
</fC03>
<fC03 i1="04" i2="3" l="ENG"><s0>General circulation models</s0>
<s5>04</s5>
</fC03>
<fC03 i1="05" i2="X" l="FRE"><s0>Climatologie</s0>
<s5>05</s5>
</fC03>
<fC03 i1="05" i2="X" l="ENG"><s0>Climatology</s0>
<s5>05</s5>
</fC03>
<fC03 i1="05" i2="X" l="SPA"><s0>Climatología</s0>
<s5>05</s5>
</fC03>
<fC03 i1="06" i2="2" l="FRE"><s0>Transport</s0>
<s5>06</s5>
</fC03>
<fC03 i1="06" i2="2" l="ENG"><s0>transport</s0>
<s5>06</s5>
</fC03>
<fC03 i1="06" i2="2" l="SPA"><s0>Transporte</s0>
<s5>06</s5>
</fC03>
<fC03 i1="07" i2="2" l="FRE"><s0>Propriété optique</s0>
<s5>07</s5>
</fC03>
<fC03 i1="07" i2="2" l="ENG"><s0>optical properties</s0>
<s5>07</s5>
</fC03>
<fC03 i1="07" i2="2" l="SPA"><s0>Propiedad óptica</s0>
<s5>07</s5>
</fC03>
<fC03 i1="08" i2="X" l="FRE"><s0>Humidité relative</s0>
<s5>08</s5>
</fC03>
<fC03 i1="08" i2="X" l="ENG"><s0>Relative humidity</s0>
<s5>08</s5>
</fC03>
<fC03 i1="08" i2="X" l="SPA"><s0>Humedad relativa</s0>
<s5>08</s5>
</fC03>
<fC03 i1="09" i2="2" l="FRE"><s0>Croissance</s0>
<s5>09</s5>
</fC03>
<fC03 i1="09" i2="2" l="ENG"><s0>growth</s0>
<s5>09</s5>
</fC03>
<fC03 i1="10" i2="X" l="FRE"><s0>Fonctionnelle</s0>
<s5>10</s5>
</fC03>
<fC03 i1="10" i2="X" l="ENG"><s0>Functional</s0>
<s5>10</s5>
</fC03>
<fC03 i1="10" i2="X" l="SPA"><s0>Funciónal</s0>
<s5>10</s5>
</fC03>
<fC03 i1="11" i2="X" l="FRE"><s0>Modèle thermodynamique</s0>
<s5>11</s5>
</fC03>
<fC03 i1="11" i2="X" l="ENG"><s0>Thermodynamic model</s0>
<s5>11</s5>
</fC03>
<fC03 i1="11" i2="X" l="SPA"><s0>Modelo termodinámico</s0>
<s5>11</s5>
</fC03>
<fC03 i1="12" i2="2" l="FRE"><s0>Distribution dimension</s0>
<s5>12</s5>
</fC03>
<fC03 i1="12" i2="2" l="ENG"><s0>size distribution</s0>
<s5>12</s5>
</fC03>
<fC03 i1="13" i2="2" l="FRE"><s0>Monde</s0>
<s5>13</s5>
</fC03>
<fC03 i1="13" i2="2" l="ENG"><s0>global</s0>
<s5>13</s5>
</fC03>
<fC03 i1="13" i2="2" l="SPA"><s0>Mundo</s0>
<s5>13</s5>
</fC03>
<fC03 i1="14" i2="2" l="FRE"><s0>Carbone organique</s0>
<s5>14</s5>
</fC03>
<fC03 i1="14" i2="2" l="ENG"><s0>organic carbon</s0>
<s5>14</s5>
</fC03>
<fC03 i1="14" i2="2" l="SPA"><s0>Carbono orgánico</s0>
<s5>14</s5>
</fC03>
<fC03 i1="15" i2="X" l="FRE"><s0>Ciel serein</s0>
<s5>15</s5>
</fC03>
<fC03 i1="15" i2="X" l="ENG"><s0>Clear sky</s0>
<s5>15</s5>
</fC03>
<fC03 i1="15" i2="X" l="SPA"><s0>Cielo sereno</s0>
<s5>15</s5>
</fC03>
<fC03 i1="16" i2="2" l="FRE"><s0>Atmosphère</s0>
<s5>16</s5>
</fC03>
<fC03 i1="16" i2="2" l="ENG"><s0>atmosphere</s0>
<s5>16</s5>
</fC03>
<fC03 i1="16" i2="2" l="SPA"><s0>Atmósfera</s0>
<s5>16</s5>
</fC03>
<fC03 i1="17" i2="2" l="FRE"><s0>Refroidissement</s0>
<s5>17</s5>
</fC03>
<fC03 i1="17" i2="2" l="ENG"><s0>cooling</s0>
<s5>17</s5>
</fC03>
<fC03 i1="17" i2="2" l="SPA"><s0>Enfriamiento</s0>
<s5>17</s5>
</fC03>
<fC03 i1="18" i2="2" l="FRE"><s0>Amérique du Sud</s0>
<s5>18</s5>
</fC03>
<fC03 i1="18" i2="2" l="ENG"><s0>South America</s0>
<s5>18</s5>
</fC03>
<fC03 i1="18" i2="2" l="SPA"><s0>America del sur</s0>
<s5>18</s5>
</fC03>
<fC03 i1="19" i2="2" l="FRE"><s0>Amérique Centrale</s0>
<s5>19</s5>
</fC03>
<fC03 i1="19" i2="2" l="ENG"><s0>Central America</s0>
<s5>19</s5>
</fC03>
<fC03 i1="19" i2="2" l="SPA"><s0>America central</s0>
<s5>19</s5>
</fC03>
<fC03 i1="20" i2="2" l="FRE"><s0>Europe</s0>
<s5>20</s5>
</fC03>
<fC03 i1="20" i2="2" l="ENG"><s0>Europe</s0>
<s5>20</s5>
</fC03>
<fC03 i1="20" i2="2" l="SPA"><s0>Europa</s0>
<s5>20</s5>
</fC03>
<fC03 i1="21" i2="2" l="FRE"><s0>Asie</s0>
<s5>21</s5>
</fC03>
<fC03 i1="21" i2="2" l="ENG"><s0>Asia</s0>
<s5>21</s5>
</fC03>
<fC03 i1="21" i2="2" l="SPA"><s0>Asia</s0>
<s5>21</s5>
</fC03>
<fC03 i1="22" i2="2" l="FRE"><s0>Analyse sensibilité</s0>
<s5>22</s5>
</fC03>
<fC03 i1="22" i2="2" l="ENG"><s0>sensitivity analysis</s0>
<s5>22</s5>
</fC03>
<fC03 i1="23" i2="X" l="FRE"><s0>Captation</s0>
<s5>23</s5>
</fC03>
<fC03 i1="23" i2="X" l="ENG"><s0>Uptake</s0>
<s5>23</s5>
</fC03>
<fC03 i1="23" i2="X" l="SPA"><s0>Captación</s0>
<s5>23</s5>
</fC03>
<fC03 i1="24" i2="2" l="FRE"><s0>Particule</s0>
<s5>24</s5>
</fC03>
<fC03 i1="24" i2="2" l="ENG"><s0>particles</s0>
<s5>24</s5>
</fC03>
<fC03 i1="25" i2="2" l="FRE"><s0>Echantillon référence</s0>
<s5>25</s5>
</fC03>
<fC03 i1="25" i2="2" l="ENG"><s0>standard samples</s0>
<s5>25</s5>
</fC03>
<fC03 i1="25" i2="2" l="SPA"><s0>Roca patrón</s0>
<s5>25</s5>
</fC03>
<fC03 i1="26" i2="2" l="FRE"><s0>Afrique Centrale</s0>
<s2>NG</s2>
<s5>61</s5>
</fC03>
<fC03 i1="26" i2="2" l="ENG"><s0>Central Africa</s0>
<s2>NG</s2>
<s5>61</s5>
</fC03>
<fC07 i1="01" i2="2" l="FRE"><s0>Afrique</s0>
</fC07>
<fC07 i1="01" i2="2" l="ENG"><s0>Africa</s0>
</fC07>
<fC07 i1="01" i2="2" l="SPA"><s0>Africa</s0>
</fC07>
<fN21><s1>002</s1>
</fN21>
<fN44 i1="01"><s1>OTO</s1>
</fN44>
<fN82><s1>OTO</s1>
</fN82>
</pA>
</standard>
<server><NO>PASCAL 06-0013167 INIST</NO>
<ET>Direct radiative forcing of anthropogenic organic aerosol</ET>
<AU>YI MING; RAMASWAMY (V.); GINOUX (Paul A.); HOROWITZ (Larry H.)</AU>
<AF>Visiting Scientist Program, University Corporation for Atmospheric Research, Geophysical Fluid Dynamics Laboratory/Princeton, New Jersey/Etats-Unis (1 aut.); Geophysical Fluid Dynamics Laboratory/Princeton, New Jersey/Etats-Unis (2 aut., 3 aut., 4 aut.)</AF>
<DT>Publication en série; Niveau analytique</DT>
<SO>Journal of geophysical research; ISSN 0148-0227; Etats-Unis; Da. 2005; Vol. 110; No. D20; D20208.1-D20208.12; Bibl. 32 ref.</SO>
<LA>Anglais</LA>
<EA>This study simulates the direct radiative forcing of organic aerosol using the GFDL AM2 GCM. The aerosol climatology is provided by the MOZART chemical transport model (CTM). The approach to calculating aerosol optical properties explicitly considers relative humidity-dependent hygroscopic growth by employing a functional group-based thermodynamic model, and makes use of the size distribution derived from AERONET measurements. The preindustrial (PI) and present-day (PD) global burdens of organic carbon are 0.17 and 1.36 Tg OC, respectively. The annual global mean total-sky and clear-sky top-of-the atmosphere (TOA) forcings (PI to PD) are estimated as -0.34 and -0.71 W m<sup>-2</sup>
, respectively. Geographically the radiative cooling largely lies over the source regions, namely part of South America, Central Africa, Europe and South and East Asia. The annual global mean total-sky and clear-sky surface forcings are -0.63 and -0.98 W m<sup>-2</sup>
, respectively. A series of sensitivity analyses shows that the treatments of hygroscopic growth and optical properties of organic aerosol are intertwined in the determination of the global organic aerosol forcing. For example, complete deprivation of water uptake by hydrophilic organic particles reduces the standard (total-sky) and clear-sky TOA forcing estimates by 18% and 20%, respectively, while the uptake by a highly soluble organic compound (malonic acid) enhances them by 18% and 32%, respectively. Treating particles as non-absorbing enhances aerosol reflection and increases the total-sky and clear-sky TOA forcing by 47% and 18%, respectively, while neglecting the scattering brought about by the water associated with particles reduces them by 24% and 7%, respectively.</EA>
<CC>220; 001E; 001E01</CC>
<FD>Transfert radiatif; Forçage; Aérosol; Modèle circulation générale; Climatologie; Transport; Propriété optique; Humidité relative; Croissance; Fonctionnelle; Modèle thermodynamique; Distribution dimension; Monde; Carbone organique; Ciel serein; Atmosphère; Refroidissement; Amérique du Sud; Amérique Centrale; Europe; Asie; Analyse sensibilité; Captation; Particule; Echantillon référence; Afrique Centrale</FD>
<FG>Afrique</FG>
<ED>Radiative transfer; Forcing; aerosols; General circulation models; Climatology; transport; optical properties; Relative humidity; growth; Functional; Thermodynamic model; size distribution; global; organic carbon; Clear sky; atmosphere; cooling; South America; Central America; Europe; Asia; sensitivity analysis; Uptake; particles; standard samples; Central Africa</ED>
<EG>Africa</EG>
<SD>Transferencia radiativa; Forzamiento; Aerosol; Climatología; Transporte; Propiedad óptica; Humedad relativa; Funciónal; Modelo termodinámico; Mundo; Carbono orgánico; Cielo sereno; Atmósfera; Enfriamiento; America del sur; America central; Europa; Asia; Captación; Roca patrón</SD>
<LO>INIST-3144.354000135086770130</LO>
<ID>06-0013167</ID>
</server>
</inist>
</record>

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Direct radiative forcing of anthropogenic organic aerosol

Direct radiative forcing of anthropogenic organic aerosol

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