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1.
E. Kuhlbrodt 《Meteorology and Atmospheric Physics》1954,7(1):170-187
Zusammenfassung Für die inneren Tropen läßt sich die Kenntnis der Höhenströmungen nur durch direkte Beobachtungen gewinnen. Für den Golf von Guinea liegen Messungen innerhalb der Breite 5° N bis 9° S von drei Profilen der Meteor-Expedition und von zwei Studienfahrten der Deutschen Seewarte vor. Eine Voruntersuchung der mittleren Windwerte für die einzelnen benachbarten 5°-Felder einer Breitenzone (gleicher Jahreszeit) ergibt weigehende Übereinstimmung. Deshalb wird die zusammengefaßte Länge 10° W bis 5° E (für jede Breitenzone) der statistischen Bearbeitung zugrunde gelegt. Ziel der Untersuchung ist, die sich bei der Höhenwind-Statistik deutlich heraushebenden, charakteristischen Hauptströmungen zu beiden Seiten des Äquators und im jahreszeitlichen Unterschied zu erkennen und zahlenmäßig zu diskutieren. Nach einer Darstellung der Schichtung der mittleren Komponenten für 0 bis 19 km Höhe werden die einzelnen Strömungssysteme an Hand von Tabellen und Abbildungen näher beschrieben. Untere Troposphäre: Monsun, Antimonsun; Passat. Mittlere Troposphäre: Ostströmung (Urpassat). Hohe Troposphäre: Hohe Westströmung (Anti-Urpassat). Tropopausen-Schicht: Übergang von W in hohen Ost (Oberpassat). Hierbei wird für Test-Höhen die Streuung der beobachteten Einzelwinde besprochen. Größte gemessene Einzelgeschwindigkeit nahe dem Äquator: in der E-Strömung: SE 20 m/s (9 bis 10 km), in der hohen W-Strömung: SW 21 m/s (15 bis 16 km, nördlich vom Äquator), NW 21 m/s (13 bis 14 km, südlich vom Äquator). Die Rolle des Äquators bei den Höhenströmungen (meridionale Komponente) wird zusammenfassend betrachtet.
Mit 5 Textabbildungen. 相似文献
Summary Knowledge on the currents of the upper atmosphere in the inner tropics can be obtained only by direct observations. In the Gulf of Guinea, between the latitudes 5° N and 9° S, three profiles were determined by the Meteor expedition and measurements carried out by two expeditions of the Deutsche Seewarte. A preliminary test of the average wind values gives good agreement for all adjoining 5°-fields of a zone of latitude (during the same season). Therefore, the longitude 10° W-5° E as a whole (for every zone of latitude) could be applied to statistical evaluation. Purpose of this investigation is to establish and discuss quantitatively the characteristic mean currents on both sides of the equator such as result from the wind statistics of the upper atmosphere in their seasonal variations. The distribution of the mean components is given for 0–19 km altitude; the different systems of currents are described in detail by tables and illustrations. Lower troposphere: monsoon, anti-monsoon; trade-wind. Medium troposphere: easterlies (Urpassat). High troposphere: high west-wind (Anti-Urpassat). Tropopause: transition from west to high east-wind (Oberpassat). For certain test heights the dispersion of the different observed winds is discussed. Measured maximum velocities near equator: in the eastern current: SE 20 m/s (9–10 km), in the western current: SW 21 m/s (15–16 km, north of equator), NW 21 m/s (13–14 km, south of equator). The rôle of the equator in connection with high currents (meridional component) is discussed comprehensively.
Résumé On ne peut connaître l'allure de la circulation dans la haute atmosphère de la zone tropicale que par des observations directes. Dans le Golfe de Guinée on dispose de trois profils obtenus entre 5° N et 9° S par l'expédition du «Meteor» et de deux croisières d'étude de la Deutsche Seewarte. Une étude préalable des valeurs moyennes de vent relatives aux diverses surfaces de 5° d'une zone (mêmes saisons) aboutit à des résultats très concordants; aussi a-t-on soumis à l'examen statistique chaque bande zonale de 5° allant de 10° W à 5° E de longitude. Le but de cette recherche est de mettre en évidence les principaux courants en altitude de part et d'autre de l'équateur et d'examiner leurs valeurs numériques dans leurs variations saisonnières. Après avoir représenté la stratification des composantes moyennes entre 0 et 19 km, on décrit les différents systèmes de courants à l'aide de tableaux et de croquis et qui sont les suivants. Troposphère inférieure: mousson et contre-mousson; alizés. Troposphère moyenne: courant d'Est (Urpassat). Troposphère supérieure: courant d'Ouest supérieur (Anti-Urpassat). Tropopause: transition du courant d'Ouest à celui d'Est (Oberpassat). A cet effet on discute la dispersion des vents observés pour des niveaux choisis. Vitesse maximum observée près de l'équateur: dans le courant d'Est SE 20 m/s (à 9–10 km), et dans le courant d'Ouest supérieur SW 21 m/s (à 15–16 km au Nord de l'équateur), NW 21 m/s (à 13–14 km au Sud de l'équateur). On considère en résumé le rôle de l'équateur dans les courants en altitude (composante méridienne).
Mit 5 Textabbildungen. 相似文献
2.
《Atmospheric Science Letters》2001,2(1-4):18-24
At Tromsø (69°N; 19°E), ionospheric data from 1952 onwards indicate that the mean altitude of the F2 layer is dropping by 4 km per decade on average. This effect is thought to be attributable to middle atmosphere cooling due to increasing concentrations of anthropogenic carbon dioxide and methane. 相似文献
3.
R. R. Reddy K. Rama Gopal L. Siva Sankara Reddy K. Narasimhulu K. Raghavendra Kumar Y. Nazeer Ahammed C. V. Krishna Reddy 《Journal of Atmospheric Chemistry》2008,59(1):47-59
In the present study, an attempt has been made to examine the governing photochemical processes of surface ozone (O3) formation in rural site. For this purpose, measurements of surface ozone and selected meteorological parameters have been
made at Anantapur (14.62°N, 77.65°E, 331 m asl), a semi-arid zone in India from January 2002 to December 2003. The annual
average diurnal variation of O3 shows maximum concentration 46 ppbv at noon and minimum 25 ppbv in the morning with 1σ standard deviation. The average seasonal
variation of ozone mixing ratios are observed to be maximum (about 60 ppbv) during summer and minimum (about 22 ppbv) in the
monsoon period. The monthly daytime and nighttime average surface ozone concentration shows a maximum (55 ± 7 ppbv; 37 ± 7.3 ppbv)
in March and minimum (28 ± 3.4 ppbv; 22 ± 2.3 ppbv) in August during the study period. The monthly average high (low) O3 48.9 ± 7.7 ppbv (26.2 ± 3.5 ppbv) observed at noon in March (August) is due to the possible increase in precursor gas concentration
by anthropogenic activity and the influence of meteorological parameters. The rate of increase of surface ozone is high (1.52 ppbv/h)
in March and lower (0.40 ppbv/h) in July. The average rate of increase of O3 from midnight to midday is 1 ppbv/h. Surface temperature is highest (43–44°C) during March and April months leading to higher
photochemical production. On the other hand, relative humidity, which is higher during the rainy season, shows negative correlation
with temperature and ozone mixing ratio. It can be seen that among the two parameters are measured, correlation of surface
ozone with wind speed is better (R
2=0.84) in compare with relative humidity (R
2=0.66). 相似文献
5.
Sarbari Ghosh Utpal Kumar De Atmospheric Science Research Department of Physics Jadavpur University Calcutta India Received April revised July 《大气科学进展》1997,(1)
ＡＣｏｍｐａｒａｔｉｖｅＳｔｕｄｙｏｆｔｈｅＡｔｍｏｓｐｈｅｒｉｃＬａｙｅｒｓｂｅｌｏｗＦｉｒｓｔＬｉｆｔｉｎｇＣｏｎｄｅｎｓａｔｉｏｎＬｅｖｅｌｆｏｒＩｎｓｔａｎｔａｎｅｏｕｓＰｒｅ－ＭｏｎｓｏｏｎＴｈｕｎｄｅｒｓｔｏｒｍＯｃｕｒｅｎｃｅａｔＡｇａ... 相似文献
6.
使用日本静止气象卫星(GMS)观测的候平均云量资料,分析了1978年5月—1984年12月和1978年5月—1981年12月两个时期内,印度洋中部(90°E)至太平洋(170°W)热带地区云量的低频变化特征。主要结果如下: 1.考查地区的云量存在两类低频振荡:30—60天的季节内振荡和周期为2—4年的年际振荡(可称之为甚低频振荡)。 2.在非厄尼诺时期,30—60天的低频振荡较明显,可以一直东传到中太平洋;有厄尼诺影响时,它的东传过程将受到抑制,主要限于130°E从西地区。 3.130°E以西地区的2—4年振荡,主要与厄尼诺/南方涛动的信息有关;在非厄尼诺时期,这一类振荡消失。 相似文献
7.
On the basis of the analysis of atmospheric carbon dioxide concentration variations and the annual mean air temperature at Syowa Station, Antarctica in the period of 1984-1988, the following results are easily obtained:(1) The annual mean values of the atmospheric carbon dioxide concentration are gradually increased and equal to 342.59, 343.80, 345.15, 346.83 and 348.82 ppmv for 1984, 1985, 1986, 1987 and 1988, respectively. Its annual increase rates are 1.21, 1.35, 1.68 and 1.99 ppmv/yr. For 1984-1985, 1985-1986, 1986-1987 and 1987-1988, respectively and are raised year by year.The seasonal variations are observed and the maximum concentration is in spring and the minimum one is in late-summer or early-autumn.(2)The increasing tendency of the concentration of the atmospheric carbon dioxide is consistent with that of the a.ir temperature. 相似文献
8.
2期 热带气象资料室:156oE、180”E逐候总云量剖面资料 187 来11S6”Efff总云邑(1160.S一19BI.4) — —人188 热 带 气 象 二卷 4＄,—— 5016 5 5 T 5 5 6 7 7 9 9 9 9 8 9 9 8 9 9 9 8 8 8 9 48i 8 6 T 8 sl6 7 7 8 8 8 8 T 8 9 9 9 7 9 8 8 9 8 4617 7 7 6 2 2 7 8 6 8 8 7 相似文献
9.
广东省热带海洋气象研究所热带气候资料室 《热带气象学报》1985,(3):280-285
Pgr纬度在:1981年12月20至ZI日缺资料广东省热带沟洋气象研究所热带气候资料室156e巨、180”Effi候总云量剖面资料282 i热 带 气 象3卷 156“E逐候总云量坛\日 阶 01/106 11 16 21 26 31 05 10 15 ZQ 2502 07 12 1722 27 01/4 06 11 16 21 26 ”\31 1015 20 25 30 04/2 09 14 1 相似文献
10.
广东省热带海洋气象研究所热带气象资料室 《热带气象学报》1984,(1):99-107
为准足热带气象科研需要,我室整理了气象常规观测资料较缺乏的中太平洋上156°E和180°E两经线自1978年5月以来的逐候总云量,在本刊分期连载,每期给出上述两经度十二个月(73候)总云量剖面资料,直至载完为止。本资料来自日本东京气象卫星中心发行的《气象卫星月报》。资料表以纬度为纵座标,时间为横座标,列成可直接分析使用的剖面,其南北宽度为50°N—48°S,资料点距为2个纬度;资料中99表示陆地;10表示云量大于9.5。 相似文献
11.
12.
G. S. GOLITSYN 《大气科学进展》2009,26(3):585-598
The goal of this paper is to quantitatively formulate some necessary conditions for the
development of intense atmospheric vortices. Specifically, these criteria are discussed for tropical
cyclones (TC) and polar lows (PL) by using bulk formulas for fluxes of momentum, sensible heating,
and latent heating between the ocean and the atmosphere. The velocity scale is used in two forms: (1)
as expressed through the buoyancy flux b and the Coriolis parameter lc for rotating fluids convection,
and (2) as expressed with the cube of velocity times the drag coefficient through the formula for
total kinetic energy dissipation in the atmospheric boundary layer. In the quasistationary case the
dissipation equals the generation of the energy. In both cases the velocity scale can be expressed
through temperature and humidity differences between the ocean and the atmosphere in terms of the
reduced gravity, and both forms produce quite comparable velocity scales. Using parameters b and lc,
we can form scales of the area and, by adding the mass of a unit air column, a scale of the total
kinetic energy as well. These scales nicely explain the much smaller size of a PL, as compared to
a TC, and the total kinetic energy of a TC is of the order 1018-1019 J. It will be shown
that wind of 33 m s-1 is produced when the total enthalpy fluxes between the ocean and the
atmosphere are about 700 W m-2 for a TC and 1700 W m-2 for a PL, in association with
the much larger role of the latent heat in the first case and the stricter geostrophic constraints
and larger static stability in the second case. This replaces the mystical role of 26oC as
a criterion for TC origin.
The buoyancy flux, a product of the reduced gravity and the wind speed, together with the atmospheric
static stability, determines the rate of the penetrating convection. It is known from the observations
that the formation time for a PL reaching an altitude of 5--6 km can be only a few hours, and a day, or
even half a day, for a TC reaching 15--18 km. These two facts allow us to construct curves on the plane
of Ts and ΔT=Ts-Ta to determine possibilities for forming an intense vortex. Here, Ta is the atmospheric temperature at the height z=10 m. A PL should have ΔT>20oC in accordance
with the observations and numerical simulations. The conditions for a TC are not so straightforward but
our diagram shows that the temperature difference of a few degrees, or possibly even a fraction of a
degree, might be sufficient for TC development for a range of static stabilities and development times. 相似文献
13.
G. S. GOLITSYN 《大气科学进展》2009,26(3)
The goal of this paper is to quantitatively formulate some necessary conditions for the development of intense atmospheric vortices. Specifically, these criteria are discussed for tropical cyclones (TC) and polar lows (PL) by using bulk formulas for fluxes of momentum, sensible heating, and latent heating between the ocean and the atmosphere. The velocity scale is used in two forms: (1) as expressed through the buoyancy flux b and the Coriolis parameter lc for rotating fluids convection, and (2) as expressed with the cube of velocity times the drag coefficient through the formula for total kinetic energy dissipation in the atmospheric boundary layer. In the quasistationary case the dissipation equals the generation of the energy. In both cases the velocity scale can be expressed through temperature and humidity differences between the ocean and the atmosphere in terms of the reduced gravity, and both forms produce quite comparable velocity scales. Using parameters b and lc., we can form scales of the area and, by adding the mass of a unit air column, a scale of the total kinetic energy as well. These scales nicely explain the much smaller size of a PL, as compared to a TC, and the total kinetic energy of a TC is of the order 1018 - 1019 J. It will be shown that wind of 33 m s-1 is produced when the total enthalpy fluxes between the ocean and the atmosphere are about 700 W m-2 for a TC and 1700 W m-2 for a PL, in association with the much larger role of the latent heat in the first case and the stricter geostrophic constraints and larger static stability in the second case. This replaces the mystical role of 26~C as a criterion for TC origin. The buoyancy flux, a product of the reduced gravity and the wind speed, together with the atmospheric static stability, determines the rate of the penetrating convection. It is known from the observations that the formation time for a PL reaching an altitude of 5-6 km can be only a few hours, and a day, or even half a day, for a TC reaching 15-18 km. These two facts allow us to construct curves on the plane of Ts and △T= Ts - Ta to determine possibilities for forming an intense vortex. Here, Ta is the atmospheric temperature at the height z = 10 m. A PL should have △T > 20℃ in accordance with the observations and numerical simulations. The conditions for a TC are not so straightforward but our diagram shows that the temperature difference of a few degrees, or possibly even a fraction of a degree, might be sufficient for TC development for a range of static stabilities and development times. 相似文献
14.
15.
本文利用西南太平洋地区近12年的热带气旋资料,给出了热带气旋活动频数;同时还运用达尔文区域气象中心发布的部分资料,结合1984至85年度热带气旋活动的特点,从多种不同角度讨论和分析了热带气旋活动多和少的不同环流特征,找出热带气旋发生较为有利的地区。最后还发现该区域热带气旋移动的引导层可能不同于西北太平洋地区,以及一种南太平洋地区热带气旋形成的高低层流场配置。 相似文献
16.
A comprehensive study on the chemistry of deposition and the concentration of tropospheric ozone and particulate sulfate in the ocean atmosphere was carried out for the data sets in 1990’s. It is important to study the atmospheric situation over the past years as well as the latest, especially in the East Asian region where emission amount of anthropogenic air pollutants have increased year by year due to rapid economic growth. The survey was conducted for 5 years in East Asia and West Oceania (35°N–35°S, 100–135°E) in August and September in 1990’s. The purpose of the survey was to study and understand the chemistry of deposition and the concentration of tropospheric ozone and particulate sulfate in the ocean atmosphere comprehensively in one project. Rainfall over the ocean was insufficiently neutralized. Gas and aerosol over the ocean were mature, i.e., well-mixed, during the period of the transportation. The characteristic latitudinal dependence was observed in the tropospheric ozone concentration, namely, higher in the southern hemisphere and lower in the northern hemisphere (approximately 25 ppb in the 10–40°S region and 5–15 ppb in the 20–40°N region). On the other hand, high concentrations of tropospheric ozone of over 30 ppb were observed in the northern hemisphere, which was attributable to the long-range transportation. The TSP concentration was approximately under the level of 40 μg m?3 irrespectively of the latitude; in contrast, the nss-SO4 2- concentration showed a clear latitudinal dependence, i.e., higher in the northern hemisphere and lower in the southern hemisphere. The background levels of the nss-SO4 2- concentration were approximately 0.5 μg m?3 in the 10–40°S region and 2–3 μg m?3 and 4–5 μg m?3 in the 0–20°N and 20–40°N regions, respectively. 相似文献
17.
18.
《气象》2006,(4)
日12345678910111213141516171819202122232425262728数5113158199214266344338269270324298239188208289294279315288269195191269305313259270120°E14161514(14)1312141414(14)(15)14141514141414151715(14)(14)(14)(14)(13)(12)130°E13141615151413151415(15)16151516151516151617(15)15(15)(14)(14)(14)(14)140°E131516151615151515141516161617161617171717(16)15(15)(15)(15)15(15)2006年2月亚洲地区逐日500hPa西风环流指数及副热带高压脊线(120°E、130°E、140°E)位置$中央气象台中期预报科~~… 相似文献
19.