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There is a temporary drop in February, followed by a partial recovery in the autumn, but the flow is least in winter. The third factor is the convection which takes place during periods of light winds, clear skies, and intense sunshine, especially when the preceding winds have brought cold air over the land from the south. After conditions of the type mentioned have endured for several days, the convection is likely to be so intense as to produce local showers.

These are often heavy, sometimes accompanied by thunder, and occasionally of the nature of local cloud-bursts. Rainfall of this type is most common in the interior of continents. Being caused by solar radiation, it is most frequent when solar radiation is strongest—namely, in summer.

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According to type B, therefore, we would have a relatively wet summer and a dry winter. Type C is developed strongly in Westland and the south-west Fiord country. It is shown fairly well by Hokitika, but much more distinctly if the data for a number of West Coast stations be combined. It is dominant in the far South, in the mountains of Nelson, and in the portion of the North Island not yet referred to. In this latter area, however, types A and C combine in varying proportions.

Most districts show the effect of the westerly winds in a relatively high rainfall in October, but this is least noticeable in the low country east of the main ranges. The areas where type C dominates are those with the heaviest rainfall. Type B is dominant in the interior and southern portions of Canterbury and the central and eastern portions of Otago, and is especially characteristic of the dry areas of the provinces mentioned.

The summer rains of this type are of great importance to the farming communities in the interior of Canterbury and Otago. Next to the amount and the annual variation of precipitation, the frequency with which it falls is its most important characteristic. In Table 2 the average number of days with rain in each month is given for some representative stations. A day with rain is one on which 0. Generally speaking, there is a fairly close relationship in New Zealand between the amount of rain and the number of rain days, but the latter is not directly proportional to the rainfall.

There are considerable areas on the west coast of the South Island, for instance, which have ten or more times as much rain as the driest portions of the interior, but only about double the number of rain days. Marlborough seems to have a small number of wet days compared with its rainfall.

To the south of New Zealand there is a rapid increase in cloudiness, showers fall with great frequency, and the number of rain days becomes high. New Zealand is extremely fortunate in that, even where the rainfall is very heavy, intervals between rains are almost everywhere sufficiently frequent and prolonged to ensure adequate drainage, while there is enough sunshine to dry the soil surface. Otherwise, large areas in the west and south would be covered with peat. Temperature is no less important than rainfall in determining the living conditions of a country and the yield from its soil.

But it is much less variable, and in the Southern Hemisphere especially, is largely determined by latitude. Its influence is therefore taken much more for granted.

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The specification of the temperature of a place is, however, not so simple a matter as might appear. Many different factors are involved in the determination of the precise temperatures experienced in any locality. The sea, for instance, responds very slowly to both daily and yearly changes in the amount of heat received from the sun, while on the land the response is rapid.

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Consequently, the nearer a station is to the sea the smaller are its daily and yearly fluctuations of temperature. It is to this effect that the principal difference between a continental and a marine climate is due. Although New Zealand is narrow, the high ranges shield the country to the east of them to a considerable extent, so that there is a nearer approach to continental conditions than would otherwise be expected, particularly in the interior of Canterbury and Otago.

Again, on plain country the air tends to stagnate, especially at night.



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At night-time the surface layer cools rapidly through radiation from the ground, while during the day it becomes heated by the sun. There is less stagnation in the warm layer of the daytime than in the cold layer of the night. Consequently, stations on level plains or plateaux tend to be subject to frost and to have a relatively low mean temperature. The effect is accentuated near the slopes of hills because the cold air flows away down the slopes to lower levels.

The hills, therefore, gain freedom from frost at the expense of the plains. In windy situations, also, the susceptibility to frost is lowered owing to the prevention of stagnation. Apart from the effects due to air-drainage and windiness, the temperature decreases with altitude.



It is unsound, therefore, to compare, for example, temperatures recorded at Thorndon, Wellington, which was only 12 ft. Such a procedure would lead to the erroneous conclusion that the climate had become colder. If charts of mean temperature are to be prepared it is clear that they will be very complicated, especially in a mountainous country like New Zealand, owing to this effect of altitude. This has been done in Table 3.

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The Rotorua values, for example, have been increased by 2. If the actual temperature is required, it can be found by reversing this process. In New Zealand publications it has been the general practice to derive monthly mean temperatures from the means of the daily maximum and minimum.

But, even on the average, the mean of the maximum and minimum differs slightly from the true mean for the day. The correction to the mean for the day has been determined from the records of thermographs with fair accuracy at Wellington and more roughly at several other places. In Table 3 , therefore, the temperatures are reduced to sea-level and mean of day. For the remainder of the temperature tables the observed readings have been used without correction. All are in Fahrenheit degrees. Table 3. Mean Temperature reduced to Sea-level.

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Average of period of years. The stations given in the above table were chosen with a view to illustrating the effect of changing latitude, the difference between east and west coasts, especially in the South Island, and the contrast between coastal and inland conditions. The preceding tables Nos. Corresponding information regarding minimum temperatures follows. This gives some idea of the susceptibility to severe frosts, such as would affect fruit-trees. The last line gives the number of ground frosts. According to the British Convention, a ground frost is recorded when the grass minimum thermometer falls below In the preparation of these tables some of the older records have, for various reasons, been discarded.

In Table 11 are listed for each month and the year the average number of hours of sunshine at all places from which a sufficiently long record is available. The greatest amounts are recorded at places protected from the prevailing winds by high mountain ranges. The excellence of New Zealand's climate, particularly for the growth of pasture, is undoubtedly due to the abundance of sunshine combined with a high rainfall and an absence of extreme temperatures.

Tables giving monthly averages for a number of stations under each of the heads distinguished below, will be found on page 25 of the edition of the Year-Book. Most of the fogs recorded are shallow radiation fogs occurring only in the early morning. During the approach of cyclonic depressions, however, widespread and persistent fog is a frequent occurrence. Occasionally, parts of the coast are affected by fog in calm weather. The landlocked harbours and estuaries of North Auckland appear to be unusually susceptible.

In the interior and at high altitudes it occurs more frequently. On the summits of the ranges in the whole length of the South Island and on the highest peaks in the North Island snow falls, on the average, on over thirty days per annum. In the interior of the South Island there is a considerable area of settled country which is subject to half that number.

Towards the coast, however, the number falls off rapidly. Data regarding snow lying are scanty. In the North Island any snow falling on the low levels almost invariably melts as it falls, but on the high plateaux it may lie, especially in the hollows, for from one to three weeks during the year. In the South Island it practically never lies at low levels on the north or west coasts, but on the east coast does so on a few days in some years. At altitudes between ft. Railway traffic is seldom interfered with by snow, even to a minor extent. It occurs more often in spring than at other times of the year.

The latter are usually associated with thunderstorms, and are probably a little less numerous on the east coast than the west or in the North Island than in the South. They are very rare in eastern districts in winter.

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Strong Winds. These figures include a proportion of high winds force 7 on the Beaufort scale as well as gales force 8 and over.