氣象專業(yè)英語6講課教案

1、氣象專業(yè)英語612. Reside vi. 駐扎；駐扎； resident 居民居民13. Southern Oscillation 南方濤動；南方濤動； North Atlantic Oscillation (NAO) 北大西洋濤動北大西洋濤動 Arctic Oscillation (AO) 北極濤動；北極濤動；Antarctic Oscillation (AAO)南極濤動；南極濤動； Quasi-Biennial Oscillation (QBO) 準兩年振蕩準兩年振蕩 Seesaw 翹翹板；翹翹板； Fluctuation n. 振蕩，振蕩， 擾動；擾動；Perturbation n.

2、擾動擾動14. Passive a. 消極的，被動的；消極的，被動的； active a. 主動的主動的15. Quasi-biennial oscillation 準兩年振蕩準兩年振蕩 *quasi+ 準準 （approximate, not exact) For example, quasi-static 準靜力；準靜力； quasi-geostrophic 準地轉(zhuǎn)的；準地轉(zhuǎn)的； quasi-stationary front 準靜止鋒，準靜止鋒，etc. * biennial 兩年一次；兩年一次； biannual 一年兩次一年兩次16. Condensation n. 濃縮，凝結(jié)濃縮，凝

3、結(jié); condense vt.17. Convergence n. 匯合，輻合；匯合，輻合； divergence n. 輻散；輻散； 散度散度18. gradients n. 梯度梯度 ； temperature gradients, pressure gradients, SST gradients, etc.19. Anomaly n. 不規(guī)則，異常；不規(guī)則，異常；anomalies復(fù)數(shù)復(fù)數(shù)20. Hypothesize v. 假想；假想； hypothesis n. ; hypotheses 復(fù)數(shù)復(fù)數(shù) 21. Instability n. 不穩(wěn)定性；不穩(wěn)定性； stability 穩(wěn)定

4、性；穩(wěn)定性； unstable adj. 不穩(wěn)定的不穩(wěn)定的 in+ 否定否定 （構(gòu)詞法）（構(gòu)詞法） inaccurate 不精確，不精確， invisible 不可見，不可見，incompressible 不可壓縮不可壓縮 independent 獨立；獨立； inhomogeneous 不均勻；不均勻； informal 非正式非正式22. Orographic barrier 地形分界線；地形分界線； topographic23. Spatial coherence 空間相干性；空間相干性； spatial adj. 空間的；空間的； temporal adj. 時間的時間的 二、Mete

5、ology Today 有關(guān)MONSOON內(nèi)容三、氣象科技英語900句 有關(guān)MONSOON內(nèi)容四、課文內(nèi)容 The term “monsoon” appears to have originated from the Arabic word mausim which means season. It is most often applied to the seasonal reversals of wind direction along the shores of the Indian Ocean, especially in the Arabian Sea, that blow from

6、 the southwest during one half of the year and from the northeast during the other. As monsoons have come to be better understood, the definition have been broadened to include almost all of the phenomena associated with the annual weather cycle within the tropical and subtropical continents of Asia

7、, Australia, and Africa and the adjacent seas and oceans. It is within these regions that the most vigorous and dramatic cycles of weather events on the earth take place.Paragraph 1 The dominant characteristic of the great monsoon systems, the annual cycle itself, has led the inhabitants of the mons

8、oon regions to divide their lives, customs, and economics into two distinct phases: the “wet” and the “dry”. The “wet”, of course, refers to the rainy season, during which warm moist and very disturbed winds blow inland from the oceans. The dry refers to the other half of the year, when the wind rev

9、erses bringing cool and dry air from the hearts of the winter continents. In some locations, the cold and dry winter air flows across the equator toward the hot continents of the summer hemisphere. In this manner, the dry of the winter monsoon is tied to the wet of the summer monsoon, and vice versa

10、.Paragraph 2 Surface winds during northern hemisphere a) summer b) winterIn this article, we shall concentrate mainly on the annual cycle of the monsoon. However, it is incorrect to think of summer and winter phases of the monsoon as just prolonged periods of rain or drought, each of some months dur

11、ation. There are also significant variations that exist on time scales ranging from days to weeks. Thus , while the monsoon appears to have a well-defined annual cycle, closer inspection shows that the monsoon varies substantially and that within the cycles a significant substructure exists that bec

12、omes evident as the intensity of the monsoon rains wax and wane through the wet season.Paragraph 3Paragraph 4Short-term variations include the individual weather disturbances （ i.e., a period of disturbed weather or storms lasting some days) that occur in rapid succession during the so-called active

13、-monsoon periods. A prolonged period of one to several weeks marked by an absence of weather disturbances is called a break-monsoon, or more correctly, a break in the active monsoon. During an active phase the weather is unstable with frequent storms that produce the rain deluges traditionally assoc

14、iated with the monsoon. But , during a dormant or break phase of the monsoon, the weather is hot, clear, and dry. Monsoon breaks are drought period and , if prolonged, may cause considerable hardship and even famine in the monsoon lands. In the course of the Southwest monsoon, there are periods when

15、 the monsoon trough shifts northwards to the foot of the Himalayas, and rains decrease over much of India except along the slopes of the Himalayas and parts of Northeast India, and the Southern peninsula. This synoptic situation is called break in monsoon. The break are most frequent in July and Aug

16、ust, and they typically last from a few days to three weeks.Mean pressure departure,03GMT, in mb, during break in monsoon. From Rao(1976)Fig.3.20 Percentage rainfall departure in peak phase of break in monsoon. Symbols are as follows: cross-hatching excess of +50% or more; simple hatching excess of

17、+1 to 49%; thin dot raster deficit of 1 to 49%; thick dot raster deficit of 50% and beyond. From Rao(1976)Paragraph 5 A variable of the monsoon system of considerable importance is the timing of the commencement of the set. This , the so-called onset of the monsoon, is usually sudden with the weathe

18、r changing abruptly from the premonsoon heat (similar to the torrid climate of the break-monsoon), to the weather disturbances, storms, and intense rainfall of an active period. For a farmer knowledge of when the onset will occur is critical as with it resides the key to the timing of the planting o

19、f his crops. The withdrawal of the monsoon ( i.e., the cessation of rainfall over the continents) during the early autumn is a much more gradual transition than the onset. Das(1984) describes the following working rules used to define the onset of the monsoon over Kerala: (i) starting with 10 May, i

20、f at least 5 out 10 stations in Kerala report 24 hour rainfall totals of 1 mm for two consecutive（連續(xù)的） days, an onset is declared on the second day; (ii) if 3 out of 7 stations in Kerala report no rainfall for the next 3 days, indication are given for a recession （撤回）of the monsoon; (iii) after the

21、monsoon has advanced North of 13N even a temporary recession is a rare event. Das futher mentions that there are similar working rules for other parts of India.Normal dates of (a) onset, and (b) withdrawal of Southwest monsoon over India. From Rao (1976) (copyright by the Government of India).Onset

22、and withdrawal of monsoon over IndiaOnsetWithdrawalParagraph 6Relationships between the Indian monsoon rainfall and the Southern Oscillation were established by Walker in the beginning of this century and versions of them have been used since for operational forecasting of monsoon rainfall. It is, t

23、herefore, useful to reexamine the relationship by using the Darwin sea level pressure for the period 1901-1981. Darwin pressure is chosen because its long-term record is considered to be more accurate and more complete than that for any other station in that region. Although Tahiti minus Darwin pres

24、sure is considered to be better index of the Southern Oscillation, Tahiti pressure is available only for the period 1935-1981, and for this period the correlation coefficient between the spring TahitiParagraph 6 ( to be continued)pressure and Indian monsoon rainfall is only 0.01. The summer monsoon

25、rainfall data used in this study is the area weighted average of the percentage departure for each of the 31 subdivisions of India, and is referred to as the whole Indian monsoon rainfall anomaly.Paragraph 7 and 8If one is going to predict monsoon rain, it is necessary to examine the Southern Oscill

26、ation before the monsoon. However, it should be recalled that one of Walkers most important findings was that monsoon rainfall has very significant correlations with the subsequent global circulation.Paragraph 8The most remarkable of Walkers results was his discovery of the control that the Southern

27、 Oscillation seemingly exerted upon subsequent events and in particular of the fact that the index for the Southern Oscillation as a whole for the summer quarter June-August, had a correlation coefficient of 0.8 with the same index for the following winter-quarter, though only of 0.2 with the previo

28、us winter quarter. Paragraph 8 (to be continued)It is quite in keeping with this that the Indian monsoon rainfall has its connections with later rather than earlier events. The Indian monsoon therefore stands out as an active, not a passive feature in world weather more efficient as a broadcasting t

29、ool than as an event to be forecast.Paragraph 9 During the recent years we have gained a better understanding of large-scale atmospheric phenomena such as El Nino and the Southern Oscillation, the quasi-biennial oscillation and atmospheric blocking. This new knowledge provides a better synoptic and

30、dynamical framework to examine the interannual and long-term variability of monsoon. The El Nino Southern Oscillation seems to be the single most important feature of the ocean-atmosphere systems. Its period is quite large (2-5 years) and therefore it can be of practical value for predicting fluctua

31、tions of a seasonal phenomenon like the monsoon. It is therefore necessary to document the main features of the global circulation, including the monsoon, during different phases of the Southern Oscillation. It should, however, be recognized that the fluctuations of the monsoon can also be one of th

32、e important factors affecting the Southern Oscillation.Paragraph 9 (to be continued)Paragraph 10 The prospects for long-range forecasting of large-scale, seasonal mean monsoon rainfall appear to be good. There are significant correlations between large-scale seasonal mean Indian (rainfall) anomalies

33、 and low-frequency changes in the Southern Oscillation. There are also significant correlations between seasonal Indian rainfall anomalies and slowly varying boundary conditions of sea surface temperature and snow cover.Paragraph 11Tropical and monsoon flows are dominated by the thermally forced pla

34、netary scale Hadley and Walker type circulations for which the primary energy source is the latent heat of condensation. The large-scale moisture convergence required for the release of the latent energy is organized by gradients of temperature at the earths surface. Solar heating can produce therma

35、l low-pressure areas over the land which can further deepen due to latent-heating if the dynamical circulation is favorable for moisture convergence. Therefore fluctuations of soil moisture can influence the intensity of the tropical heat sources over the land. Paragraph 11 (to be continued) Similar

36、ly, the tropical heat source over the oceans can be influenced by the anomalies of sea surface temperature. It is therefore reasonable to expect that the changes in the large-scale tropical flows would be related to the changes in the slowly varying boundary conditions at the earths surface. Since d

37、ynamical instabilities are not too strong in the tropics, it is also reasonable to hypothesize that the changes in the large-scale flows are dominated by the changes in the boundary conditions. Therefore arguments collectively suggest that there is a physical basis for predictability of the large-scale,seasonally averaged monsoon flow and rainfall.P