hie INENO Vong be ve unt gn Ny vf 3 % hy ay PRS: SE Fi ty BP ee che aya ee Sue ‘ sh ; ie Sie 24 ; y +e See ae) ov ; NAW es Oy 4 +o RINSE EN 4 x p ice i 4 ty j ue) Paisley! batae see) 4 es ine y fem) f ay hia Kanes ie 1) att 7 Q 1907 LB. 62: ere 1 No. 1.1890: Zz EDITED BY 72 eS }. Woop- Mason, Fs. VICE-PRESIDENT. Se Ns “Phe pounds of its investigation will be the geographical limits of Asia: and within these limits its inquiries will be extended to whatever is performed by man or produced by nature.”’—Sirk WILLIAM JONES. #*,* Communications should be sent under cover to the Secretaries, Asiat. Soc., to whom all orders for the work are to be addressed in India; or, in Lon- don, care of Messrs. Tritbner and Co., 57 5 59, Ludgate Hill. CALCUTTA: PRINTED AT THE PAPTIST MISSION PRESS, ae AND PUBLISHED BY THE ee ASIATIC SOCIETY, 57, PARK STREET, 1890. A S— SoSOeeeSer NNN aE — om se ‘exclusive of postage) to Subscribers, Re. 1.— To Non-Subscribers, Re, 1-8 Price in England, 2 Shillings and sixpence. Issued May 17th, 1890 Be nS aes Sad | aa Shei ee ' * cant vecisional Inversion of the Bo aL ie. the Hills and Plains of Northern India. M. A., Meteorological Reporter to the Governmen. Il.—Natural History Notes from H. M. Indian Me Steamer ‘Investigator,’ Commander ALFRED CARPEN.. Naturalist to the Marine Survey, (With Pl. 1.)............000.00 00. T11.—On Clebsch’s Transformation of the Hydrokinetic Hquations.—- By Asutosn Muxnorapuyay, M. A., F. R.A. S., F.R.S. E., IV.—Note on Stokes’s Theorem and Hydrokinetic Oirculation. By Asurosn Muxnorapayay, M. A., F. R. A. S., F. R.S. E., V.—On a Curve of Aberrancy. Gee AsurosH Muxnoprapnyay, M. A., F.R. A.S., F. B.S. E., odes Bb sodas ViI—WNatural History Notes ie om H. M. ntl ete Sai vey Steamer ‘Investigator,’ Commander Atrrep Carpgnter, R. N., D. S. O., commanding —No. 15. Descriptions of seven ale eae aS ae aS D. S. O., commanding.—No. 14. Observations on the Gestation, of some Sharks and Rays.—By Aurrep Aucock, M. B., Surgeon-. tional new Indian Amphipods.— By G. M. Gites, M. B., FP. R. C. S., late Surgeon-Naturalist to the Survey, (With Pl. IL.)...... 7 = rh Sas eee (i fi ( nied ve JOURNAL OF THE ASIATIC SOCIETY OF BENGAL. = @G One Part II.—NATURAL SCIENCE, No. I.—1890. I.— On the occasional Inversion of the Temperature Relations between the Hills and Plains of Northern India.—By Joun Entor, M. A., Murn- OROLOGICAL REPORTER TO THE GOVERNMENT oF Inp1a. [Received December 2nd ;—Read December 4th, 1889.] One of the more important features of the meteorology of the month of January 1889 in Northern India was the remarkable variations of the temperature relations between the hills and plains of Northern India and more especially of Upper India. Under normal conditions of de- crease of temperature vertically the temperature at the Punjab hill _ stations snould be 15° to 20° lower than at the adjacent plain stations. The relation is sometimes reversed in the cold weather and the night temperatures are found to be several degrees higher at the hill stations than in the Punjab plains. Such variations or inversions of the or- dinary temperature relations are of occasional occurrence in all moun- tain and adjacent valley districts. They have been observed in pre- vious years in Northern India, but were larger and more prominent in Northern India in January 1889 than has been the case for many years.* The present hence appears to be a favourable period for discussing the * Similar large and prolonged inversions of temperature occurred in the years 1879, 1880, and 1881 in Upper India. 3 i 2 John Eliot—On the oceasional Inversion of the Temperature [No. 1, facts and causes of these occasional inversions of temperature in North- ern India, Before commencing with the subject proper of the paper it is de- sirable to give a summary of what is known generally of these occasional inversions of the ordinary vertical temperature relations. Ferrel states it is probable the diurnal temperature oscillations of the upper strata of the atmosphere in the open air away from the in- fluence of contact with the Earth’s surface are extremely small. The effect of the Earth’s temperature on that of the air above is not so great as it is below, so that this causes the amplitudes in the oscilla- tions of the air temperature near the Harth’s surface, though less than those of the Earth’s surface, to be greater than those of the air above. The effect of this, it is readily seen, is to cause the temperatures in winter and during the night to approximate more nearly to the tem- peratures above, and hence to diminish the rate of decrease of tempera- ture with increase of altitude at these times. But during the summer and the warmest part of the day, the effect is the reverse ; it causes the temperatures below to differ still more from the temperatures above, and hence to increase the rate of diminution of temperature with increase of altitude. In the diurnal oscillations the rate near the surface at night from the effect of nocturnal cooling is reversed for some distance above the Harth’s surface, the temperature being greater above than at the surface. As the Harth cools, the air in contact also cools when the air. is calm, until the surface and likewise the lower air strata are cooled very low and the law of decrease of temperature is reversed. It is different during the day. The increase of the temperature of the Harth’s surface, and of the lower strata in contact, brings about a state of unstable equi- librium from which at once arises a vertical interchange of air, by means of ascending and descending currents, which tend to equalize, in some mea- sure, the temperatures above and below, so that, although the Harth’s sur- face may be heated to a much higher temperature than the air immediately above, the decrease of temperature with increase of altitude never becomes very much greater than that of about 1° C. for 100 meters, corresponding to the initial state of unstable equilibrium. The effect of the heat of the Earth’s surface cannot be confined to the lower strata merely, as that of the cooling of the surface is, but, as soon as the first stratum in contact with the Harth is heated, the effect is carried to those above. Spring also refers in his meteorology to the same subject and states that the inversion of the ordinary temperature relations takes place occasionally, and usually during periods of very high pressure, and when the amount of cloud and humidity is abnormally small. The cause of the increased temperature at a higher elevation is ascribed to compression of the air. 1890.] Relations between the Hills and Plains of Northern India. 3 The following extract from an article on Climate in the Encyclo- pedia Britannica (written by A. Buchan, Esq.), I believe, fairly repre- sents the opinion of English meteorologists on this subject : —- “These results which only affect the mean daily temperature in different seasons, and which are due exclusively to differences of ab- solute height, though of the greatest possible practical importance, yet leave untouched a whole field of climatological research—a field embra- cing the mean temperature of different hours of the day at different heights, for an explanation of which we must look to the physical con- figuration of the earth’s surface and to the nature of that surface, whether rock, sand, black soil, or covered with vegetation. “Under this head by far the most important class of conditions are those which result in extraordinary modifications, amounting frequently to subversions of the law of the decrease of temperature with the height. This will perhaps be best explained by supposing an extent of country diversified by plains, valleys, hills and table-lands to be under atmos- pheric conditions favourable to rapid cooling by nocturnal radiation. Hach part being under the same meteorological conditions, it is evident that terrestrial radiation will proceed over all at the same rate, but the effects of radiation will be felt in different degrees and intensities in different places. As the air in contact with the declivities of hills and rising grounds becomes cooled by contact with the cooled surface, it ac- quires greater density and consequently flows down the slopes and ac- cumulates on the low-lying ground at their base. It follows, therefore, that places on rising ground are never exposed to the full intensity of frosts at night; and the higher they are situated relatively to the im- mediately surrounding district the less are they exposed, since their re- lative elevation provides a ready escape downwards for the cold air almost as speedily as it is produced. On the other hand, valleys sur- rounded by hills and high grounds not only retain their own cold of radiation, but also serve as reservoirs for the cold heavy air which pours down upon them from the neighbouring heights. Hence mist is fre- quently formed in low situations whilst adjoining eminences are clear. Along low-lying situations in the valleys of the Tweed and other rivers of Great Britain, laurels, araucarias, and other trees and shrubs were destroyed during the great frost of Christmas 1&60, whereas the same species growing on relatively higher grounds escaped, thus shewing by incontestible proof the great and rapid increase of temperature with height at places rising above the lower parts of the valleys. “This highly interesting subject has been admirably elacidated by the numerous meteorological stations of Switzerland. It is there ob- served in calm weather in winter, when the ground becomes colder A; John Eliot—On the occasional Inversion of the Temperature [No. 1, than the air above it, that systems of descending currents of air set in over the whole face of the country. The direction and force of these descending currents follow the irregularities of the surface and, like currents of water, they tend to converge and unite in the valleys and gorges, down which they flow like rivers in their beds. Since the place of these air-currents must be taken by others, it follows that on such occasions the temperature of the tops of mountains and high grounds is relatively high, because the counter-currents come from a great height and are therefore warmer. Swiss villages are generally built on emi- nences rising out of the sides of the mountains with ravines on both sides. They are thus admirably protected from the extremes of cold in winter, because the descending cold air-currents are diverted aside into the ravines and the counter-currents are constantly supplying warmer air from the higher regions of the atmosphere, “Though the space filled by the down-flowing current of cold air in the bottom of a valley is of greater extent than the bed of a river, it is yet only a difference of degree, the space being in all cases limited and well defined, so that in rising above it in ascending the slope the increased warmth is readily felt, and, as we have seen, in extreme frosts the destruction to trees and shrubs is seen rapidly to diminish. The gradual narrowing of a valley tends to a more rapid lowering of the temperature for the obvious reason that the valley thereby resembles a basin almost closed, being thus a receptacle for the cold air-currents which descend from all sides. The bitterly cold furious gusts of wind which are often encountered in mountainous regions during night are simply the outrush of cold air from such basins.” The most important recent contribution to the subject is a memoir on “Mountain Meteorology” by Professor William Morris Davis, Harvard College, Cambridge, U.S8S., in which he gives a summary of the facts up to date. In this he points out that examples of inversion of temperature relations are by no means rare in mountain districts in Europe and America, and that they are most common in winter. He quotes a monograph of Professor Hann’s which states that the inversion is best shewn in hill-enclosed valleys where the air stagnates and is not replaced by air from above. Such inversions, it is there pointed out, are most frequent during the passage of areas of high pressure or the prevalence of anti-cyclonic conditions. The unusual warmth in the hill regions is shewn to be an effect of the compres- sion of the descending air, whilst the cold in the valleys and low ground is due to other causes, and takes place in spite of the descent of air into it. A remarkable example in Hurope of the inversion due to the prevalence of anti-cyclonic conditions occurred in December 1879 1890.] Relations between the Hills and Plains of Northern India. 5) and was the subject of numerous investigations. Hann, in his paper on Die Temperatur Verhiiltnisse des Decembers 1879, investigated the matter very thoroughly. He made in that paper a comparison between the temperature of Klagenfurth (in the valley) and Hochober (at an elevation of 5215 ft. above Klagenfurth), and states that from December 6th to 18th it was continually warmer on the mountain than in the valley. The mean difference of the 7 a. mM. temperatures for these thirteen days was 23°4° in favour of the mountain, at 2 p. M. 21:2°, and at 9 P. m. 19°6° F. Other examples are given in the same memoir of the abnormal vertical temperature conditions which occasionally obtain in Hurope and America. Buchan, in a paper published in the Journal of the Scottish Meteorological Society, states that on the 3lst December 1883 the tem- perature at the top of Ben Nevis was 4°5° higher than at Fort William. In this case too pressure was abnormally high. Woeikoff, the Director of the Russian Meteorological Department, on the strength of certain evidence, believes there is a persistent inversion of temperature during the winter in Siberia. Inversion of temperature is also said to be of common occurrence on Mount Washington (in Massachusetts). It is also occasionally shewn by the Pikes’ Peak Observations. That moun- tain has an elevation of 14134 feet and is 8,840 feet higher than Denver. Professor Loomis gives 39 examples of higher temperature at the top of Pikes’ Peak than at Denver from four years’ observations. In the most extreme cases the differences of temperature amounted to 15° and 16°. It may be noted that these inversions all occurred during the winter. It is not necessary to quote from the earlier meteorological works of Herschel, Buchan, &c., as they only recognize the cccasional oc- currence of lower temperature at night in valleys than on the adjacent hills, and ascribe the effect chiefly to the flow of cold air down the sides of the hills. Recent meteorological writings in some cases continue to ascribe the cooling almost entirely to the descent of the air from the mountain sides into the valleys, and state that the inversion of the vertical temperature relations is of comparatively frequent occurrence in mountanous districts. The facts about to be given, however, appear to indicate the probabi- lity that these inverse relations which are exhibited by the mountain observations are due to general conditions that prevail in plains as well as in mountain districts, and hence that similar relations may obtain much more generally and widely than is usually supposed. No distinct statement, however, occurs to this effect, so far as I am aware, and the evidence of inversion of the vertical temperature relations is, in the absence of suitable balloon. observations, confined to differences be- 6 John Eliot—On the occasional Inversion of the Temperature [No. 1, tween mountain stations and the neighbouring valley or other low-lying stations. They are hence assumed to be phenomena restricted to hills and the neighbouring confined valleys and hence of limited extent. The explanation generally given, whilst making the inversion a pheno- menon of terrestrial radiation, attaches much weight to the flow of cool air down the mountain sides into the valleys, and hence suggests that it is peculiar to mountain districts. The present paper will, I believe, prove that inversion may occur over very large plain areas, and that it has, in some cases at least, little or nothing whatever to do with air motion between hills and valleys. It will also shew that the vertical temperature relations during the cold weather in Northern India are much more variable and complicated than they have been hitherto supposed to be, and that the descensional motion which accompanies cooling of the air during the night in fine clear weather is almost entirely one of slow compression, and is not the opposite of the ascensional and convective movement which takes place largely during the day, or, in Professor Ferrel’s suggestive words, “ the effect of the heating of the earth’s surface is not confined to the lower strata merely, as that of the cooling of the surface is, but as soon as the first stratum in contact with the earth is heated, the effect is carried to these above.” The principle is, I believe, of great importance generally, and more especially in India, in connection with the production of the dry winds of the Gangetic plain during the hot weather months of , March, April, and May. The paper consists of three parts ;—Ilst, a statement of the normal meteorological temperature conditions of the plain and hill districts of Upper India in the month of January and of certain meteorological conditions and actions upon which temperature mainly depends; 2nd, a statement of the more striking abnormal temperature relations of the month of January 1889 and of the cold weather period generally in Upper India; and 3rd, a discussion of the causes which produce these unusual temperature conditions and variations. It may be premised that one or two of the actual observations quoted for the month of January 1889 appear to me to be somewhat doubtful. Ihave, however, thought it best to include them, as it is on the whole more probable that they are exaggerated examples of the peculiar temperature relations about to be discussed than that they represent instrumental or observational errors. The following table gives the average maximum temperatures of the month of January of certain selected pairs of stations in Upper India, each pair consisting of a hill station and the nearest plain station at which there is an observatory :— 1890.] Relations between the Hills and Plains of Northern India. 7 3 ]2 prrrcreed co) b= Mean maximum tem- Fy Deane ae qa Be wo H | perature for January. |. ¢ 5 8|\3 98 °F Names of pairs of 28 a ogg a Fae glee stations. sins © Sel eB eso 8 Be el Hill Plan |S g°2|{%o28S Ey on station. | station. ge ae as 5 OS fas) A 5 HSB3a b oan on eueuta \ “6° 1Q0 +O -1° Jacobabad 5300 163 516 73°3 21-7 4:1 Murree os pe ms Rawalpindi } 4700 30 | 47°8 63°39 15°5 33 Simla a Ss oe i eaeevy \| 6200 | 80] 512 67-6 16-4 2-7 Chakrata ee na hess ae Pen cs \| 6200 | 58) 501 69:4 19°3 3:1 Ranikhet ws ba e Bareilly } 5500 90 540° 7071 16:1 29 Dhubri Le on a 0 Darjeeling } 7300 116 443 73°4 291 4:0 Deesa aS a mn . Tce Ain \\ 3500 | 40] 671 82-2 15:1 43 Pachmarhi a aE ron cae Hoshangabad } 2500 48 | 706 80°1 95 38 A full description of these observatories and of the more important local peculiarities of exposure will be found in Mr. Blanford’s Report on the Meteorology of India for 1885. It will suffice here to point out that both Ranikhet and Simla are situated at some distance within the first line of hills, whereas Murree and Chakrata are practically on the crest of the first line of elevations overlooking the plains. Assuming these as more typical of the relations between hills and plains, the preceding data shew that in Upper India the temperature near the hills decreases vertically with elevation at the hottest time of the day in the month of January very nearly 3° in 1000 feet up to a height of 7000 feet?at least. The remarkably low day temperature at Darjeeling during this period as shewn by the table appears to be due to the following causes, of which the first is probably the most influential. 1st.—The great humidity and large amount of fog at that station (as in the Hastern Himalayan districts generally) in January, in which respects it contrasts strikingly with the hill stations of Upper India, where the air is, except in stormy weather, very dry and clear. 2nd.—The contiguity of the immense snow mass of Kanchinjunga and neighbouring mountains, which include some of the highest peaks in the Himalayas. This area embraces an enormous ex- tent of snow covered ground, the southern edge of which (in summer) is at a distance as the crow flies of not more than 30 8 John Ehot—On the occasional Inversion of the Temperature [No. 1, or 35 miles from Darjeeling. The first line of snows is at a distance of at least 45 or 50 miles from Simla and Murree and at a distance of about 40 miles from Chakrata. The neighbouring areas of perpetual snow are of greater elevation and of con- siderably less extent in the case of all these stations than of Darjeeling and hence exercise a much smaller influence. As the meteorological conditions of Darjeeling are thus essentially different from those of the hill stations of Upper India, it will be ex- eluded from the final discussion, although data for it are given in the tables for the preliminary comparisons. The following table gives the average minimum temperature data for the same pair of stations for the month of January. F ses [oe 2a o | Mean minimum tem- 5 ga 12 ae cis oo 8 | perature for Jannary. =.8 3 |\SE oss x ih ° d q S oS a8 |+ ao rq et ames of pairs of 2.9 i oe mg |Sa eS x stations. AS Q Sow SB |o 4 8 hm fy a 4 3 Ooglh |\Pua Br é 8 Hill Plan | 8 oe [835 So a a station. station, = g Big 5 RoR acd Quetta Ge 19° «Q° po .e0 Jacebabad 5300 163 29:2 4,2°8 136 2:6 MEO \) 4700 | 30] 985:5° 379° 2-4° 05° Rawalpindi J Simla eee “4° {2°52 27° Pe i) Se \| 200 | 80) 36-4 43°5 71 eo! (GPa }| e200 | 58) 357° | 442° 85° 14° Roorkee Sat ia nee “}) 5500 | 90), 395° | 459° 64° 12° Bareilly tee eee st) 7300 | 116 | 346° | 585° 18:9° 26° Darjeeling Deesa 9° a) .9° ea ed \} 3500 | 40] 509 511 0-2 0 Pachmarhi 417-22 525° 130 7° Hoshangabad } zoe ete 7 : a This table shews that at all these stations the average difference of temperature at night is much smaller than by day. The rate of difference is greatest in the cases of Quetta and Jacobabad, Pach- marhi, and Hoshangabad, and Darjeeling and Dhubri, for which it averages about 2° or less than half of the rate of difference for the maximum temperature. The result for Deesa and Mount Abu is so anomalous as to point to peculiar local conditions, the nature of which have, however, not yet been determined.* In the case of the pairs of stations in Upper India the average rate of change of temperature with * T have recently (January 1890) visited these two stations: the temperature observations are carefully recorded, and are taken under the same conditions of ex- 1890.] Relations between the Hills and Plains of Northern India, 9 elevation at night in January varies from 0°5° for Murree and Rawal- pindi to 1°4° for Chakrata and Roorkee, and averages 1°, that is, little more than one third of the day rate of decrease of temperature vertically. These two tables may hence be summarized as follows :— (a). The rate of decrease of temperature with elevation at the time of maximum day temperature in the month of January averages 3° per 1,000 feet in the Western Himalayas and 4° per 1,000 feet in the Eastern Himalayas up to 7,000 feet and in the Aravalli and Vindhya Hills and perhaps also in Beluchistan. (b). The rate of decrease of temperature with elevation at night or at the time of minimum temperature averages 1° per 1,000 feet in the Western Himalayas, 2° per 1,000 feet in the Hastern Himalayas and Vindhyas, and 23° per 1,000 feet in Beluchistan. An interesting point in connection with the night temperature in the plains of Upper India is shewn by the data of the following table. The first column gives the average minimum temperature of the month of January at stations nearest to the hills and the second that of stations at a greater distance than those of the first column. BS Be ig ee g° Eo : : do ES Rae Sy =H Plain stations| .& 2 5 Bo a's Plain stationsnear| -= 2 . at consider- Be. Sere S altel 5 | 2 Bs hills. FE | abledistance| & € & Crane (lease ctaes a8 from hills SoS) Hic Ose ail) eS q : | OMe Onn: Sei S | a aga HBOB HY n Bc oo oo 8 Oo H B's alae Teel SP Sei seses aia. || oe a (A. (B.) A iam) Rawalpindi aa) eee Peshawar 39°1° — 12° 100 miles Sialkot Boo) eas Lahore 42°4° 0'5° UE pe Ludhiana we | 43°5° Sirsa 424° Holy 190 ,, Roorkee wee | 44°2° Meerut 44°4° — 0°2° 0). Delhi On A Bareilly von || 419° Agra 120 ges Lucknow 459° 0° 25s O Allahabad AT5° 11° 75) ar Gorakhpur p00 48 6 | Benares 4)7-9° 07° 100 ih Dhubri son || eee Berhampore 53°2° 0:3° L5Ola: The geographical relations between Rawalpindi and Peshawar are quite different from those of the other pairs of stations, which are all situated in the great plain of Northern India stretching along the foot of the Himalayas from the North Punjab to East Bengal. posure as at other stations in India. Several series of hourly observations of tem- perature during the night have been recently taken, and, as they confirm the con- clusions of the present paper, I hope to discuss them in a brief paper to be submitted to the Society shortly. 2 ~ 10 John Eliot—On the occasional Inversion of the Temperature [No. 1, The differences here are small and to some extentundoubtedly depend upon the peculiarities of position of the observatories at the observing stations. Their general uniformity, however, appears to indicate clearly that the lowest minimum temperatures in January in the great Nor- thern or Gangetic plain of India are not found at and near the foot of the hills, but in the midst of the great plain at a distance of 100 to 200 miles from the Himalayas, or, as it might be more fully expressed, the axis of minimum or lowest night temperature in Northern India in the month of January runs nearly parallel to the Himalaya mountains at a distance from their southern base varying from 100 to 200 miles. This fact seems to be of great importance as it shews that, whatever the rapid cooling in these plains may be due to, it cannot be ascribed to the cause usually assigned for the greater cold in valleys than in hill sides, viz., the sinking of air cooled by contact with the sides of the hills into the valleys. For it is not possible that the cooled air sinking down with a motion which is imperceptible to the anemometer or senses should produce the greatest effects at distance of one or two hundred miles from the foot of the hills and where the temperature is higher by day, as is shewn by the following table :— ; ; pate F £2 AS S23 ne A= o do A o © ae ae A Bay 2 eS) 3 Ble Os VS Ay =| # . | Plain stations| FE . Fou - 8 Plain stations a & | at consider- - a Pe 25) #8 | rs 3 near hills. @£8 | abledistance| ¢88 | oe8 ma 26 se A | from hills, SS Zon ag Oona . (A) @) |esbe | Be arr fo) Se ~ ra Rawalpindi Hb G3:80 Peshawar | 640° Oe 100 miles Sialkot aol 6Gnda Lahore 67°6° 09° BS S665 Ludhiana all 67-65 Sirsa 70°8° 330° TOOK a Roorkee .. | 69°4° Meerut 701° Oe GOES Delhi 710° 0:9° QO Ap Bareilly Peale Oda {Ain 734° 33° 120t ae Lucknow 73°8° 37° 125, wi) Allahabad 73:60 02 125 Gorakhpur (BF { Benares 747° 1:32 100 i Dhubri | 734° Berhampore 78°2° 4°8° 150; The following table gives mean daily temperature (7. e., means of the maximum and minimum temperatures) data of the month of January for the same pairs of stations :— 1890.] Relations between the Hills and Plains of Northern India. 11 o o Mean daily tempera- 3 a os ad ture January. g ie o.g 2 58 Pairs of stations. gS 5 TS & 2 | Hill sta- | Plain sta- BS ioe Se tion. tion. A £ oF A (A.) (B.) Bee Pe Quetta atele eee 4AN-Ae2 “Ne ato) -Q0 Cae fe } 5300 40°4 58-0 17°6 33 Murree ws a) po “9° 9° mee iad: e ; 4700 | 41°97 50°6 8-9 1:9 Simla C 5o6 ~QO° Wale) -QO “O° ae a } 6200 43:8 55:6 11:8 1-9 Chakrata sae | ¢ QO ° “ne QO Roorieoee 5a: f 6200 42°8 568 140 2°3 Ranikhet 900 aie) “no 2Q0 7° meee. i \ 5500 46-7 58-0 11°3 21 Dhubri oe 7 .po ro Prate) 690° Darjeeling i } 7300 39°5 63°5 24:0 33 Deesa 000 els “No te) ete) 19° memes e } 3500 59-0 667 77 22 Pachmarhi chs ¥ “Qo .Q0 42 “7° rea eabed s \ 2500 58-9 66°3 7-4 3:0 The data of this table are not of much importance in connection with the present discussion. They shew that the average decrease of temperature with elevation (as determined from day and night observa- tions) varies from 1:9° per 1000 feet in the North-West Himalayas to 3°3° per 1000 feet in Beluchistan and Sind, where the general climatic con- ditions at that time are apparently very similar to those of the Punjab. The following table gives the average daily range of temperature at the plain and hill stations of each pair of stations. Average daily range of temperature for Ratio of daily January. range at plain sta- Pairs of stations. ieee Hill Plain ete UL station. station. (B.) (A) (B.) (A.) Quetta ies 000 oso ° “RO “4° Jacobabad 4 228 ae : Murree Pao yO 1° Rawalpindi ... } ee oe He Simla ob wen Sha 6Q° ° 1p? Ludhiana ... — SBD | nae oa He Chakrata ... ae a +A° 92 40 Roorkee a00 500 006 } ie oe ad Ranikhet oor 005 ojete } 14, 5° 242° 17° Bareilly Darjeeling HO a2 “n° Dhubri... oe oh ou ay 20 Mount Abu eee Boo coe 16:2° 311° 1:92 Deesa 500 on6 G00 \ Pachmarhi ... ; ° ° ° eo e . 7} Hoshangabad Tere \ AP) 278 Sule 12 John Eliot-—-On the occasional Inversion of the Temperatnre (No. 1, This shews that in Upper India the average daily range of tem- perature in January is very nearly twice as great in the plains as at the adjacent hill stations at elevations of 6000 to 7000 feet. The ratio is even greater in the Hastern Himalayas, the daily range of temperature probably varying from 2} to 3 times as much in Assam and North Bengal as it is in the adjacent Himalayas at an elevation of 7000 feet. In the hills of Upper India this diminished range of temperature cannot be ascribed to any deficiency of radiating power, either of the sun or of the earth at this period of the year, for the air is much clearer (free from dust, smoke, etc.) and drier in the hills than the plains in Up- per India, and, as shewn in the following tables, solar heat is absorbed more largely by day and terrestrial heat given out more rapidly by night in the hills than in the adjacent plain districts. The only measure for the radi- ating power in either case that we at present possess is the average daily difference between the readings of the solar radiation thermometer and maximum thermometer in the one case and between the readings of the grass radiation thermometer and minimum thermometer in the other. The following two tables give these differences for the pair of stations selected. F Average difference be- tween readings of solar radiation and maximum | Ratio of differ- thermometer in shade. ence for hill January. station to that Names of pairs of stations, for plain sta- ; tion. Hill Plain stations. station. Me A B. B Quetta eee coo 2 -Q° -Q° 7° Jacobabad .,., oe ac 62°9 59°9 Ld Murree oes eae Ao “0 190 Rawalpindi ... n00 ead eee pane ve Simla eve eee 00g ie) mo «9° Ludhiana... acd toe Cai ore ae Chakrata aD BAG 190 Pot) Roorkee a nop Sad } 670 543 12 Ranikhet tee coo eee yar) Wate) +99 Bareilly, ie oe 60"7 AOU 18 Darjeeling ... tee oon 42 Jo 4° Dhubri eee coo a 96) } bt 2 sy : u : Mount Abu ... au 6 Bots 40 199 aaa a ae 622 53-4 1:2 Pachmarhi ... cots vee ee 40 ° Hoshangabad 40 } ers pos yee 1890.] Relations between the Hills and Plains of Northern India. 13 This table establishes conclusively that the average direct heating power of the sun is greater at the hill stations in January than at the corresponding plain stations. And, if it might be assumed that the re- lative intensity in the two cases is, roughly speaking, proportional to the ratios given in the preceding table, the heating power of the sun at an elevation of 7000 feet in the Himalayas is on the average about one- fifth greater than at the level of the adjacent plains, or, in consequence of the absorbing action of the lower strata, the sun is one-sixth less power- ful in heating the earth’s surface at the level of the plains than it is at that of the hill stations of the Himalayas. The following table gives similar data for nocturnal radiation from the Harth’s surface :— Average difference between grass radiation thermo- F «en meter readings and those | Batie 2 ean of minimum in shade ther-- oy... station to that Names of pairs of stations. AOA IE HOS JSUT | of corresponding | plain station Hill Plain | A. station. station, | B= A. B Quetta 56 S00 56 Ao ° Jacobabad ... Kon ase \ ne DOL 10° Murree a SO bos ° Beolendies i Gy ws Te 1:6" Simla COO oo ose 9.9° fe) Ludhiana a o00 i ee oe 1:3 Chakrata o0 Ado “mo ) Roorkee 606 Ano aes } 95 v2 13° Ranikhet tele oy aXe) ° Bareilly Sil 280 ce 16 Darjeeling a0 ° ) Dhubri i } OS OL 15° Mount Abt ... oie) ° Deesa 06 Aer Wd a1 1:9° Pachmarhi ... ane ae ° Hoshangabad ne } ey | Oe ae These figures show that nocturnal radiation goes on much more rapidly at the hill stations than at the adjacent plain stations, and that the ratios as measured by the differences given in the preceding table are much greater than the ratios in the corresponding tables for solar radia- tion. ‘Taking the average of all the stations as a rough approximation, they appear to indicate that nocturnal radiation goes on upwards of 50 per cent. more rapidly at the hill stations than at the adjacent plain stations. : 14 John Eliot—On the occasional Inversion of the Temperature [No. 1, This result is undoubtedly in part due to the greater length of the night (or period of effective terrestrial radiation) than of the day in the month of January in Northern India, and perhaps also to the greater clearness and homogeneity of the atmosphere arising from the stillness of the air and absence of wind at night as compared with the day. It will, however, be presently seen it is probable that the mean monthly minimum temperature at the hill stations represent an average of conditions different from that at the plain stations and hence the figures given above are almost certainly of little value for the comparison of nocturnal radiation in the plains and hills of Northern India. It is, however, evident that the figures as a whole support the inferences based on the known laws of radiation from cooling bodies. It is certain there- fore that in clear weather in January, if there were no other action than mere radiation and heating and cooling of the adjacent air by contact with the Harth’s surface, the Harth’s surface and adjacent air would be heated to a greater extent by day and cooled to a larger amount at night at the hill stations than at the plain stations and hence the daily range of temperature might be expected on this account alone to be consider- ably greater (probably from 10° to 20°) at the hill stations than at the plains. The following table gives the average cloud amount during the month at the selected stations. (RS SS EE Mean proportion of cloud; Ratio of cloud in January. proportion of hill station to plain Names of pairs of stations. station. Hill Plain station. station. A. A. B. B. uetta tee : : d Soe oes } ae zie es Murree oes : “A, ¢ Rawalpindi ... ooo } Be i ee Simla vee } 56 3:9 1°4 Ludhiana oe Chakrata eee r 4:8 34 14 Roorkee oo) Ranikhet eee \ Al 30 1:4 Bareilly oo Darjeeling see \ 55 7 3:2 Dhubri An ap Mount Abn ... so 26 22 12 Deesa : vee Pachmarhi ... Bao } 23 2-2 10 Jubbulpore ... is 1890.] Relations between the Hills and Plains of Northern India. | 15 The following table gives the average humidity of the month of January at the same pairs of stations. Mean relative humidity | Ratio of average in January. humidity of hill station to that of Names of pairs of stations. plain station. Hill Plain station. station. A. A. B. B. Quetta a0 } : Jacobabad O00 OY ee 14 Murree o E Rawalpindi ... Ban } 59 73 08 Simla a p Ludhiana su } Or 68 09 Chakrata abd } 63 65 1-0 Roorkee G00 Ranikhet sere ; Bareilly ie 63 oh ve) Darjeeling ae } a ; Dhubri... a g du 1D Mount Abu ... aH } 40 38 1-0 Deesa 900 see Pachmarhi ... see : Jubbulpore ... ad } oe 60 Ve These tables show that while the amount of cloud is considerably greater at the hill-stations that at the plain stations in Upper India, the air is actually on the average drier or less humid in the former case. As these results are based on day observations chiefly, it is probable if night observations of equal weight were included the difference would be even more marked. The following is a brief general summary of the mean temperature conditions at the level of the hill stations in the Himalayas and on the adjacent plains. (1.) The rate of decrease with elevation of the average daily tem- perature of the month of January is very approximately 24° per 1,000 feet or more exactly 1° per 470 feet. The rate of decrease is, however, very irre- gular, varying not only from day to day but also from hour to hour during the day. The rate of decrease of the average minimum or night temperature with elevation in Upper India is only about 11° per 1,000 feet and of the average maximum temperature is 3° per 1,000 feet. (2.) The daily range of temperature is much less at the hill stations than in the adjacent plain districts and is little more than half that at the adjacent plain stations. Tt also follows from the previous remarks that any explanation of the | 1 | | 16. John Eliot— On the occasional Inversion of the Temperature [No. 1, smaller average difference of the minimum temperature at the hills and at the adjacent plain stations (or of the small night vertical range of temperature compared with the day) must recognize :— (a.) That the airis on the average less humid at the hills than at the adjacent plain stations in Upper India. (b.) That there is on the average more cloud at the hill stations. (c.) That the intensity of solar radiation is considerably greater at the hill stations, probably at least 20 per cent. greater. (d.) And that the intensity of radiation from the earth’s surface at night is very considerably greater at the hills than the adjacent plains. We now proceed to give data for the same pairs of stations for January 1889. The following tables give the comparative temperature data of eight hill stations in Northern India and of the eight nearest plain stations at which there are observations for that month. The first table gives the maximum temperature of each day of the month of January 1889 and the variation from the normal. The variations are obtained from the daily means of the past eleven years (1878-88) smoothed so as to give a fairly regular series. The positive sign affixed to a number in this table indicates that the actual tempera- ture was above the normal and a minus sign that it was below it. The second table gives similar date for the minimum temperature of the same 16 stations for the same period. The third table gives the daily difference of the maximum tempera- tures for each of eight pairs of stations consisting of a hill station and adjacent plain station. Iu every case the maximum temperature at the plain stations exceeds that at the neighbouring hill station. The fourth table gives the difference between the minimum tem- perature registered at each of the eight selected hill stations and the neighbouring plain stations. In the majority of cases the minimum temperatures at the plain stations exceed those at the plain stations in which case no sign is prefixed to the number. 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