bluuebunny/crossref_metadata_2025_split huggingface dataset:
ChemInform Abstract: The Aza‐Payne Rearrangement: A Synthetically Valuable Equilibration
Authors: IBUKA T. 
Published: July 2010

AbstractChemInform is a weekly Abstracting Service, delivering concise information at a glance that was extracted from about 100 leading journals. To access a ChemInform Abstract of an article which was published elsewhere, please select a “Full Text” option. The original article is trackable via the “References” option.
ChemInform Abstract: Carbocycles from Carbohydrates via Free Radical Cyclizations: New Synthetic Approaches to Glycomimetics
Authors: MARTINEZ‐GRAU A. , MARCO‐CONTELLES J. 
Published: July 2010

AbstractChemInform is a weekly Abstracting Service, delivering concise information at a glance that was extracted from about 100 leading journals. To access a ChemInform Abstract of an article which was published elsewhere, please select a “Full Text” option. The original article is trackable via the “References” option.
The single‐layer problem in the atmosphere and the height‐integral of pressure
Authors: Richardson Lewis F. , Munday Russell E. 
Published: July 2010

Abstract(1) The conditions under which the atmosphere could be treated as a single dynamical layer are investigated theoretically.(2) We have found nothing in the observations to justify the hope that the atmosphere could be treated as a single dynamical layer. Some possibilities, however, remain unexplored.(3) Pi, the height‐integral of pressure, has been computed from the published records of registering balloons. The termini1 of the integral have been 500 metres above mean sea‐level, and a height so great that the air above it is negligible.(4) The value of Pi, found from the mean distribution, is 7.1 × 1011 dyne cm.−1 at the equator, and 6.9 × 1011 in latitude 50° N.(5) When balloon ascents are taken individually, Pi at European stations ranges from 6.5 to 7.2 bar km.(6) When many ascents are considered at one place, the variations of Pi are correlated with those of pi. For the winter season the points on the (pi, Pi) diagram lie near lines having the slope dPi/dpi=12.4 km. for Lindenberg (long. 14° 7′ E, lat. 52° 13′ N), and 8.1 km. for Pyrton Hill (long. 1° 6′ W, lat. 51° 42′ N). For other seasons the scatter is large.The name “temporal dynamic height” has been given to dPi/dPi found from many times at one place.(7) When two places are compared at one time the ratio of the difference of Pi to that of pi has been called the “ spatial dynamic height,” and denoted by J. The median value of J is found to be 9.90 km.; but J varies from −50 km. to + 80 km.(8) Because these two dynamic heights are so unequal and inconstant it follows that Laplace's equations for free tidal oscillations in an ocean of uniform depth are a very bad description of ordinary disturbances of the European atmosphere. We have not examined the question whether the same equations, modified by additional terms to represent the gravitational field of the sun and moon, are a good description of small special forced tidal oscillations of the atmosphere.(9) In particular we need no longer be puzzled by that conflict between tidal theory and observation which provoked this research, namely, that when the free tidal equations are applied to an atmosphere above a horizontal earth they imply that the surface pressure pG is rising wherever pG, increases towards the east.2 This refers to the tidal equations in their usual form, in which terms of the second degree in the velocities are neglected. Dr. Jeffreys has shown that the second‐degree terms may have important effects.3.(10) The variations of J have been explored in a number of ways, but no simple connections have been found.(11) Equations sufficient to predict the changes of pressure, density and momenta are formulated in š 5 for a dry atmosphere moving adiabatically. But these equations cannot be summarized for a “single layer.”.
The rate of ascent of pilot balloons at melbourne
Authors: Kidson E. , Treloar H. M. 
Published: July 2010

Abstract1. The wind regime at Melbourne is described, the prevalence of North‐westerly winds at all levels being emphasised.2. The mean rate of ascent is shown to be above that given by J. S. Dines's formula near the surface but below it above 200 metres.3. There is an annual variation in the mean rate of ascent, which is highest in summer and lowest in winter.4. The rate of ascent, as has been found at other places, is very variable, the departures from normal being sufficiently' serious to render the single theodolite method insufficiently accurate for at least some practical purposes. The standard deviation of the height after various intervals from the commencement is given and the distribution of the departures shown.5. There is evidence that heat turbulence is more effective in increasing the rate of ascent near the surface than the turbulence produced by high winds. This the authors believe to be due to its being on a smaller scale.6. By far the most important factor causing variations in the rate of ascent is turbulence. The greater the turbulence, the greater the mean rate of ascent. It is believed, however, that with the same amount of turbulence the rate of ascent would be appreciably less in stable than in unstable air.7. The diurnal variation in the rate of ascent and the variation with different types of weather are complicated and depend chiefly on the development of stable or unstable conditions in the different air layers.8. There is considered to be evidence of definite ascending currents in the spring months. Except in the case of upward currents of considerable vertical extent, pilot balloon observations are not calculated to give a measure of true vertical currents as distinct from those due to turbulence.
Discussion of memoirs. On a theory of upper‐atmospheric ozone
Authors: Chapman S. 
Published: July 2010

AbstractThe main part of the paper consists of a discussion of the daily and annual variations of the ozone content of the atmosphere in any latitude up to about 50°. The ozone is treated as if it were uniformly spread through a layer of air 10 km. thick, having the same density as the air at the level of maximum ozone density. Convection and diffusion of ozone are neglected. The thermal decomposition of ozone (2O5 = 3O2) is discussed, and estimated to be negligible, except possibly in connection with an eleven‐year (sunspot) variation of ozone. The ozone is supposed formed and decomposed in the 10 km. layer; formation is attributed ultimately to dissociation of O2 by ultra‐violet radiation (1300‐1800Å); the ozone is supposed decomposed by longer‐wave radiation (2300‐2900Å); the intensities of radiation in these bands are supposed to be not greatly different from those that would occur in the spectrum of a black body at 6000°; the photo‐electric efficiency of the radiations is supposed not to be very low. Then, day by day, the dissociation of ozone would seriously reduce its amount, were it not compensated by rapid reformation (O + O2 = O3). The fact that the daily variation of ozone is inconspicuous is used to estimate a lower limit for the rate of this recombination.In so far as dissociation (O3 = O + O2) and re‐formation (O + O2 = O3) balance one another, they have no ultimate effect on the amount of ozone; but new O atoms are formed by dissociation of O2, and this tends to increase the amount of ozone. This rate of increase is supposed held in check by reactions which cause the reversion of some of the O (formed from O2 and O3) and O3 to O2, by the reactions 2O = O2, O+O3 = 2O2. These reactions occur mainly by day; most of the O atoms then present have been formed from 03. It is shown that the varying rates of these reactions can explain the observed annual variation of ozone, provided that the coefficients of reaction have suitable values.
Report on the phenological observations in the British Isles from December, 1929, to November, 1930. no. 40
Authors: Clark J. Edmund , Margary Ivan D. , Marshall Richard , Cave C. J. P. , Bonacina L. C. W. 
Published: July 2010

AbstractA survey of the 40 years since the late Edward Mawley reorganized the Society's phenological records shows that so satisfactory were his method and selection of events for observation that later developments have followed the lines he laid down. The chief increase has been in stations, which now total to thrice the average number previous to 1920.The year 1930 was officially characterised as “A Wet Year.” In fact it was the ninth in succession, giving a total rainfall excess of 90 per cent of an ordinary year. Abnormal December and January warmth and excess of sunshine in December, 1929, and November, 1930, make very partial amends for almost continuous adverse conditions in between, save only in June and the brief spell of glorious harvest weather which ended August. Hence, for farm and garden, conditions were as a rule bad. The result on the floral calendar was that no district records were early before the convolvulus in July. Spring flowers in southern parts were almost a week late. But the floral isophenes are naturally much nearer normal than in 1929. The corresponding isakairs are early mainly over southern Scotland and north‐west Ireland; they are latest in west Ireland, central Highlands and scattered English areas. Insects and birds were late; the 20 migrants by two days. A natural exception was the very early first song of the thrush. The spring isophenes can now be compared with the chart of return movements, a matter of decided interest.Three independent and unusual events are recorded, due apparently to a very exceptional diversion of the warm Atlantic current. Finally abnormal weekly divergences in the three main meteorological factors (cf. monthly values in Tables IA‐c) have been based on definite numerical values, thus permitting in future greater precision in comparing year with year.
On the secular variation of rainfall at Rothamsted
Authors: Wishart J. 
Published: July 2010

AbstractA detailed study of the rainfall at Rothamsted over the 76 harvest years, 1854‐1929, has revealed the fact that not only have there been sensible changes in the average yearly rainfall of a similar character to those observed at other stations in England and Wales, but the distribution of rainfall throughout the year has changed. The maximum in autumn (and equally the minimum in spring) occurs significantly later to‐day than was the case 76 years ago, but there is some sign that this movement is now reversing its direction, as appeared to have happened towards the end of the eighteenth and again in the middle of the nineteenth centuries, as judged from early records at a number of other stations. It would be interesting to have similar detailed analyses of the rainfall data at other places. The British Rainfall Organization is responsible for collecting the records of a very large number of stations, and a useful supplement to the monthly values now recorded would be a statement of the numerical constants specifying the distribution of rainfall throughout each year, taking as a unit a period of six days, or some other agreed number. The calculations for each year can be made on a single sheet of foolscap, and might form a routine operation at each station at the close of the year. If done for a large number of stations this analysis would furnish valuable climatological information on the general character of the incidence of rainfall over the whole country. Given information of an equal precision as to crop yield or other data of agricultural importance, the value of such rainfall distribution constants would be very great for the purposes of agricultural meteorology.
Report on the phenological observations in the British Isles from December, 1931, to November, 1932. no. 42
Authors: Clark J. Edmund , Margary Ivan D. , Cave C. J. P. 
Published: July 2010

AbstractThe Report is again based on over 15,000 individual events, although Tables VII (Tree Records) and XIV (Hevingham Records) are wanting. But we have the cheering news that the latter, going back to 1736, will reappear with the records for 1932 and 1933, thanks to the Rev. A. F. Marsham, a son of Major H. L. Marsham.Exceptional warmth again prevailed until February, which was also excessively dry. But the year was most notable for its wetness and dullness, above all, April, May and July. These gave half as much rain again as usual and only three quarters of the sunshine average. June and early autumn largely saved the situation for field and garden crops and gave a fine floral display from August on.Table V shows lateness in plant events after April to early July, of ten days or more in England and Wales, but a bare week for the British Isles as a whole, since Scotland and Ireland fared much better. Worst were England SE, SW and Midlands. The Floral Isakairs (equal divergences from the average) show this well, with areas in the former over a fortnight late for all plants against ten days early in the latter.Scarcity and lateness of the three butterflies in Tables IX and X were the response to the wet cold of late April and May. The same cause accounted for no bird in the main migrant table being early. Owing presumably to food shortage, the seven insect‐feeders up to May 9 averaged four days later than the other eight birds in the same period. The Spring migrant isophenes (equal appearance dates) lay much further south than usual, the reverse occurring in autumn, when the genial weather favoured lingering.The additional notes received from many proved, as usual, of great value and form an important part of the letterpress. The names and stations of all our observers appear this year in Table II.Tables III and V present the dates of the separate plants in each of the II Districts, with averages for England and Wales and for the British Isles, also corresponding averages for 35 years, which are confirmed after 40 pears. In an appendix are now tabulated the results decade by decade, with comparisons and ranges. Table A shows plant events by Districts, B and C by flowers, respectively, for England and Wales and for the British Isles. These tables summarise a presentation of our results from an aspect not previously attempted.
Rainfall from above 6,000 feet, in relation to upper wind and fronts
Authors: Douglas C. K. M. 
Published: July 2010

AbstractRainfall from above 6,000 feet, and the movement of rain areas with the winds at those levels, are of importance in forecasting, and sometimes cause difficulties. A suggested classification of “thermal” upper winds is into ideal frontal, frontal zonal, and non‐frontal types. The upper wind system of an ideal front is briefly discussed. Non‐frontal “thermal)” winds sometimes cause an exceptional forward extension of a rain area (example in Fig. 2). A rain area is also liable t o travel in an abnormal manner along a front, owing to upper winds of frontal zonal type (see Figs. 4 and 5). Quasi‐frontal and non‐frontal rainfall, in connection with which upper winds are often important, are discussed briefly. In an appendix it is shown that the angle of slope of a surface of discontinuity should increase as a depression deepens, and that in consequence large‐scale energy transformations are probably related mainly to converging and diverging movements over large areas, and only indirectly to surfaces of discontinuity.
Rainfall and loss over the Vyrnwy catchment area
Authors: Lloyd David 
Published: July 2010

AbstractRain falling over a catchment area is partly recovered in stream How. In specific periods, rainfall is equated to stream How plus loss. The loss is affected by several causal agents. Consequently in periods of similar rainfall the resulting stream flow varies. The relation of stream How to rainfall is deduced by analysing data from the Vyrnwy catchment area, where water is impounded by the Liverpool Corporation Water Undertaking. Records are available over a period of fifty years. Annual loss is correlated with associated rainfall and temperature data by a recent statistical method after M. Ezekial, which overcomes the inflexibility of Pearsonian methods. The functional effects of rainfall and temperature in terms of loss are described numerically and graphically. The percentage of the variance in loss due to differences in those causal agents suggests the reason why loss cannot be related to rainfall without taking into consideration other causal factors. The relations are produced descriptive of conditions at the area in a reservoired and an unreservoired state.
Natural and artificial clouds
Authors: Brunt D. 
Published: July 2010

AbstractThe motions which occur when an unstable layer of fluid breaks down have been found to be in the form of polygonal prismatic cells, in which the motion at the centre of the cell is upward when the fluid is a liquid. In air it is shown that while the motions in deep layers resemble those in liquids, except that the direction of motion is reversed, the motion in shallow layers of air made unstable by heating from below is different in appearance, and consists of a large number of ascending currents, surrounded by much slower descending currents. The motion of the air is made visible by cigarette smoke.When the air is bounded at its upper limit by a movable glass plate, it is found that the shearing produced by moving this plate will give long rolls extending through the whole length of the chamber, if the upper plate is moved sufficiently rapidly. With slower movements of the upper plate, the chamber is filled with distorted prismatic cells, and with very slow movement of the plate, the chamber is filled with rolls transverse to the direction of motion of the plate.These experimental results are applied to explain a variety of cloud forms, which are thus presumably to be explained as in part due to the effects of instability. Among these clouds are those which consist of small cloudlets on a background of blue sky, cloud sheets which show a series of clear holes, and clouds in rolls, which may be analogous to either the longitudinal rolls found in the laboratory with rapid shearing of the top plate, or to the transverse rolls found with slow shearing of the upper plate.Some comparison is given of the evidence of ascending currents in the atmosphere found by gliding pilots.A film exhibited at the meeting shows the forms taken by unstable layers during the process of breakdown, as well as of some clouds which closely resemble the structures obtained in the laboratory.
The cyclone series in the Caribbean Sea, October 17–24, 1935
Authors: Kidson E. 
Published: July 2010

AbstractIt has been held by some who have applied frontal methods of analysis to tropical cyclones, that it is the air that comes across the equator which acts as the cold air. The author has twice passed through the Caribbean Sea during disturbed periods, and the present paper is a study of the weather experienced: the information available indicates that the cold air came from the north and that the air from across the equator was the warm mass.
The lunar atmospheric tide at five Japanese stations
Authors: Chapman S. 
Published: July 2010

AbstractThe lunar atmospheric tide at five Japanese stations, Taihoku, Naha, Kumamotu, Tokio and Sapporo, in latitudes 25°, 26°, 33°, 36°, 43°N., have been found from bi‐hourly values of the barometric pressure extending, in the aggregate for the five stations, over 193 years. The harmonic coefficients for the solar diurnal barometric variation at these stations have also been calculated.
Report on the phenological observations in the British Isles from December, 1335, to November, 1936. No. 46
Authors: Margary Ivan D. 
Published: July 2010

AbstractThe year was remarkable for sunlessness generally, and also for wetness in England and Wales, b u t temperature after a cool winter remained close to normal. The result was a rather gloomy and inclement year due to lack of sunshine and excess of rain rather than to low temperature. Plants generally flowered late, all in the Midlands, nearly all in England SE., SW., and Ireland S., but were earlier in Scotland, especially in Scotland W. Floral isakairs show a late strip across southern Ireland and Wales, the Midlands and England NE., with slight earliness over a wide area in NE. Ireland, the Scottish Lowlands and East Coast. Insects were nearly all late in appearing in England, but were very erratic in Scotland and in Ireland N. Spring migrants were generally late, save in Scotland, but the earliest arrivals were early as they just escaped the cooling of April. Spring migrant isophenes show a restriction of the usual early landing areas, with a rather slow advance afterwards. The autumn migrants were mostly early in moving.
Kinetic energy liberated in an unstable layer
Authors: Normand C. W. B. 
Published: July 2010

AbstractKinetic energy is released when an unstable super‐adiabatic layer of constant lapse‐rate ϵΣ rights itself (where Σ is the adiabatic lapse‐rate and ϵ > I). The average kinetic energy can be computed analytically by Margules's method or graphically on the tephigram. By Margules's method a good approximate formula for the resulting average velocity is shown in this paper to be v = constant × Ap/II {(ϵ‐I)Θ)½, where II and Θ are the mean pressure and temperature of the column and Δp is the pressure difference between the top and bottom of the column. The method of the tephigram gives the average energy to be equivalent to one‐sixth the area of a parallelogram of which the diagonals are the initial and final temperature curves of the column. Some examples are numerically evaluated by these methods and the results show close agreement with values previously calculated by a longer and more laborious method by Littwin.
The importance of vertical motion in the development of tropical revolving storms
Authors: Durst C. S. , Sutcliffe R. C. 
Published: July 2010

AbstractThe problem discussed is that of the mechanism for the eviction of air from tropical revolving storms. By the examination of the equations of motion it is found that this eviction could be explained by the up How of air from layers of greater velocity to those of less velocity.A proposition which may have important applications to many other problems is enumerated.
Does thunderstorm rain play any part in the replenishment of the earth's negative chaarge?
Authors: Banerji S. X. 
Published: July 2010

AbstractAt Bombay thunderstorms invariably move overhead in some east‐west or west‐east direction according as they are “heat” thunderstorms or “line‐squall” thunderstorms. Lln analysis has been made of the charge brought down by rain during the passage of 23 thunderstorms over Bombay in the years 1930‐32. During 1930‐31, nine thunderstorms transferred to each sq. cm. of ground 0.52 E.S.U. of positive charge and 0'75 E.S.U. of negative charge, and during 1931‐32 fourteen thunderstorms transferred to each sq. cm. of ground 0.59 E.S.U. of positive charge and 1.46 E.S.U. of negative charge. Therefore, the 23 thunderstorms, collectively transferred t o each sq. cm. of ground 1.11 E.S.U. of positive charge, and 2.22 E.S.U. of negative charge. Estimating that an area of (100 km.)2 received charge at the rate recorded at Bombay, it is concluded that on the average each thunderstorm transferred to the ground an excess of about 2 × 103 coulombs of negative electricity.
Atmospheric optical phenomena in North East Land
Authors: Moss R. , Whipple F. J. W. 
Published: July 2010

AbstractA record is given of the various atmospheric optical phenomena observed during the ten months' occupation of a station on the inland ice of North East Land (80° N., 20° E.) by the Oxford University Arctic Expedition, 1935‐36.As well as the more common mock‐suns and mock‐moons, several complexes were observed, notably on June 6, 1936, when the comparatively rare Parry arc occurred.There were also many instances of a phenomenon which has occasionally been described previously, but which has not been distinguished from others, with which it usually occurs simultaneously. It takes the form of a pair of white mock‐suns on or near the visible horizon; they do not appear to be essentially connected with the usual “prismatic” halo phenomena. The name “hypohelia” is proposed for them.