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temperature and greatest dryness combined. The regions of largest amplitude include the East India Islands, Eastern Peninsula, India, Arabia, tropical Africa, and tropical South and Central America, where it either closely approaches or exceeds 0·100 inch. At Silchar, in Assam, it is 0-133 inch. In the tropical parts of the ocean the oscillation is from 0-020 to 0-030 inch less than on land. The influence of the Mediterranean Sea in lessening, the amount over all regions bordering it is very strongly marked. The line showing an oscillation of 0.050 inch crosses North America about lat. 44°, curves southward at some distance from the east coast to lat. 23°, then north-eastward along the coast of Africa, passes eastwards near the north coast of that continent, thence strikes northwards, cutting the eastern part of the Black Sea, and eastward across the Caspian to a point to northward of Peking, and then bends southward to the Loo Choo Islands. The line of 0.020 inch cuts the N.W. of Spain and N.W. of France, and runs northward through Great Britain as far as the Tweed, thence to Christiania, then southwards to Copenhagen and to Cracow, the latitude of which it follows eastward through Asia.

The more marked seasonal changes are these:-In India the oscillations during the dry and wet seasons, or in January and July, respectively, are-Bombay, 0·120 and 0-067 inch; Poonah, 0·133 and G-059 inch; and Calcutta, 0-132 and 0-091 inch. At Madras, where the rain-bringing characters of the monsoons are reversed, the numbers are 0114 and 0-115 inch, and at Roorkee, where rain falls all the year round, 0.088 and 0.079. Again, at Aden, in Arabia, where the weather of July is peculiarly hot and dry, the oscillation in December is 0-106, but in July it rises to 0-137 inch The point to be insisted on here is, that, whatever be the cause or causes to which the daily barometric oscillation is due, the absolute amount is largely dependent on comparatively local influences.

While illustrations similar to the above may be adduced from many other parts of the globe, showing the influence in the same direction of prevailing dry or wet, hot or cold seasons on the amplitude of the oscillation, the North Atlantic and regions adjoining present an apparent exception to the law which seems to be indicated by these results. The whole of the North Atlantic, particularly north of lat. 20°; and the sea-boards which bound it, to which the Mediterranean and its immediate sea-board may be added, are strikingly characterised by a small summer cscillation; and this diminution is most strongly marked along the eastern part of the ocean. Thus, in July, at Ponta Delgada, in the Azores, the oscillation is only 0.06 inch; at Angra do Heroisma, also in the Azores, 0010 inch; at Funchal, Madeira, 0·011 inch; at Oporto, 0·018; Lisbon, 0-030; and Lagos, 0·021; at Naples and Palermo, 0·008; and at Malta, 0·020 inch. Now, with reference to this extensive region, it is to be noted that the rainfall of July is either zero or very small; and yet with this dry state of the atmosphere and high temperature (the annual maximum occurring at the time), this oscillation is extraordinarily diminished, being exactly the reverse of what takes place during the dry and wet scasons in India. The diminution on the western half of the Atlantic, though not so great, is also striking, the January and July oscillations being 0-056 and 0.036 inch in Barbadoes, 0.080 and 0-056 at Jamaica, 0.082 and 0.054 at Havanna, 0053 and 0·024 in the Bahamas, and 0.054 and 0·022 in Bermuda. Over the whole of the region here indicated the rainfall of July is largely in excess of that of January. The apparently exceptional character of this region is probably due to the circumstance, that at this time of the year the sun's rays fall perpendicularly over a more diversified surface of the earth, that is, on a greater extent of laud, than at any other season. At this time the Mediterranean,

| which is completely shut in by land, and the Atlantic, which is bounded by two great continents, show a much smaller oscillation than prevails over the land adjoining them, and the lines of equal oscillation now attain their annual maximum. On the other hand, in January, when the sun's rays fall perpendicularly over the most uniform surface, or over the maximum extent of ocean, the lines are almost everywhere parallel with the parallels of latitude. Again, on advancing inland from the Atlantic, the effects of comparatively local influences are very striking, as the following mean July oscillations, from places situated in lines running in different directions, show :Dublin, 0·012; Oxford, 0.022;' Ostend, 0·009; Brussels, 0.019; Vienna, 0.049; Odessa, 0·024; and Tiflis, 0·077: Limerick, 0·010; Helston, 0·007; Paris, 0·020; Geneva, 0·045; Turin, 0·052; Rome, 0·036; Palermo, 0·008; and Malta, 0·020. But the most remarkable illustration is the following, the places being all situated between 38° and 42° N. lat. San Francisco, 0.068; Fort Churchhill, 0.091; Washington, 0.063; Angra do Heroisma, 0·006; Lisbon, 0-030; Campo Maior, 0-054; Palermo, 0·008; Tiflis, 0.077; and Peking, 0.060.

It follows from what has been stated that much which has been written regarding these fluctuations, and in explanation of them, does not rest on facts; and nearly everything yet requires to be done in the way of collecting data towards the representation and explanation of the daily oscillations of atmospheric pressure which are, as regards two-thirds of the globe, perhaps, as already stated, the most regular of recurring phenomena, and an explanation of which cannot but throw much light on many of the more important and difficult problems of the atmosphere. The data chiefly required are-barometric data from which the amplitude of the four daily oscillations can be represented in their distribution and times, of occurrence for each of the months; temperature data, comparable inter se, from which the diurnal march of tempera ture for each month can be ascertained; hygrometric data for hourly values; rain data also for the hours; wind observations conducted on a satisfactory and uniform plan; together with magnetic and electrical obscrvations. It is singularly unfortunate that the disposition of meteorologists of recent years has been to recommend as hours of observations for places which observe only twice or thrice daily, hours which do not correspond with the times when the great barometric and thermometric daily phases occur; hence these phases cannot be noted except at the great observatories, which are too few and far apart to give sufficient data for the proper discussion of many of those questions.

Since the two maxima of daily pressure occur when the temperature is about the mean of the day, and the two minima when it is at its highest and lowest respectively, there is thus suggested a connection between the daily barometric oscillations and the daily march of temperature; and similarly a connection with the daily march of the amount of vapour and humidity of the air. Tho view entertained by many of the causes of the daily oscillations may be thus stated:-The forenoon maximum is conceived to be due to the rapidly increasing temperature, and the rapid evaporation owing to the great dryness of the air at this time of the day, and to the increased elasticity of the lowermost stratum of air which results therefrom, until a steady ascending current has set in. As the day advances, the vapour becomes more equally diffused upwards through the air, an ascending current, more or less strong and steady, is set in motion, a diminution of elasticity follows, and the pressure falls to the afternoon minimum. From this point the temperature declines, a system of descending currents set in, and the air of the lowermost stratum

approaches more nearly the point of saturation, and from the increased elasticity, the pressure rises to the evening maximum. As the deposition of dew proceeds, and the fall of temperature and consequent downward movement of the air are arrested, the elasticity is again diminished, and pressure falls to the morning minimum. Since the view propounded some years ago, that if the elastic force of vapour be subtracted from the whole pressure, what remains will show only one daily maximum and minimum, has not been confirmed by observation, it follows that the above explanation is quite insufficient to account for the phenomena; indeed, the view can be regarded in no other light than simply as a tentative hypothesis.

and the other gases and substances which are found in the air, will be afterwards adverted to.

Besides these three constituents of air, there is a fourth, viz., the vapour of water, from which no air, even at the lowest temperatures yet observed, is wholly free, so that absolutely dry air does not exist in the free atmosphere. The dry air of the atmosphere-oxygen (inclusive of ozone), nitrogen, and carbonic acid-is always a gas, and its quantity is constant from year to year; but the vapour of water does not always remain in the gaseous state, and the quantity present in the atmosphere is, by the processes of evaporation and condensation, varying every instant. Water evaporates at all temperatures, even the lowest, and rises into the air in the form of an invisible elastic gas called aqueous vapour. The elasticity of vapour varies with the temperature. At 0° Fahr. it is capable of sustaining a pressure equal to 0.044 inch of the mercurial barometer, as calculated from Regnault's experiments; at 32° (freezing), 0·181 inch; at 60°, 0.518 inch; at 80°, 1023 inch; and at 100°, 1918 inch, being nearly the average pressure of the atmosphere.

Singularly enough, Lamont and Broun, a few years ago, were led, independently of each other, to form an opinion that the daily barometric oscillations were due to the magneto-electric influence of the sun. It admits of no doubt, looking at the facts of the case so far as they have been disclosed, that the daily barometric oscillations originate with the sun, and that more than the sun's influence as exerted on the diurnal march of the temperature and humidity of the atmosphere is concerned in In investigating the hygrometry of the atmosphere, the bringing them about. But from the facts adduced, it is chief points to be ascertained are- -(1), the temperature of equally certain that, be the originating cause what it may, the air; (2), the dew-point; (3), the elastic force of vapour, its effects are enormously modified by the distribution of or the amount of barometric pressure due to the vapour land and water over the globe, by the wind, and by the present; (4), the quantity of vapour in, say, a cubic foot of absolute and relative humidity of the atmosphere. The air; (5), the additional vapour required to saturate a cubic smallness of the amount of the summer oscillation from the foot of air; (6), the relative humidity; and (7), the weight forenoon maximum to the afternoon minimum over the of a cubic foot of air at the pressure at the time of obserNorth Atlantic as far south as lat. 30°, and its diminished vation. The vapour of the atmosphere is observed by means amount, as far south at least as the equator, will no doubt of the hygrometer (see HYGROMETER), of which it is only play an important part in the unravelling of this difficulty. necessary here to refer to Regnault's as the most exact, and One of the most important steps that could be taken August's as the most convenient, and, consequently, the would be an extensive series of observations from such one in most general use. August's hygrometer consists of a countries as India, which offers such splendid contrasts of dry and a wet bulb, with which are observed the temperaclimate at all seasons, has a surface covered at one place ture of the air and the temperature of evaporation. Of with the richest vegetation, and at others with vast stretches these two observed data, the formula of reduction, as of sandy deserts, and presents extensive plateaus and deduced from Apjohn's investigations, is as follows :-Let sharp ascending peaks-all which conditions are indis- F be the elastic force of saturated vapour at the dew-point, pensable in collecting the data required for the solution off the elastic force at the temperature of evaporation, d the this vital problem of atmospheric physics. difference between the dry and wet bulb, and ỏ the barometric pressure, then

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The ancients thought that air was one of the four elements from which all things originated, and this doctrine continued to prevail till 1774, when Priestley discovered oxygen gas, and showed it to be a constituent part of air. Nitrogen, the other constituent of air, first called azote, was discovered when the reading of the wet bulb is above 32°; and soon after, and the marked differences between these two gases could not fail to strike the most careless observer. It is 'remarkable that Scheele independently discovered both oxygen and nitrogen, and was the first to enunciate the opinion that air consists essentially of a mixture of these two gases. From experiments made by him to ascertain their relative volumes he concluded that the proportions are 27 volumes of oxygen and 73 volumes of nitrogen. It was left to Cavendish to show from 500 analyses that the relative proportions were practically constant, and that the proportion is 20-833 per cent. of oxygen. The results obtained by Cavendish, though not attended to for many years after they were published, have been shown by recent and more refined analyses to be wonderfully exact. The most recent analyses of specimens of air collected under circumstances which ensure that it is of average purity, give as a mean result the following:

Volume.

when below it. From Regnault's values of the elastic force of vapour, f is found, and d and b being observed, F is calculated. From F the dew-point is found. In calculating relative humidity, saturation is usually assumed to be 100, perfectly dry air 0. The humidity is found by dividing the elastic force at the dew-point by the elastic force at the temperature of the air, and multiplying the quotient by 100.

The elastic force may be regarded as representing approximately the absolute quantity of vapour suspended in the air. It may be termed the absolute humidity of the atmosphere. Since the chief disturbing influences at work in the atmosphere are the forces called into play by its aqueous vapour, a knowledge of the geographical distribution of this constituent through the months of the year is of the utmost possible importance. Hence every effort ought to be made to place the observation of the hygrometry of the air, and the reduction of the observed data, on a sounder basis than has yet been done. As regards geogra phical distribution, the elastic force is greatest within the The circumstances under which these oroportions vary, tropics, and diminishes towards the poles it is greater over

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the ocean, and decreases on advancing inland; greater in | local irregularities in the distribution or temperature in summer than in winter; and greater at midday than in the the atmosphere. The local expansion of the atmosphere by morning. It diminishes with the height generally; but in heat during the day is greatest over land, where the air is particular cases, different strata are superimposed on each clear, dry, and comparatively calm, and least over the other, differing widely as regards dryness and humidity, ocean, where the sky is clouded, and the air loaded with and the transitions from the one to the other are often moisture. On the other hand, the local contraction by sharp and sudden. cold during night is greatest over land, where the air is clear, dry, and calm, or nearly so, and least over the ocean, where the air is clouded, and loaded with moisture. As familiar illustrations of atmospheric movements resulting from local expansions by heat and contractions by cold, we may refer to the land and sea breezes, and what depend upon exactly the same principle, the dry and rainy monsoons in different parts of the globe. But the illustra tion of the principle on the broadest scale is the system of atmospheric circulation known as the equatorial and polar currents of the atmosphere, which originate in the unequal heating by the sun of the equatorial, temperate, and polar regions.

The relative humidity of the air may be regarded as the degree of approach to saturation. It is greatest near the surface of the earth during night, when the temperature, being at or near the daily minimum, approaches the dewpoint; it is also great in the morning, when the sun's rays have evaporated the dew, and the vapour is as yet only diffused a little way upwards; and it is least during the greatest heat of the day.

Between the humidity, both absolute and relative, of the air and the temperature there is a vital and all-important connection. Observation shows that when the quantity of vapour in the air is great, and also when the relative humidity is high, temperature falls little during the night, even though the sky be perfectly clear; but when the quantity of vapour is small, or the relative humidity is low, temperature rapidly falls. On the other hand, during the day the temperature rises slowly, when the quantity of vapour is great, or relative humidity high, even though the sky be clear, but when the quantity of vapour is small, and humidity low, temperature rapidly rises. These facts are explained by the circumstance that perfectly dry air is diathermanous, that is, it allows radiant heat to pass through it without being sensibly warmed thereby. Add vapour to this air, and its diathermancy is diminished. The diathermancy is also reduced if the temperature approach nearer to the dew-point; in other words, if the relative humidity be increased. Hence, with an increase of vapour or with increased humidity, the effects of both solar and terrestrial radiation are much less felt on the surface of the earth-the vapour screen performing, in truth, one of the most important conservative functions of the atmosphere.

Since ascending currents fall in temperature as they ascend, through diminished pressure and consequent dilatation, they increase their relative humidity; and since descending currents increase in temperature, and consequently reduce their relative humidity, it follows that, over a region from which ascending currents rise, solar and terrestrial radiation is very considerably obstructed, but over a region upon which currents descend, radiation is much less obstructed. Most of our exceptionally hot summer and cold winter weather is to be explained in this way, on which occasions there is generally observed a high barometric pressure overspreading a comparatively limited region, on which a slow downward movement of the air proceeds.

Of the solar heat which reaches the surface of the globe, that part which falls on the land may be regarded as wholly absorbed by the thin superficial layer exposed to the heating rays; and since there is no mobility in the particles of the land, the heat can be communicated downwards only by conduction. On the other hand, the solar heat which falls on water is not, as in the case of land, arrested at the surface, but penetrates to a considerable depth, the heating effect being in the case of clear water appreciably felt at a depth of from 500 to 600 feet. Since the heat daily received by the ocean from the sun is diffused downwards through a very considerable depth, the surface of the ocean on which the atmosphere rests is much less heated during the day than is the surface of the land. Similarly it is also less cooled during the night by terrestrial radiation.

This points to a chief acting force on which the great movements of the atmosphere depend, viz., simultaneous

The other principal motive force in atmospheric circulation depends on the aqueous vapour. The many ways in which this element acts as a motive force will be seen when it is considered that a large quantity of sensible heat disappears in the process of evaporation, and reappears in the process of condensation of the vapour into rain or cloud; that saturated air is specifically lighter than dry air; and that the absolute and relative amount of the vapour powerfully influences both solar and terrestrial radiation. The question to be carefully considered here is, how in these ways the vapour produces local irregularities in the distribution of atmospheric pressure, thus giving rise to aerial movements which set in to restore the equilibrium that has thus been disturbed.

It is from these local irregularities-using the word local in a very wide sense-in the distribution of atmos pheric pressure, whether the irregularities originate in the temperature or aqueous vapour, that all winds, from the lightest breeze to the most destructive hurricane, take their rise; for, as already stated, wind is merely the flowing away of the air from where there is a surplus of it to where there is a deficiency.

In examining weather charts embracing a considerable portion of the earth's surface, such, for instance, as those published in the Journal of the Scottish Meteorological Society, vol. ii. p. 198, which include a large part of the northern hemisphere, there are seen two different systems of pressure changing their forms and positions on the globe from day to day-one set being systems of low pressure marked off by concentric isobarics enclosing pressures successively lower as the central space is approached, and the other set being systems of high pressure marked off by roughly concentric isobarics bounding pressures successively higher towards their centres. These two systems are essentially distinct from each other, and without some knowledge of them the circulation of the atmosphere cannot be understood.

1. Areas of Low Pressure, or Cyclones.-The annexed woodcut, fig. 1, is a good representation of a cyclone which passed over north-western Europe on the morning of 2d November 1863. The pressure in the central space is 28.9 inches, from which it rises successively, as shown by the isobarics, to 291, 29-3, 29-5, 29-7, and 29.9 inches. The arrows show the direction and force of the wind, the force rising with the number of feathers on the arrows. The two chief points' to be noted are the following:-(1.) The direction of the arrows shows a vorticose motion of the air inwards upon the space of lowest pressure, the motion being contrary to that of the hands of a watch. will be observed that the winds blow in conformity with what is known as Buys-Ballot's "Law of the Winds," already

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referred to, but which may be otherwise thus put:-Stand | overspread the greater part of Europe at that time. Here

with your back to the wind, and the lowest barometer, or centre of depression, will be to your left in the northern hemisphere (in the southern hemisphere to the right); this rule holds universally. (2.) The force of the wind is proportional to the barometric gradient, or the quotient of the distance between two places stated in miles by the difference of pressure stated in inches of mercury as observed at the two places. Hence, in the Channel, where the isobarics are close 29-5 together, winds are high, but in the north of Scotland, where the isobarics are far apart, winds are light. This rule also holds uniFIG. 1.—Weather chart, showing cyclone. versally, though the exact relation requires still to be worked out by observation. As regards the important climatic elements of temperature and moisture, the air in the S.S.E. half of the cyclone is mild and humid, and much rain falls; but in the other half it is cold and dry, and little rain falls. A succession of low pressures passing eastward, in a course lying to northwards of Great Britain, is the characteristic of an open winter in Great Britain; on the other hand, if the cyclones follow a course lying to the southward, the winters are severe. This is a chief point of climatic importance connected with the propagation eastward of these cyclonic areas.

2. Areas of High Pressures, or Anticyclones-The accom

Fia. 2.-Weather chart, showing anticyclone.

panying weather chart, fig. 2, for 2-4th August 1868, represents an anticylone or region of high pressure, which

the highest pressure is in the centre of the system, and, as usually happens, the isobarics are less symmetrical than those near the centre of a cyclone. The winds, as usual in anticyclones, are light; this, however, is the essential point of difference-the winds do not flow inwards upon the centre, but outwards from the region of high pressure; and it will be observed that in many cases they cut the isobarics at nearly right angles. Another important point of difference is in the air over the region covered by the anticyclone being, particularly in its central portion, very dry, and either clear or nearly free from clouds.

Climatically, the significance of the anticyclone consists in the space covered for the time by it being, on account of its dryness and clearness, more fully under the influence of both solar and terrestrial radiation; and consequently in winter it is accompanied with great cold, and in summer with great heat. As shown by Buchan, in reviewing the weather of north-western Europe for 1868,1 the intense heat which prevailed in Great Britain during 2-4th August of that year was due to the high barometric pressure accompanying this anticyclone, the comparative calmness of the atmosphere, the clearness of the sky, the dryness of the air, and the strong insolation which took place under these circumstances.

Thus, then, the tendency of the winds on the surface of the earth is to blow round and in upon the space where pressures are low and out of the space where pressures are high. Now, since vast volumes of air are in this way poured into the space where pressure is low, without increasing that pressure, and, on the other hand, vast volumes flow out of the space where pressure is high, without diminishing that pressure, it necessarily follows that the air poured in is not allowed to accumulate over this space, but must escape into other regions; and also that the air which flows out from the anticyclonic region must have its place supplied by fresh accessions from above. In other words, the central space of the cyclone is occupied by a vast ascending current, which after rising to a con siderable height flows away as upper currents into sur rounding regions; and the central space of the anticyclone is filled by a slowly descending current, which is fed from upper currents, blowing towards it from neighbouring regions. When the area of observation is made sufficiently wide, cyclones are seen to have one, or sometimes more, anticyclones in proximity to them, the better marked anticyclones having two, and sometimes more, cyclones in their vicinity. In fig. 2, a part of a cyclone in Iceland is seen, and another cyclone in the Crimea accompanied the anticyclone there figured. Hence the cyclone and the anticyclone are properly to be regarded as counterparts, belonging to one and the same great atmospheric disturb

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ance.

From this it follows that observations of the winds cannot be conducted, and the results discussed, on the supposition that the general movement of the winds felt on the earth's surface is horizontal, it being evident that the circulation of the atmosphere is effected largely through systems of ascending and descending currents. The only satisfactory way of discussing the winds, viewed especially in their climatic relations, is that recently proposed by Köppen of St Petersburg, and applied by him with very fruitful results in investigating the weather of that place during 1872 and 1873. In attempting an explanation of these phenomena, we are met with several as yet insuper able obstacles-(1.) An imperfect knowledge of the mode

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of formation and propagation of low-pressure systems; (2.) | owing to the law of diffusion obtaining among elastic fluids Imperfect knowledge of the relations of the formation of mixed together. While the proportion of these gases is in cloud and aqueous precipitation to barometric fluctuations; a general sense constant, there are, however, consistent (3.) A want of information with reference to the merely differences in the amounts of oxygen and nitrogen in the mechanical effects of ascending, descending, and horizontal air of unwholesome places, as first shown by Regnault. currents of air or the barometric pressure; in other words, The following figures, showing the volume per cent. of we do not know how far the barometric pressure is an oxygen, rest on the authority of Dr Angus Smith, who has indication of the mass of air in the column vertically over given much attention to this subject :-Sea-shore of Scotit, when that column is traversed by air-currents; (4.) land and Atlantic (lat. 43° 5' N., long. 17° 12′ W.), 20.99; An almost total absence of really good wind observations; tops of Scottish hills, 20.98; in sitting-room feeling close and (5.) Deficient information in nearly everything that but not excessively so, 20.89; backs of houses and closets, respects aqueous vapour-its relation to radiant heat, 20.70; under shafts in metalliferous mines, 20-424; when both solar and terrestrial; its mode of diffusion vertically candles go out, 18.50; when it is very difficult to remain in and horizontally in the free atmosphere, especially from an the air many minutes, 17-20. The variations in the amounts evaporating surface; the influence which its condensation of carbonic acid in different situations are great; thus-in into cloud and rain exerts on aerial currents,-in regard to the London parks it is 0301; on the Thames, 0343; where all which more satisfactory methods of observing this vital fields begin, 0369; in London streets in summer, '0380; element, and discussing the results of observation, are during fogs in Manchester, 0679; in workshops it rises to greatly to be desired. There are here large important 3000, and in the worst parts of theatres to 3200; and fields of inquiry awaiting experimental and observational the largest amount, found in Cornwall mines, is 2.5000. physicists. Great differences have been observed by Dr A. Smith between country rain and town rain: country rain is neutral; town rain, on the other hand, is acid, and corrodes metals and even stones and bricks, destroying morter rapidly, and readily spoiling many colours. Much information has been obtained regarding impurities in the air of towns and other places by examining the rain collected in different places. The air freest from impurities is that collected at the sea-coast and at considerable heights. Again, ammonia is found to diminish, while nitric acid increases, in ascending to, at least, habitable heights. As regards organic matter in the air, it corresponds to a con siderable extent with the density of the population. As might have been supposed from the higher temperature, more nitric acid is contained in rain collected on the Continent than in the British Islands. This inquiry, which is only yet in its infancy, will doubtless continue to be vigorously prosecuted, particularly since we may hopo thereby to arrive at the means of authoritatively defining the safe limits of the density of population, and the extent to which manufactures may be carried on within a given area. The influence of atmospheric impurities on the public health has received a good deal of attention.

The law of the dilatation of gases, known as the "Law of Boyle" or "Law of Mariotte," is this: The volume occupied by a gas is in inverse ratio to the pressure under which it exists, if the temperature remains the same; or the density of a gas is proportioned to its pressure. Consequently, air under a pressure equal to that of two atmospheres will occupy only half the volume it occupied under the pressure of one atmosphere; under the pressure of three atmospheres, onethird of that volume, &c. By doubling the pressure we double the elasticity. If, however, the temperature be increased, and the air occupy the same space, the pressure will be increased; but if the pressure is to remain the same, the air must occupy a larger space. From Regnault's experiments, it is concluded that the co-efficient which denotes increase of elasticity for 1° Fahr. of air whose volume is constant equals 002036; and that the coefficient which denotes increase of volume for 1° Fahr. of air whose elasticity is constant equals 002039.

Those portions of the atmosphere in contact with the earth are pressed upon by all the air above them. The air at the top of a mountain is pressed upon by all the air above it, while all the portion below it, or lying between the top of the mountain and the surface of the sea, exerts no pressure whatever upon it. Thus the pressure of the atmosphere constantly diminishes with the height. If, then, the pressure of the atmosphere at two heights be observed, and if at the same time the mean temperature and humidity of the whole stratum of air lying between the two levels were known, the difference in height between the two places could be calculated. For the development of this principle, see BAROMETRIO MEASUREMENTS OF HEIGHTS.

The air thus diminishing in density as we ascend, if it consists of ultimate atoms, as is no doubt the case, it follows that the limit of the atmosphere will be reached at the height where the force of gravity downwards upon a single particle is equal to the resisting force arising from the repulsive force of the particles. It was long supposed, from the results of observations on the refraction of light, that the height of the atmosphere did not exceed 45 miles; but from the observations of luminous meteors, whose true character as cosmical bodies was established a few years ago, it is inferred that the height of the atmosphere is at least 120 miles, and that, in an extremely attenuated form, it may even reach 200 miles.

Though there are considerable differences in the specific gravities of the four constituent gases of the atmosphere, viz., oxygen, nitrogen, carbonic acid gas, and aqueous vapour, there is yet no tendency to separation among them,

The relation of weather to mortality is a very important inquiry, and though a good deal has been known regarding the question for some time, yet it has only recently been systematically inquired into by Dr Arthur Mitchell and Mr Buchan, the results of the investigation which deals with the mortality of London being published in tho Journal of the Scottish Meteorological Society (New Series, Nos. 43 to 46). Considering the weather of the year as made up of several distinct climates differing from each other according to temperature and moisture and their relations to each other, it may be divided into six distinct climates, characterised respectively by cold, cold with dryness, dryness with heat, heat, heat with moisture, and cold with moisture. Each of these six periods has a peculiar influence in increasing or diminishing the mortality, and each has its own group of diseases which rise to the maximum, or fall to the minimum mortality, or are subject to a rapid increase or a rapid decrease. The mortality from all causes and at all ages shows a large excess above the average from the middle of November to the middle of April, from which it falls to the minimum in the end of May; it then slowly rises, and on the third week of July suddenly shoots up almost as high as the winter maximum of the year, at which it remains till the second week of August, falling thence as rapidly as it rose to a secondary minimum in October. Regarding the summer excess, which is so abrupt in its rise and fall, it is almost altogether

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