Core and margin in warm convective clouds – Part 2: Aerosol effects on core properties
<p>The effects of aerosol on warm convective cloud cores are evaluated using single cloud and cloud field simulations. Three core definitions are examined: positive vertical velocity (<span class="inline-formula"><i>W</i><sub>core</sub></span>), su...
| Main Authors: | , , , , |
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| Format: | Article |
| Language: | English |
| Published: |
Copernicus Publications
2019-08-01
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| Series: | Atmospheric Chemistry and Physics |
| Online Access: | https://www.atmos-chem-phys.net/19/10739/2019/acp-19-10739-2019.pdf |
| _version_ | 1819277378893905920 |
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| author | R. H. Heiblum L. Pinto O. Altaratz G. Dagan G. Dagan I. Koren |
| author_facet | R. H. Heiblum L. Pinto O. Altaratz G. Dagan G. Dagan I. Koren |
| author_sort | R. H. Heiblum |
| collection | DOAJ |
| description | <p>The effects of aerosol on warm convective cloud cores are evaluated using
single cloud and cloud field simulations. Three core definitions are
examined: positive vertical velocity (<span class="inline-formula"><i>W</i><sub>core</sub></span>), supersaturation
(RH<span class="inline-formula"><sub>core</sub>)</span>, and positive buoyancy (<span class="inline-formula"><i>B</i><sub>core</sub></span>). As presented in Part 1 (Heiblum et al., 2019),
the property <span class="inline-formula"><math xmlns="http://www.w3.org/1998/Math/MathML" id="M4" display="inline" overflow="scroll" dspmath="mathml"><mrow><msub><mi>B</mi><mi mathvariant="normal">core</mi></msub><mo>⊆</mo><msub><mi mathvariant="normal">RH</mi><mi mathvariant="normal">core</mi></msub><mo>⊆</mo><msub><mi>W</mi><mi mathvariant="normal">core</mi></msub></mrow></math><span><svg:svg xmlns:svg="http://www.w3.org/2000/svg" width="107pt" height="13pt" class="svg-formula" dspmath="mathimg" md5hash="4b48f5ce235ae08f6aa376e6e7adc73c"><svg:image xmlns:xlink="http://www.w3.org/1999/xlink" xlink:href="acp-19-10739-2019-ie00001.svg" width="107pt" height="13pt" src="acp-19-10739-2019-ie00001.png"/></svg:svg></span></span> is
seen during growth of warm convective clouds. We show that this property is
kept irrespective of aerosol concentration. During dissipation core
fractions generally decrease with less overlap between cores. However, for
clouds that develop in low aerosol concentrations capable of producing
precipitation, <span class="inline-formula"><i>B</i><sub>core</sub></span> and subsequently <span class="inline-formula"><i>W</i><sub>core</sub></span> volume fractions may
increase during dissipation (i.e., loss of cloud mass). The RH<span class="inline-formula"><sub>core</sub></span>
volume fraction decreases during cloud lifetime and shows minor sensitivity
to aerosol concentration.</p>
<p>It is shown that a <span class="inline-formula"><i>B</i><sub>core</sub></span> forms due to two processes: (i) convective
updrafts – condensation within supersaturated updrafts and release of
latent heat – and (ii) dissipative downdrafts – subsaturated cloudy downdrafts
that warm during descent and “undershoot” the level of neutral buoyancy. The
former process occurs during cloud growth for all aerosol concentrations.
The latter process only occurs for low aerosol concentrations during
dissipation and precipitation stages where large mean drop sizes permit slow
evaporation rates and subsaturation during descent.</p>
<p>The aerosol effect on the diffusion efficiencies plays a crucial role in the
development of the cloud and its partition to core and margin. Using the
RH<span class="inline-formula"><sub>core</sub></span> definition, it is shown that the total cloud mass is mostly
dictated by core processes, while the total cloud volume is mostly dictated
by margin processes. Increase in aerosol concentration increases the core
(mass and volume) due to enhanced condensation but also decreases the margin
due to evaporation. In clean clouds larger droplets evaporate much slower,
enabling preservation of cloud size, and even increase by detrainment and
dilution (volume increases while losing mass). This explains how despite
having smaller cores and less mass, cleaner clouds may live longer and grow
to larger sizes.</p> |
| first_indexed | 2024-12-23T23:55:10Z |
| format | Article |
| id | doaj.art-be5b510104ff43838dc21f3125baa62f |
| institution | Directory Open Access Journal |
| issn | 1680-7316 1680-7324 |
| language | English |
| last_indexed | 2024-12-23T23:55:10Z |
| publishDate | 2019-08-01 |
| publisher | Copernicus Publications |
| record_format | Article |
| series | Atmospheric Chemistry and Physics |
| spelling | doaj.art-be5b510104ff43838dc21f3125baa62f2022-12-21T17:25:16ZengCopernicus PublicationsAtmospheric Chemistry and Physics1680-73161680-73242019-08-0119107391075510.5194/acp-19-10739-2019Core and margin in warm convective clouds – Part 2: Aerosol effects on core propertiesR. H. Heiblum0L. Pinto1O. Altaratz2G. Dagan3G. Dagan4I. Koren5Department of Earth and Planetary Sciences, Weizmann Institute of Science, Rehovot, IsraelDepartment of Earth and Planetary Sciences, Weizmann Institute of Science, Rehovot, IsraelDepartment of Earth and Planetary Sciences, Weizmann Institute of Science, Rehovot, IsraelDepartment of Earth and Planetary Sciences, Weizmann Institute of Science, Rehovot, Israelnow at: Atmospheric, Oceanic and Planetary Physics, Department of Physics, University of Oxford, Oxford, UKDepartment of Earth and Planetary Sciences, Weizmann Institute of Science, Rehovot, Israel<p>The effects of aerosol on warm convective cloud cores are evaluated using single cloud and cloud field simulations. Three core definitions are examined: positive vertical velocity (<span class="inline-formula"><i>W</i><sub>core</sub></span>), supersaturation (RH<span class="inline-formula"><sub>core</sub>)</span>, and positive buoyancy (<span class="inline-formula"><i>B</i><sub>core</sub></span>). As presented in Part 1 (Heiblum et al., 2019), the property <span class="inline-formula"><math xmlns="http://www.w3.org/1998/Math/MathML" id="M4" display="inline" overflow="scroll" dspmath="mathml"><mrow><msub><mi>B</mi><mi mathvariant="normal">core</mi></msub><mo>⊆</mo><msub><mi mathvariant="normal">RH</mi><mi mathvariant="normal">core</mi></msub><mo>⊆</mo><msub><mi>W</mi><mi mathvariant="normal">core</mi></msub></mrow></math><span><svg:svg xmlns:svg="http://www.w3.org/2000/svg" width="107pt" height="13pt" class="svg-formula" dspmath="mathimg" md5hash="4b48f5ce235ae08f6aa376e6e7adc73c"><svg:image xmlns:xlink="http://www.w3.org/1999/xlink" xlink:href="acp-19-10739-2019-ie00001.svg" width="107pt" height="13pt" src="acp-19-10739-2019-ie00001.png"/></svg:svg></span></span> is seen during growth of warm convective clouds. We show that this property is kept irrespective of aerosol concentration. During dissipation core fractions generally decrease with less overlap between cores. However, for clouds that develop in low aerosol concentrations capable of producing precipitation, <span class="inline-formula"><i>B</i><sub>core</sub></span> and subsequently <span class="inline-formula"><i>W</i><sub>core</sub></span> volume fractions may increase during dissipation (i.e., loss of cloud mass). The RH<span class="inline-formula"><sub>core</sub></span> volume fraction decreases during cloud lifetime and shows minor sensitivity to aerosol concentration.</p> <p>It is shown that a <span class="inline-formula"><i>B</i><sub>core</sub></span> forms due to two processes: (i) convective updrafts – condensation within supersaturated updrafts and release of latent heat – and (ii) dissipative downdrafts – subsaturated cloudy downdrafts that warm during descent and “undershoot” the level of neutral buoyancy. The former process occurs during cloud growth for all aerosol concentrations. The latter process only occurs for low aerosol concentrations during dissipation and precipitation stages where large mean drop sizes permit slow evaporation rates and subsaturation during descent.</p> <p>The aerosol effect on the diffusion efficiencies plays a crucial role in the development of the cloud and its partition to core and margin. Using the RH<span class="inline-formula"><sub>core</sub></span> definition, it is shown that the total cloud mass is mostly dictated by core processes, while the total cloud volume is mostly dictated by margin processes. Increase in aerosol concentration increases the core (mass and volume) due to enhanced condensation but also decreases the margin due to evaporation. In clean clouds larger droplets evaporate much slower, enabling preservation of cloud size, and even increase by detrainment and dilution (volume increases while losing mass). This explains how despite having smaller cores and less mass, cleaner clouds may live longer and grow to larger sizes.</p>https://www.atmos-chem-phys.net/19/10739/2019/acp-19-10739-2019.pdf |
| spellingShingle | R. H. Heiblum L. Pinto O. Altaratz G. Dagan G. Dagan I. Koren Core and margin in warm convective clouds – Part 2: Aerosol effects on core properties Atmospheric Chemistry and Physics |
| title | Core and margin in warm convective clouds – Part 2: Aerosol effects on core properties |
| title_full | Core and margin in warm convective clouds – Part 2: Aerosol effects on core properties |
| title_fullStr | Core and margin in warm convective clouds – Part 2: Aerosol effects on core properties |
| title_full_unstemmed | Core and margin in warm convective clouds – Part 2: Aerosol effects on core properties |
| title_short | Core and margin in warm convective clouds – Part 2: Aerosol effects on core properties |
| title_sort | core and margin in warm convective clouds part 2 aerosol effects on core properties |
| url | https://www.atmos-chem-phys.net/19/10739/2019/acp-19-10739-2019.pdf |
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