Band-by-band Cloud Radiative Forcing: new dimension to evaluate the GCM simulation and understand cloud feedback
主讲人： Prof. Xianglei Huang, Department of Atmospheric, Oceanic, and Space Sciences, University of Michigan
间：日 15:10
地点：物理楼北539
同时转发到我的视友空间
您还可以输入140字
同时评论给 北京大学电视台radiative forcing on the surface的用法和样例：
He is honest only on the surface.
他只是表面诚实而已。
Hauglustain, D.A., Granier, C.,Brasseur, G.P.,and Megie , G. (1994),”The importance of atmospheric chemistry in the calculation of radiative forcing on the climate system”, J.Geophys.Res.
林清和，1990，台湾北部地区严重空气事件日之分析，国立台湾大学环境工程学研究所硕士论文。
On the surface, she's a charming, helpful person.
从表面上看，她又很动人又肯助人。
In many cases an overall drag coefficient is given so that the net force on the surface can be determined.
在许多情况下，总的拖曳系数是已知的，因而可以确定作用于表面上的净力值。
The wet glass left a mark on the surface of the table.
湿杯子在桌面上留下一个痕迹。
radiative forcing on the surface的海词问答与网友补充：
radiative forcing on the surface的相关资料：
相关词典网站：& Radiative Forcing of Climate by non-CO2 Atmospheric Gases
Radiative Forcing of Climate by non-CO2 Atmospheric Gases
Radiative Forcing of Climate by non-CO2 Atmospheric Gases
What is Radiative Forcing of Climate by Trace Gases?
Radiative forcing of climate by trace gases is commonly referred to as the "greenhouse
Solar radiation that passes through clouds and that is not reflected back to space
strikes the Earth's surface.
The longer wavelength (infrared) radiation created there is
reflected upwards, and then is absorbed by clouds and the greenhouse gases (GHGs
include carbon dioxide (CO2), methane (CH4), nitrous oxide (N2O), etc.).
constituents reradiate upwards and downwards, thereby heating the Earth's surface.
Earth's surface temperature is 35 K warmer than its effective blackbody temperature,
because of the presence of clouds and GHGs or called the natural greenhouse effect.
Increasing concentrations of GHGs can cause more warming (+ or positive values), and
vice-versa, decreasing means less warming or even cooling (- or negative values).
the entire group of climate forcing agents identified by the Intergovernmental Panel for
Climate Change (IPCC), the climate forcing for the well-mixed GHGs is the most certain
(left-most bar, Figure 1).
The total effective climate forcing for all GHGs
including CO2 and ozone (O3) from the beginning of the industrial revolution in 1750 to
the year 2000 is 2.63 watts per square meter.
As a good comparison, the natural
greenhouse effect that warms the Earth's surface by 35 K is, on average, ~150 watts per
square meter.
What are the non-CO2 greenhouse gases?
Like carbon dioxide, many non-CO2 atmospheric gases absorb in the infrared and
contribute to climate forcing.
The major non-CO2 GHGs or classes of gases listed by the
Kyoto Protocol of the United Nations Framework Convention on Climate Change are
CH4, N2O, hydrofluorocarbons (HFCs), sulfur hexafluoride (SF6), and perfluorocarbons
(PFCs, includes CF4 and C2F6, etc.).
Other classes of GHGs are included in the Montreal
Protocol for Substances that Deplete the Ozone Layer and its subsequent amendments
and are the chlorofluorocarbons (CFCs), halons, and chlorine- and bromine-
containing (halogenated) solvents (methyl chloroform (CH3CCl3), carbon tetrachloride
(CCl4), bromochloromethane (CH2BrCl), etc.).
Emissions of some of the non-CO2
GHGs may be more cost-effective or easier to limit or reduce than those of CO2.
vapor is a major greenhouse gas, but it is considered as a feedback in the climate system
related to the human activities on other greenhouse gases and by changes in land use
Why are the non-CO2 atmospheric gases important?
Radiatively speaking, the most important non-CO2 GHGs are CH4, N2O, CFCs, and
ozone (O3) (Figure 1).
The non-CO2 GHGs have added 1.17 watts per square meter
(44.5% of total from all GHGs) of climate forcing from 1750 to 2000.
Regardless of our
future national energy strategy (fossil fuels (oil, coal) versus renewable energy (solar,
wind, biofuels, tidal, etc.)), there will still exist the need to feed the ever-growing
population (N2O released thru fertilizer use), refrigerate food for storage (leakage and
release of the refrigerant, HFCs), and distribute electrical power (dielectric gases used
like SF6).
Many of the halogen-containing, non-CO2 atmospheric gases are also
stratospheric ozone-depleting gases including the CFCs, halons, chlorinated solvents, and
other halocarbons.
The stratospheric ozone depletion resulting from these ozone-
depleting gases has amounted to a -0.16 watt per square meter (medium understanding
compared to the well-mixed GHGs).
Tropospheric ozone, which is produced by man-made
emissions of O3-forming gases, has increased 35% from 1750 to 2000, and adds
0.35 watt per square meter with also a medium degree of uncertainty.
Source: IPCC, 2001
Figure 1. Major climate forcing agents and their forcing from the
beginning of the industrial revolution to 2000.
What do we know?
The physics of radiative forcing is well known, and the level of understanding in
the climate forcing from the well-mixed, longer lifetime GHGs is high.
The atmospheric lifetime of a GHG in the atmosphere is important to the length of
time that the gas affects climate forcing (time horizons used in climate forcing
calculations). Through chemical and inventory studies, the atmospheric lifetimes
for the majority of the GHGs are well known.
Concentrations of methane in the global atmosphere are leveling off (Figure 2).
Nitrous oxide and sulfur hexafluoride are increasing at a nearly constant rate
because of Earth's population's increased requirements for fertilizer and electrical
power distribution (Figures 2 and 3).
The Montreal Protocol and its subsequent amendments have decreased the
concentrations of many CFCs and chlorinated solvents where total equivalent
chlorine peaked in 1993-94 and has decreased by 8% by the end of 2005 (Figure
The growth rate for atmospheric concentration of the HCFC-14Xb series, CFC
replacement compounds, are slowing down as a result of reduced
production
in developed countries since 2004,
due to the Montreal Protocol and its subsequent amendments
(Figure 3).
The atmospheric growth of two of the key CFC replacements, HFC-134a and -
152a are increasing in the atmosphere.
It is predicted that the HFC-134a radiative
forcing will be as great or greater as all of the CFCs were in the early 1990s
(Figure 3)
Three long-term Northern Hemispheric station trends of O3 mixing ratios from
ozonesondes in the lower troposphere since 1970 show increases that were
significant (5-25% increase) in the first 10-15 years, however the most recent
15 years show a flat trend. Recent records of surface O3 from U.S. and global
background stations over the past 33 years from ESRL show a mixed picture with
some locations with increases and others with little change. Cape Point,
South Africa since 1990 (10% increase) and European stations since %)
have showed significant increases over time in tropospheric ozone.
The global total column of O3 has decreased 3% from before the 1980s to
period, mostly in the mid-latitudes.
The Antarctic Ozone Hole in the
Austral spring is still present.
However, there are indications from satellite
observations that mid-latitude stratospheric O3 may have started to recover at
some altitudes and during some of the seasons.
Once the Montreal Protocol is
under full compliance with halocarbon regulations (developing nations as well as
developed, and total elimination of the production of HCFCs), the positive climate
forcing from the ozone-depleting gases and the negative climate forcing from
decreased O3 concentrations should both be reduced while the ozone layer recovers
over the 21st century.
Boulder, Colorado balloon-borne observations have shown that stratospheric H2O has
increased, on average, 1% per year, from 1980 to 2006. The recent Boulder balloon
record () however shows no statistically significant change,
which is consistent with the slowdown of the growth rate of source gas, methane (Figure 2).
Global trends of the mixing ratios of the well-mixed greenhouse
gases versus time from NOAA observations.
Logarithmic (base 10) mixing ratios of radiatively-active
halocarbon and sulfur species versus time from NOAA observations.
What don't we know?
Why are the global atmospheric concentrations of methane leveling off?
theories exist to explain this occurrence but there is no definitive answer or
smoking gun.
Is the background level of the atmospheric cleanser, hydroxide radical, OH,
It could have major consequences for many GHGs, including
methane, HCFCs, and HFCs.
Our current understanding of the atmospheric emissions for the feedstock of the
CFCs, CCl4, does not allow us to predict its concentration in the atmosphere.
What is the fate of the short-lived halogen gases in the atmosphere, particularly
their bromine organic species?
Are they changing the total bromine in the
stratosphere via tropospheric-stratospheric exchange and natural and man-made
emissions?
What are the uptake and loss strengths, biological and chemical, of important non-CO2
greenhouse and ozone-depleting gases into and out of the ocean (methyl
halides, N2O, carbonyl sulfide (COS), etc.)?
There are no perfect replacements for either the fire extinguishing agents (halons)
or fumigants (methyl bromide).
When new replacement compounds are
considered economically feasible, then the chemistry and atmospheric lifetime
will need to be established for each replacement compound.
Some of the mid-latitude increase of stratospheric water vapor (1% per year) over
the period of
can be explained by the increase of atmospheric
methane, but not all.
Is this an early indication of the feedback of water vapor in
climate change, transport, or unknown chemistry?
What is NOAA's role?
Climate is one of the four major goals of NOAA.
NOAA's Earth System Research
Laboratory provides the expertise to conduct monitoring of the GHGs worldwide,
comparison of actual emissions with industrial inventories and/or modeled natural
emissions, run numerical models for radiative forcing and gas-phase chemistry, conduct
laboratory studies, and airborne and ground based field campaigns.
What will we need to know in the future?
We will need to better understand the feedback mechanisms involved in the most
important greenhouse gas, H2O, in the Earth's atmosphere.
Increased cloud cover will
block solar radiation from striking the ground, and cool the Earth's surface, while
increasing the water content of the atmosphere will increase warming.
Future climate
models will be required that include an encompassing system approach (chemistry,
transport, economical and societal factors) in order to adequately predict climate change.
Air quality, through changes in the tropospheric ozone concentration, reactive chemistry,
and the amount of the atmospheric cleanser, hydroxide radical, OH, may effect the
strength and sign of climate forcing.
Finally, how well are international agreements like
the Montreal and Kyoto Protocols working to control future emissions of these GHGs?
How does society benefit from this knowledge?
The research accomplished here is available to the public and scientists alike through the
web, peer-reviewed scientific literature, and "state of the art" assessments of climate and
ozone depletion.
NOAA provides the data and scientific analysis for public
policymakers to make informed decisions on how to deal with these environmental
problems facing the nation.
Theme Presentations
References
IPCC, Climate Change 2001:
The Scientific Basis, Contribution of Working Group I
to the Third Assessment Report of the Intergovernmental Panel on Climate Change,
edited by J. T. Houghton, Y. Ding, D.J. Griggs, M. Noguer, P.J. van der Linden, X. Dai, K.
Maskell, C.A. Johnson, pp. 881, Cambridge University Press, Cambridge, U.K., 2001.&&&direct radiative forcing
的翻译结果:
查询用时：0.602秒
&在分类学科中查询
STUDY OF THE DIRECT RADIATIVE FORCING IN EAST CHINA WITH MODIS-GOCART ASSIMILATED AEROSOL OPTICAL DEPTH
利用MODIS-GOCART气溶胶资料研究中国东部地区气溶胶直接辐射强迫
With the regional average, the largest direct radiative forcing during clear sky is in spring reaching -34.53W/m2 in the case of one and -59.25 W/m2
平均而言，中东部地区晴空时气溶胶直接辐射强迫以春季最大，case1时达-34.53W／m~2； case2时-59.25W／m~2；
Estimation of the Direct Radiative Forcing Due to Anthropogenic Sulfate over Eastern Asia
东亚地区人为硫酸盐的直接辐射强迫
Investigations show that the maximum of monthly average of surface concentrations of tropospheric ozone and sulfate aerosol in summer are 125×10~(-9) and 8 μg/m~3, respectively. The average direct radiative forcing due to sulfate aerosol is -0.92 W/m~2, which is strong in three regions of Southwest, South and East/Central China.
研究表明我国夏季对流层臭氧和硫酸盐的月均最大地面浓度分别为 1 2 5× 1 0 - 9和 8μg/m3.对流层臭氧的平均辐射强迫为 0 .3 9W /m2 ,硫酸盐气溶胶的平均直接辐射强迫为 - 0 .92W /m2 ,两者皆在西南、华南和华中地区出现极值中心 .
The direct radiative forcing at TOA is positive over land and negative or positive over sea,and its regional average values in Spring,Summer,Autumn,and Winter are 1.08,0.88,0.37,0.40W/m~2,respectively. The solar radiative forcing is also positive over land and negative or positive over sea, but the infrared radiative forcing is positive in the modeling region.
气溶胶大气顶直接辐射强迫基本呈现大陆上为正、海洋上正负均有的分布特征,区域平均辐射强迫在春夏秋冬分别为1.08,0.88,0.37,0.40W/m2,短波辐射强迫在陆上为正、海上正负均有,长波辐射强迫均为正值;
STUDY OF THE DIRECT RADIATIVE FORCING IN EAST CHINA WITH MODIS-GOCART ASSIMILATED AEROSOL OPTICAL DEPTH
利用MODIS-GOCART气溶胶资料研究中国东部地区气溶胶直接辐射强迫
With the regional average, the largest direct radiative forcing during clear sky is in spring reaching -34.53W/m2 in the case of one and -59.25 W/m2
平均而言，中东部地区晴空时气溶胶直接辐射强迫以春季最大，case1时达-34.53W／m~2； case2时-59.25W／m~2；
Estimation of the Direct Radiative Forcing Due to Anthropogenic Sulfate over Eastern Asia
东亚地区人为硫酸盐的直接辐射强迫
Investigations show that the maximum of monthly average of surface concentrations of tropospheric ozone and sulfate aerosol in summer are 125×10~(-9) and 8 μg/m~3, respectively. The average direct radiative forcing due to sulfate aerosol is -0.92 W/m~2, which is strong in three regions of Southwest, South and East/Central China.
研究表明我国夏季对流层臭氧和硫酸盐的月均最大地面浓度分别为 1 2 5× 1 0 - 9和 8μg/m3.对流层臭氧的平均辐射强迫为 0 .3 9W /m2 ,硫酸盐气溶胶的平均直接辐射强迫为 - 0 .92W /m2 ,两者皆在西南、华南和华中地区出现极值中心 .
The direct radiative forcing at TOA is positive over land and negative or positive over sea,and its regional average values in Spring,Summer,Autumn,and Winter are 1.08,0.88,0.37,0.40W/m~2,respectively. The solar radiative forcing is also positive over land and negative or positive over sea, but the infrared radiative forcing is positive in the modeling region.
气溶胶大气顶直接辐射强迫基本呈现大陆上为正、海洋上正负均有的分布特征,区域平均辐射强迫在春夏秋冬分别为1.08,0.88,0.37,0.40W/m2,短波辐射强迫在陆上为正、海上正负均有,长波辐射强迫均为正值;
A preliminary simulation study of direct radiative forcing of mineral dust aerosol over the East Asia region
东亚地区矿物尘气溶胶直接辐射强迫的初步模拟研究
Preliminary Simulation Research of Direct Radiative Forcing of Mineral Dust Aerosol over East Asia Region
东亚地区矿物尘气溶胶直接辐射强迫的初步模拟研究
On the base of it, Using the Fifth-Generation of PSU/NCAR Mesoscale Model (MM5 ) , we firstly simulated the spatial and temporal characteristics of sulfate aerosols direct radiative forcing and climate effects during clear sky over middle eastern China, then developed the sensible experiments for the sulfate aerosols direct radiative forcing and climate effects when doubling the aerosol optical depth and selected six small areas to compare the difference of the surface temperature.
在此基础上运用MM5模式先模拟了中东部地区硫酸盐气溶胶晴空直接辐射强迫的大小和气候响应的时空变化特征，然后开展了光学厚度加倍后硫酸盐气溶胶直接辐射强迫及其气候效应的敏感性实验研究，并选取6个不同的小区域，比较它们晴空地面气温响应的差异。
This work could be of benefit to the further study of the simulation of the urban aerosol direct radiative forcing.
本文工作有助于进一步探索气溶胶直接辐射强迫的数值模拟。
Then, we improve the China Regional Climate Model by adding aerosol radiative effect. With this model, we estimate the aerosol direct radiative forcing and seasonal variation of climate response to this forcing in China.
据此，在中国区域气候模式中考虑气溶胶的辐射影响，模拟中国地区气溶胶直接辐射强迫的大小及气候响应的季节变化特征。
COMPARISON OF ON-LINE AND OFF-LINE SIMULATION
METHODS FOR DIRECT RADIATIVE FORCING OF
ANTHROPOGENIC SULFATE
硫酸盐气溶胶直接辐射效应在线与离线模拟方法的比较
查询“direct radiative forcing”译词为用户自定义的双语例句&&&&我想查看译文中含有：的双语例句
为了更好的帮助您理解掌握查询词或其译词在地道英语中的实际用法，我们为您准备了出自英文原文的大量英语例句，供您参考。&&&&&&&&&&&&&&&&&&&& The results of the numerical simulations in Volcano-Climate research are svntheti- cally summarized.These simulation results show that the climate change in recent hun- dred to thousand years is closely related to the volcanism. The large volcano eruption would produce stratospheric warming by 4℃,yearly global-averaged surface cooling by 0.4℃,and monthly about 1℃,respectively. The spatial-temporal characteristics of the temperature drop connect with many factors,such as the eruption features(including latit... &&&&&&&&&&&&文章系统地总结了火山活动对气候影响的数值模拟研究，主要结论如下：近百年至千年的气候变化和火山活动关系密切，强火由喷发可造成平流层４℃以上的增温和地表年、月平均温度约０．４℃、１℃的下降。地表温度下降的时空分布受许多因素的影响，如火山喷发特征（包括喷发位置、季节、强度等）；海陆分布；火山气溶胶的光学特性；及其由直接辐射强迫引起的经向潜热输送的变化等等。同时还回顾了１９９１年皮纳图博喷发的有关研究及其对全球气候的可能影响的数值模拟工作。&&&&&&&& Using daily direct solar radiation and sunshine duration data, we retrieve the annual and monthly mean value of 0.75 μm aerosol optical depth in China to
analyze their geographical and temporal distribution. Then, we improve the China Regional Climate Model by adding aerosol radiative effect. With this model, we estimate the aerosol direct radiative forcing and seasonal variation of climate response to this forcing in China. The results show: Sichuan Basin is a high-valu... &&&&&&&&&&&&利用太阳直接辐射日总量和日照时数等多年观测资料，反演了中国地区大气气溶胶０?７５μｍ光学厚度的年、月平均值，分析了我国大气气溶胶状况的时空分布特征。据此，在中国区域气候模式中考虑气溶胶的辐射影响，模拟中国地区气溶胶直接辐射强迫的大小及气候响应的季节变化特征。计算结果表明：我国大气气溶胶光学厚度多年平均分布状况是以四川盆地为大值中心向四周减少；长江中下游武汉附近和南疆盆地为另两个大值中心；青藏高原为气溶胶低值区；我国绝大部分地区春季气溶胶光学厚度值最大，各地气溶胶光学厚度最小值出现的季节则有所不同。气溶胶辐射强迫介于－５?３～－１３Ｗ／ｍ２之间；辐射强迫具有春、夏季大，秋、冬季小，冬季南方偏大，夏季北方偏大的特征。气溶胶辐射强迫的分布与其光学厚度的分布基本一致。由于气溶胶的影响，中国大陆地区地面气温均有所下降，四川盆地到长江中下游地区以及青藏高原北侧到河套地区降温最为明显，分别可达－０?４ｏＣ和－０?５ｏＣ。气候响应具有明显的季节特征。地面气温的变化除与辐射强迫的大小有关外，还受大气环流的影响。&&&&&&&& There exist varieties of feedback mechanisms in climate system, and the different description of these climate feedback mechanisms within climate models is one of the major causes for the different responses of these models to the same direct radiative forcing (e.g., doubling CO??2?). Only when these mechanisms are fully understood and then properly represented, these climate models can be applied to the projection of future climate changes. As the first part of this paper, some basic conc... &&&&&&&&&&&&气候系统中存在着各种各样的气候反馈机制，而气候模式对这些反馈机制描述的差异，正是造成不同模式对同一直接辐射强迫（如二氧化碳加倍）的响应不同的主要原因。因此，只有正确描述气候系统中的各种反馈作用，气候模式才可能用来对未来的气候变化进行预测。为此，本文首先介绍了气候系统及模式反馈机制分析研究时所常用的一些概念，如气候敏感性参数、云辐射强迫等，随后概述了气候模式反馈机制比较分析时常用的各种方法，并指出了这些方法各自的优缺点。而详细的有关气候系统及模式中反馈作用及其机制的分析则在文章的第ＩＩ部分给出。&nbsp&&&&&&&&相关查询:
在Springer中查有关
在知识搜索中查有关的内容
在数字搜索中查有关的内容
在概念知识元中查有关的内容
在学术趋势中查有关的内容
2008 CNKI－中国知网
北京市公安局海淀分局 备案号：110 1081725
&2008中国知网(cnki) 中国学术期刊(光盘版)电子杂志社}