wave shock earthquakes seismic direction vertical mallet velocity waves surface
EARTHQUAKE. Although the terrible effects which are often produced by earthquakes have in all ages forced themselves upon the attention of man, it is nevertheless only within the last thirty years that the phenomena have been subjected to cxact investigation. A new science has been thus established under the name of seismology (Teta inin, an earthquake). This branch of knowledge, how-ever, has hitherto attracted but few students, and its de-velopment in England has been almost exclusively due to the researches of Mr Robert Mallet. References to his principal works will be given at the end of this article.
Accounts of earthquakes are to be found scattered through the writings of many ancient authors, but they are, for the most part, of little value to the seismologist. There is a natural tendency to exaggeration in describing such phenomena, sometimes indeed to the extent of import-ing a supernatural element into the description. It is true that attempts were made by some ancient writers on natural philosophy to offer a rational explanation of earthquake phenomena, but the hypotheses which their explanations involved are, as a rule, too fanciful to be worth reproducing at the present day. It is therefore unnecessary to dwell upon the references to seismic phenomena which have come down to us in the writings of such historians and philoso-phers as Thucydides, Aristotle, and Strabo, Seneca, Livy, and Pliny. Nor is much to be gleaned from the pages of inedival and later writers on earthquakes, of whom the most notable are Fromondi (1527), Maggio (1571), and Tra,vagini (1679). In this country-, the earliest work worthy of mention is Dr Robert llooke's Discourse on Earthquakes, written in 1668, and read at a, later date before the Royal Society. This discourse, though contain-ing many passages of considerable merit, tended but little to a correct interpretation of the phenomena in question. Equally unsatisfactory were the attempts of Priestley and some other scientific writers of the last century to connect the cause of earthquakes with electrical phenomena. The great earthquake of Lisbon in 1755 led the Rev. John Michell, professor of mineralogy at Cambridge, to turn his attention to the subject ; a,nd in 1760 lie published in the Philosophical Transactions a remarkable essay on the Cause and Phenomena of Earthquakes. Regarding the earth a,s having a liquid interior covered by a comparatively thin.crust, he conceived that waves might be generated in this subterranean liquid, and that such waves by shaking the flexible crust would produce the shocks of an earthquake.
His illustration of the movement of the ground is that of a loose carpet thrown into undulations by being shaken at one corner. Although Michell's hypothesis is still a,ccepted, in a modified form, by some geologists, it should be remembered that many arguments of considerable weight have been urged by modern physicists against the doctrine of a liquid nucleus and a thin crust. Whatever the merits of Michell's theory, he failed to understand the true nature of wave-motion, and the way in which it is transmitted during an earthquake shock. Modern seismologists believe that an earthquake is a vibratory motion propagated through the solid materials of the earth,.much in the same way that sound is propagated by vibrations in the atmo-sphere. It appears that this view was first suggested by Dr Thomas Young in his Lectures on AVatural Philosophy, published in 1807. The development of this -view, especially in its quantitative results, lies at the very base of seismology. In 1816 Air Mallet communicated to the Royal Irish Academy his first paper " On the Dynamics of Earthquakes ; " and in the following year the late Atr Hopkins, of Cambridge, presented to the British .A_ssociation a, valuable report in which earthquake-phenomena are dis-cussed in some detail. Since that date the great advances in this country have been made by Mr AIallet, assisted occasionally by the Rev. Professor Haughton and other inathematicians.
Even at the present day, after all that has been written on the subject, but little is really known as to the origin of earthquakes. Probably several distinct causes should be recognized, for it is hardly to be supposed that all sub-terranean disturbances, differing as they do so widely in intensity and in duration, should be referable to one common mechanism. Any great concussion, even upon the surface, is competent to produce tremors which may be regarded 3.8 diminutive earthquakes ; thus the great landslip at the Rossberg in Switzerland in 1806 was accompanied by a local quaking of the ground. Volger and Alohr have suggested that some of the small earthquakes which have been felt in Germany may be referred to the falling-in of the roof of enormous subterranean cavities formed by the, long-continued solvent action of water on deposits of rock-salt, limestone, and gypsum. Such causes, however, can have given rise to only very petty shocks, and must be quite subordinate to subterranean disturbances of a more general character. The late Mr Poulett Scrope was led to refer most earthquakes to " the snap and jar occasioned by the sudden and violent rupture of solid rock-masses, and perhaps the instantaneous injection into them of intumescent molten ma,tter from beneath." He believed that the rupture of the rocks was dne to expansion of deeply seated masses of mineral matter, conseqUent upon either increased temperature or diminished temperature. It is argued, however, by Mr Mallet, on mechanical principles, that such fractures could produce only very weak impulses ; but he believes that some earthquakes, especially those marked by long continued tremors, may be due to the movement and crushing of rock masses by tangential pressures produced by secular cooling of the earth. Steam has always been a favourite agent with seismologists, since it is clearly com-petent to produce great effects by- its sudden generation or by its sudden condensation. It has been suggested that water, finding its way through fissures in the earth's crust, might reach Itighly-heated rocks and remain quietly, in tbe spheroidal condition, until a local reduction of temperature suddenly caused it to flash into steam. After all, the origin of earthquakes is probably to be regarded as part only of a much wider question. Whatever causes are competent to produce volcanic action are, in all likelihood, equally competent to produce the ordinary manifestations ot selstmc energy. A relation is clearly traceable between the geographical distribution of volcanoes and the chief earthquake-areas ; and although it is not for a moment to be supposed that the volcano and the earthquake stand to each other in the relation of cause and dffect, it is never-theless highly probable that they represent merely different expressions of the same subterranean forces.
Whatever may be the real origin of the earthquake shock, it is cmvenient to regard its effects as proceedin,g front a. concussion or sudden blow delivered underground at some definite centre. This centre of impulse is called the seismic focus. It must be borne in mind, however, that such a centre, so far from being anything like a, mathe-matical point, is in nature a subterranean region, which iu many cases is no doubt of very large dirnensions, measuring perhaps some miles in diameter.
From the seismic centre waves are propagated in all directions through the solid materials of the earth's crust ; and if the focus be situated beneath the sea, the vibrations of the ground will be accompanied by undulations of the water. Those waves which pass through the elastic materials of the earth consist, for the most part, of longi-tudinal vibrations, like those of atmospheric sound-waves, and consequently not like ordinary water-waves. In the sound-wave the air is alternately condensed and rarefied, the molecules advancing and retreating in the line of direc tion in which the wave is travelling. In a water-wa3,,e, on the contrary, the molecules of liquid rise and fall, or rather describe closed curves in planes which are transverse to the direction in which the undulation or wave-form advances. According to Mr Hopkins, both orders of vibra-tion - longitudinal and transversal - coexist in the earth quake-wave, and call for investigation. When, for example, the molecules of an iron bar are disturbed by a blow delivered at one end, both kinds of vibration are generally excited, and hence two waves are sent through the bar, - the longitudinal, however, having a much oTeater velocity than the transversal wave. But it may be deubted whether the seismologist need concern himself with any but longi-tudinal vibrations. For, admitting that small transversal vibrations are generated at the seismic focus, it is probable that they would be cut off to a great extent during trans-mission from stratum to stratum. Indeed, the planes of junction between the several beds in stratified deposits would hinder the transmission of transversal vibrations travelling in a direction normal to the strata. Hence Mr Mallet maintains, that in studying the effects of an earth-quake, attention may be restricted, without danger of error, to the longitudinal or normal vibrations, the transversal or tangential vibrations being neglected.
Around the seismic centre, or mean focal point, the molecules of the rock will first be squeezed tooether by the concussion, and then separated by virtue of the elasticity of the solid medium ; the onward motion is then rapidly taken up by the next set of molecules, which in like manner are pushed against each other, and then spring apart. In this way the pulse, or form of the wave may be propagated to an enormous distance, whilst t'lle excursions of the individual particles are confined within very narrow limits. It is therefore of great importa,nce to distin,guish between the transit of the wave and the move,ment of the material particles. Each molecule inay move only through a few inches, but the undulation may travel for hundreds of miles. The distance through which the individual particles oscillate is called the amplitude of the wave. After the Neapolitan earthquake of 1857 Mr Mallet found from actual observa-tion at a place called Polla, situated nearly above the seismic centre, that the amplitude of a wave which caused certain fractures in masonry could not have been more than 21 inches. He is thus led to believe, contrary to the opinion of most geologists, that earthquakes are not great aoents permanent elevation. That elevation has been frequently observed after an earthquake is a fact beyond question ; thu.s, Captain Fitzroy found, after the South American earthquake of 1835, that a part of the isle of Santa Maria, ia the Bay of Concepcion, had been raised upwards of 10 feet, and, although this elevation was followed by a slow subsidence, it is believed that the land was permanently left considerably higher than its level before the occurrence of the catastrophe. Mr Mallet, however., would refer such alteration of level to the action of elevatory forces accom-panying the earthquake, but not to the direct transit of the earth-wave.
From the density and the modulus of elasticity of a given rock, it is possible to calculate the velocity with which a vibration would travel through such a medium. But the rate deduced by calculation usually exceeds very greatly that actually observed in an earthquake. To determine the rate of transit through various rocks, Mr Mallet and his son Dr J. W. .Mallet conducted many years ago a series of experintents, at the instance of the British Association. A mile was carefully levelled and measured on sand in Killiney Bay, near Dublin, and by explosion of gunpowder the velocity of transmission through this damp sand was observed. This sand was selected as a medium likely to give a minimum velocity, whilst an assumed maximum velocity was observed by experiments on the granite of Killiney Hill. The velocity in sand was about 825 feet, and in solid granite 1665 feet per second. These figures are much lower than those obtained from theoretical con-siderations, and it is believed that the difference is due to loss of speed occasioned by the discontinuity of the rock, even the solid granite being always more or less affected by joints. The velocity deduced from these experiments accords tolerably well, however, with that observed during earthquake-shocks. Thus the velocity of shock during the Lisbon earthquake of 1755 is computed to have been about 20 miles per minute, or 1760 feet per second. This velocity of the vibration, or wave. of shock, is of course to be carefully distinguished from the velocity of the oscillat-ing particles. The mischief of the shock depends in fact on the rate at which the earth-molecules are moving, and this is vastly inferior to that of the wave. Thus Mr Mallet calculated from his observations in Naples that the shock of the great earthquake of 1857 had a mean velocity at the surface of 788 feet per second, whilst the greatest velocity of the wave-particles was never more than 15 feet per second, and in many places was very much less. Yet this low velocity is quite sufficient to produce effects of the most disastrous kind upon solid objects exposed to the shock.
If the earth were 3. homogeneous solid, perfectly isotropic - that is to say, possessing equal elasticity in all directions - the waves of alternate compression and expansion would take the form of a series of concentric spherical shells around the seismic focus as a common centre. As a matter of fact, however, the crust of the earth is made up of rocks varying greatly in physical properties, each having its own density and elasticity, whilst the rocks themselves are fissured in all directions. Symmetry of wave-surface is therefore hardly to be expected ; for the waves will neces-sarily have greater velocity in one direction than in another, whilst the transit of the tvave may be interrupted by breach of continuity in the transmitting medium. The points at which a wave-shell reaches the surface form a curve which is conveniently called a coseismal line. It is obviously the line along which an earthquake shock will be simultane-ously felt, and where the waves will emerge at the same angle. Since the wave-shells are not concentric spheres, the coseismal curves cannot be concentric circles.
It may readily be supposed that the greatest effect of an earthquake, at least in shaking a building up and clown, will be felt at that point of the surface which is situated vertically over the centre of impulse. A line joining this point with the earthquake-focus is termed the seismic vertical, and the wave travelling to the surface along this vertical has a shorter path than that of a wave emerging at any other point. Just as the seismic focus is, in nature, not a single point, but a considerable space, so the seismic vertical is not a single line, but rather a succession of parallel lines drawn vertically from every point of the focal area to the surface. The mean of these lines may be taken a.s the seismic vertical. In the neighbourhood of this line the waves emerge at very steep angles, and indeed for a considerable area may be reg,arded as practically vertical in direction. As the distance from the seismic vertical increases, the angle of emergence becomes less and less ; but it is evident that since the focus is seated beneath the surface, the path of an emergent wave can never be perfectly horizontal, unless indeed it be that of a reflected wave.
Almost any object which has been overthrown or projected by an earthquake-shock- may afford direct information as to the path of the wave along the surface. For when the vibration is trans-mitted to such a solid body as au upright column, the particles are pushed together and then pulled apart in the line of wave-transit. It is clear too that half the excursion of each particle is executed in the same direction as that ,in which the wave is travelling, and half in the opposite direction. Each particle of the object when first disturbed moves with the Nvave, aud its velocity increases from zero to the maximum, this maximum being reached et oue quarter of the total vibration • then the velocity diminishes from the maximum to zero, whicit it attains at the end of half the oscillation. Durin,g this first semi-phase, therefore, the vibration has been in the direction in which the wave moves. After the first half oscillation has been executed, niovernent begins afresh, but this time in the contrary direction, attaining its maximum at the end of the third quarter, and then again to zero when the vibration is completed. Hence during the first semi-phase, the motion of the particles is in the same sense or direction as that of the wave, and during the second semi-phase in the opposite diree-tion. But in consequence of the inertia of the body its apparent movement if free, will be in a direction contrary to that of the wave during the first senti-pliase. Whatever the direction of overthrow, however, it will always be in the tine of wave-transit. Hence the azimuthal direction of the v.-ave is easily found.
Whenever any two wave-paths, not in the same right line, can be thus traced on the surface, the position of the seismic vertical niay be immediately determi»ed. For this line must pass through the point of their in-tersection. If, for example, it is found by observation on bodies displaced by the shock that one wave moved in the direction A 11 (fig. 1), whilst another had a path along CD, it is only necessary to mark on the surface the point 0, at which them azimuths meet, and the seismic foots will be vertically be-neath such a point. The point indicates, in fact, the centre on the surfitee from which the waves radiated. Practically it is found that the several wave-paths of an earthquake do not diverge from a single point, for reasons already indicated; but intersections of - the paths are crowded together in the neighbourhood of the mean vertical.
It is easy to understand that the greatest amount of mechanical damage is not to be expected innnediately above the focus, although this is the point nearest to the origin of impulse. It is true, the shock passing directly upwards along the seisntic vertical might destroy the roof or floor of a building, but it wonlil not tend directly to overtuin the walls or produce lateral disturbance. In fact, the side-thrust will be greatest in waves which reach the surface ut small angles, and are therefore necessarily at great dis-tanees from the seismic vertical. But the energy of the wave diminishes as the square of the distance along the normal inereases. Hence there inust be some definite position upon the surface beyond which advantage of direction is counterbalanced by loss of energy. indeed it is generally possible after an earthquake to trace a zone or maximum disturbance, where the damage to the shaken country has been greatest. The line indicating this maximum is termed the meizoseisinic curve, whilst lines along which the overthrow of objects may be regarded ti.s practically the same are known as isoseismic curves. After what has been already said, it is hardly necessary to remark that these lines are not true circles, uor indeed are they in all cases regular closed curves.
Fractures and fissures in walls which have been rent by an earth-quake, are of great value to the seismologist, since they often indicate the direction in which the waves emerge at the surface. The interpretation of such phenomena, in some cases very compli-cated, has been ably discussed by Mr Mallet, who applied the results with excellent effect to bis observations on the Neapolitan earthquake. If it is possible to find, from such indications, the direction in. which any two waves emerged at the surface, the depth of the seismic focus is easily determined. For since the waves radiate from this focus, any two wave-paths when produced back-wards will meet at the seismic centre. It has already been shown how easily the vertical is found, and when this is known the deter-mination of the fecus is s.implified, for as the vertical itself repre-sents one-wave path it is necessary to find only one other. Let 0 (fig. 2) be the seismic focus, and OA the seismic vertical; if a wave, OB, emerge at the surface B, at an angle 8, it is evident that AO - AB. tan O.
To find the depth of the focus, it is consequently only necessary to know the angle of emergence of a wave at a given station, and the distance of this station from the seismic vertical. As the stations A and B are comparatively near each other, the e.arth's sphericity may be neglected, and the surface between the two regarded as practically a horizontal plane.
Where several wave-paths are known, several values of AO will be obtained, and as the seismic centre is not a point, like 0, but a cavity of determinate magnitude, the average of these different values must be taken to represent the mean focal depth. After the great Neapolitan earthquake of 1857, Mr Mallet, aided by the Royal Society, spent some months in carefully examining the country which had been visited by the shock ; and in 1862 he published an elaborate report in which his observations were fully discussed. By deterinining the wave-paths at twenty-six stations in every azimuth around the seismic vertical, he was enabled to deduce the important fad that the inean focal depth of the earthquake was about 51. geographical miles. Similar principles have since been applied by Dr Oldham to an examination of the results of an earthquake which occurred in Cachar in India, on January 10, 1860 ; and he has found that the seismic focus there must have had a depth of about 30 miles. This coincides veiy nearly with the depth which ISIr Mallet believes to be the maximum at which any earthquake is likely to originate in our planet.
When the centre of disturbance is seated beneath the sea, as appears to have been Wie case with that which produced the great earthquake of Lisbon in 1755, a water-w ave is generated; but since this has less velocity than the earth-wave, it does not roll in upon the shore until after the shock has been felt on land. The height of the sea-wave depends on the depth of the water. During the Lisbon earthquake the wave at Cadiz was as much as sixty feet in height. It is this great sea-vvave which, breaking upon the shore after the earthquake-shock, generally completes the work of devastation. At first the water retires from the land, but in a few moments the gigantic wave rolls in, and sweeps all before it. The earthquakes which are so frequently felt on the western coast of South America are generally terminated in this manner ; and the great tidal wave which accompanied the earthquake of May 1877, wrought dreadful havoc at Arica, Iquique, and other towns on the coast.
In addition to the waves 'propagated through earth and sea, it commonly happens that waves are transmitted through the air and thus produce sound. These sound-waves, travelling at the rate of about 1100 feet per second, inay reach the observer either simul-taneously with the shock or before it or even after it. They pro-bably result from sudden fracture aud dislocation of rock-masses, or from subterran3an explosions.
Almost every object disturbed by an earthquake may be made to yield, when properly questioned, more or less information with respect to the direction and intensity of shock. Special instruments termed seismometers have, however, been constructed for this purpose, and have assumed considerable variety of form. Perhaps the simplest seismometer is that suggested by Mr Babbage, consisting merely of a bowl of some viscid liquid like treacle. On the passage of a shock the liquid rises up one side of the vessel, leaving its mark to indicate rudely the direction and extent of motion. As a modification of this simple instrument Mr Mallet proposed the use of a common wooden tub having its inside rubbed with chalk, aud half filled with coloured water. An apparatus devised by Professor Cacciatore, of Palermo, and much used in Italy, is constructed with a shallow dish having eight notches in the side, and containing mercury up to the level of the lips. When any oscillation occurs, the liquid is spilt into a series of cups placed under the notches; and the quantity ejected, which may be readily weighed, gives some notion of the intensity of the shock. Since the notches face the four cardinal points and bisecting thumbs, the direction in azimuth is approximately obtained. Mr Mallet suggested a convenient form of seismometer in the shape of a system of four L-shaped glass tubes having the upper ends closed and the horizontal limbs directed to the cardinal points. The tubes are partially filled with mercury, and the horizontal component of any shock causes the mercury to move in the lower limbs; whilst the vertical component is determined by the motion of quicksilver in a U-shaped tube. In both cases, the movemeut of the liquid coluran is registered by means of indexes.
All these instruments depend for their indications on the displacement of liquids by the shock of the earthquake. But it is obvious that the oscillations of solid bodies may be equally well employed in seismometry. Thus a pendulum free to move in all directions will be set vibrat-ing by a shock, and may be made to record the direction and extent of its vibration by means of a stile below the bob, which moves over a bed of fine sand in a properly-shaped dish. Two pendulums are sometimes used, as pro-posed by Santi. One pendulum vibrates in a vertical plane directed north and south, anti the other in one striking east and west, - the arcs traversed in these planes being registered by means of a tracing-stile affixed to the bob. Professor J. Forbes employed an inverted pendulum, or rod fixed at its base and weighted. above, carrying at its free end a pencil or tracer by which any oscillation could be recorded. A modification of the inverted pendulum was proposed by Mr Budge of Valparaiso, in which the pendulum when moved by the first shock was kept in position at the end of a semioseillation, by means of a pawl working in a ratchet on the base of the vibrating body.
Such seismometers as those previously noticed require to have their indications observed after each shock. Several ingenious instruments have; however, been con-structed on self-registering principles, so that however often they are disturbed, each movement leaves a permanent record. The first of these self-registering seismometers was devised by Mr Mallet, and described in 1846. Both the horizontal and the vertical element of a shock are recorded by the movement of mercury in a system of glass tubes, the tubes being placed in a galvanic circuit so arranged that contact is broken by displacement of the liquid. As long as the circuit remains complete, a pencil traces a line on ruled paper wound round a cylinder rotated. by clock-work, but the motion of the mercury intercepts the current and thus breaks the line. Two forms of " ball seismometer " are also due to the ingenuity of the same investigator. In one of these iustruments, two heavy metal balls are placed on slightly inclined planes supported by a east-iron table, the axis of which passes through a vertical spiral spring. During the passage of au earthquake wave the spring is compressed and the balls displaced,-their displacement breaking contact in an electric circuit which had previously been completed through the balls. That ball which first moves gives the time at which the shock commences, whilst the other gives the elements of the shock. Two such instruments are necessary to form one seismometer, the two being placed at right angles to each other.
An elaborate electro-magnetic seismograph has been con-structed by Professor Palmieri, and has done good service in the observatory on Mount Vesuvius. The vertical move-ments are recorded by a helix of copper wire, the lower end of which is caused by even the slightest shock to dip into a basin of mercury, and thus complete a galvanic circuit. An electro-magnet, brought into action when the connec-tions are completed, strikes an alarm bell which calls an attendant, and also stops a clock, so that the instant at which the shock occurs is permanently 'narked. At the same time a second electro-mag,net releases the pendulum of another clock, which being thus set in motion unrolls a band of paper, while a pencil continues to mark upon the paper as long as the shock lasts. To record the vertical element a system of four U-shaped tubes is employed, the tubes being placed in different azimuths. Each limb is partly filled with mercury, and any oscillation in the level of the liquid is indicated by movement of a little float con-nected with an index. The oscillation of the quicksilver also completes a galvanic circuit, aud brings into action the electro-magnets already described.
Although the limits of this article forbid reference to some other seismometers, such as that of Kreil of Vienna, mention should certainly be made of one instrument which is marked by its extreme simplicity. Its construction, which is due to Mr Mallet, will be understood by reference to fig. 3. Two sets of right cylinders are turned in some hard material, such as boxwood. The cylinders are all of the same height, but vary in diameter. Two planks of wood are fixed to a level floor, one having its length in a north-and-south, and the other in an east-and-west direction. The cylinders stud upright on the planks in the order of their size, with a space between each pair greater than their height, .so that when one pillar falls it does not strike its neighbour. The surrounding floor is covered up to the level of the planks with dry sand. When a shock passes, some of the cylinders are overturned, the number depend-ing on the velocity of the wave. Suppose the shock knockp over the narrow-based cylinders 4, 5, 6, leaving Nos. 1, 2, 3 standing ; then the velocity of the horizontal component m us t have been greater than that needed to overturn No. 4, but not great enough to overturn No. 3. Ilence the velocity (V) can be approximately obtained by using a formula due to Professor Houghton, viz. ; y2 = I5b2 16a2. - cos 0); where a is the altitude of the column, b the diameter of its base, and 0 the angle formed by the side and a line drawn through the centre of gravity to the extremity of the base. The direction in azimuth is indicated by the position in which the overturned pillars are found, since the bed of sand prevents rolling. It is possible to obtain the exact time at which the shock commences by connecting the narrowest-based pillar with the pendulum of a clock so as to stop it at the instant of overthrow. Where the angle of wave-emergence is very steep, this instrument is not to be recommended, since it ignores the vertical element of the shock.
Catalogues of earthquakes, showing their distribution in time and space, have been constructed by Mallet, Perrey, Von Hoff, Cotte, and other seismologists. The most complete of these statis-tical works is the catalogue raisonne compiled by Mr R. Mallet and his son, Dr J. W. Mallet, and published by the Brithli Associa-tion between the years 1854 and 1858. This includes notices of all recorded earthquakes from 1606 B.C. to 1842 A.D., and is thence carried on to 1850 from Perrey's annual catalogues. Between 6000 and 7000 separate earthquakes are recorded as haying occurred in almost every part of the world, both on land and at sea. But though seisniic energy may thus become sensible at any point of the earth's surface, there are, as everyone knows, certain regions peculiarly subject to earthquakes ; and it is, in fact, possible to trace seismic bands of variable width following the great lines of elevation which divide the oceanic basins.
It is now several years since l'rofessor Alexis Perrey, of Dijon, sought to trace a relation between the occurrence of earthquakes and the age of the moon. By careful analysis of his catalogue he believed that he had established the facts-that earthquakes occur more frequently at the syzygies than at the quadratures, that their frequency increases at the perigee and diminishes at the apogee of the moon, and that shocks are more frequent when the moon is on the meridian than when 90° from it. Such a connection between seismic phenomena and the phases of the moon would accord with Zantedeschi's views on the existence of a terrestrial or terrene tide, yiews which were based, however, on the old hypothesis of a liquid nucleus in the earth, covered by a thin crust.
From Mallet's discussion of his catalogue for three centuries, lie was led to detect definite periods of maximinn energy. Thus it is found that the greatest number of earthquakes are recorded about the middle of each century ; whilst a second epoch, less powerful than the first, occnrs towards the close of the century. According to I'errey there is a preponderance of earthquake-shocks at particular seasons, the equinoxes and solsticog, which he terms " critical epochs." Mallet's analysis of a large catalogne showed a decided maximum about the winter solstice, but Perrey's other epoells were less marked. lu the present state of our knowledge it would be rash to regard seismic force, whatever it may be, as a distinctly periodic force, or to insist upon any of those relations between earthquakes and meteorological phenomena which have sometimes bon discussed.
Annual reports on earthquakes have been published for many years by Professor Fuchs. During the year 1876 he recorded 104 earthquakes, which were distributed among the months as follows :- In January 10, February 10, March 14, April 8, May 7, June 7, July 8, Au,gust 5, September 7, October 14, November 5, December 9. In the preceding year 97 earthquakes were noticed, occurring as follows :-ln January 15, February 7, March 12, April 7, May 9, June 10, July 6, Atigust 5, September 3, October 2, November 9, December 12.
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