However, the scatter of crosses in Fig 4 indicates that this is a first-order estimate only. Most importantly, it ignores the effect of the distance from the sea. Fig 4. The variation of the annual range of temperature with latitude, using data from places in Africa, South America and Europe There we find an increase of annual range westwards. The range increases from 8 K by the ocean, to 12 K at km inland, and 17 K beyond km The equation is based on Fig 5 , which shows a much better fit.
Fig 5. A wet summer and dry winter suggests a low-latitude zenithal-rain or monsoonal climate. Monsoons generally occur between degrees of the equator, but over a few degrees further north in late summer over India, and, especially, southern China.
Frontal precipitation falls at latitudes between about degrees, but lower in winter. Between degrees, mainly at west coasts, the rainfall in winter is much greater than in summer. This is because fronts stay poleward in summer. The rainfall is more uniformly distributed along east coasts and in the interior in this latitude belt, not because fronts do penetrate into these regions in summer, but because of convective rainfall. Precipitation is heaviest near the ITCZ and in areas where monsoon winds come from over a warm ocean.
Rainfall is less on the lee side of a mountain, as in the case of the Patagonian desert in Argentina, to the east of the southern Andes, where the wind is from the west.
It is also less in the Gobi desert in Mongolia, not only because monsoonal moisture is trapped by the Tibetan plateau, but also because frontal systems have lost most of their moisture on their long travel from the Atlantic. Thus, dry conditions imply either a subtropical or polar latitude, an extreme elevation, a rain shadow, situation near an anomalously-cold ocean e. Such conditions are indicated by low rainfall figures and a large daily range of temperatures The daily range of temperature is the difference between the maximum and minimum temperatures in 24 hours.
It has no meaning at latitudes above If the daily range is large, the atmosphere is dry 18 and there is little cloud, probably indicated by low rainfall figures. Within anticyclones the air is dry and the sky often cloud-free; also, there is little wind, allowing the build-up of a strong nocturnal radiation inversion. Near the ITCZ and in areas frequented by frontal systems, not only does cloudiness limit daytime heating and nighttime cooling, but also, the air is too humid to cool much at night near the ITCZ or too windy at mid-latitudes.
There appears to be no systematic variation of the annual mean daily range with latitude e. The effect of the station elevation h, in km can be isolated: there is a slight tendency for the daily range to be given by this Fig 6 -. This equation means that a range of 12 K, say, suggests very tentatively an elevation of 2 km, i.
However, it would be better to use Fig 6 directly, as a guide to R d ; in that case, the deduced elevation for a daily range of 12 K would be about 1 km. The broad scatter in Fig 6 is not surprising: a place on the windward side of mountains has a much smaller daily range than a place at the same elevation on the lee side. Fig 6. At mid-to-high latitudes, land surface temperatures can vary throughout the year, but equatorial regions tend to remain consistently warm, and Antarctica and Greenland remain consistently cold.
The two most common temperature scales are the Fahrenheit and Celsius Centigrade scales. Two other scales, the Rankin and Kelvin are known as the absolute scales because at their zero points all molecular activity ceases.
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