Weare en ‘ ‘ fee ‘ wera a. S . uct . < « ° . . ’ ay vos $
f . 5 #44 ' ; 7 : ra ; Bons dy Les Sborstye: Hand sodep pas w an
\ ». a ‘ x 4
% Alas r
/ : ; 3
’ . . wis , +
x ¥ mr . af 2
; a , 4 P2 , a
3 J 4 Say ce : x

4 : ‘i PATh ‘ Ne eee ees eer eee ee ee ee San eee hee ec tie .
A+ J . , ‘ ' - us . * . : setts eee dente “See mt
7 : é at 4 ° a
7 . as “eet * R :. .
» » z
% 2 >
J 7 <s mt + Shy,
P > afi ~ ~S ah
i. 4s - r . a y , ~ . .
: : . . " -- - poate ety
‘ - ~
s a £4 .
iF Z . sd 0 :
2 Xs 7a . ‘ a ary abit
* . ° ae . A . , = : :
rr - ~~ 4 + 4 N 4 y —_ omen Reon armani
Q ‘ 7
~ 7 43 ary aa ys . d
q
/ ‘ : : doit tment een tein eo cmap me f
- rl a x c oe :
. 2 . . ~ a s z ;

“THE INTERNATIONAL SCIENTIFIC SERIES
ee 2 VOLUME LV

- - t
»
.
i ¥,
‘ :
i
.
rf 4
eh

THE

INTERNATIONAL SCIENTIFIC SERIES,

—

bo

os

ee

=)

10.
11.

12.

13.

14.

Each BOOK COMPLETE IN ONE VOLUME, 12M0, AND BOUND IN CLOTH.

. FORMS OF WATER: A Familiar Exposition of the Origin and Phe-

nomena of Glaciers. By J. Tynpaut, LL.D., F.R.S. With 25
Illustrations. $1.50.

. PHYSICS AND POLITICS; Or, Thoughts on the Application of the

Principles of ‘‘ Natural Selection’? and ‘‘ Inheritance”’ to Political
. Society. By Watter Bacenor. $1.50.

. FOODS. By Epwarp Suiru, M. D., LL. B., F.R.S. With numerous

Illustrations. $1.75.

MIND AND BODY: The Theories of their Relation. By Atrx-
ANDER Bain, LL.D. With 4 Ilustrations. $1.50.

THE STUDY OF SOCIOLOGY. By Herspert Spencer. $1.50.

. THE NEW CHEMISTRY. By Professor J. P. Cooxe, of Harvard

University. With 31 Illustrations. $2.00.

ON THE CONSERVATION OF ENERGY. By Batrour Stewart,
M. A., LL. D., F.R.S. With 14 Illustrations. $1.50.

- ANIMAL LOCOMOTION; or, Walking, Swimming, and Flying. By

J. B. Perticrew, M. D., F.R.8., etc. With 130 Illustrations. $1.75.

. RESPONSIBILITY IN MENTAL DISEASE. By Henry Mavps-

LEY, M.D. $1.50.
THE SCIENCE OF LAW. By Professor Saztpon Amos. $1.75.

ANIMAL MECHANISM: A Treatise on Terrestrial and Aérial Loco-
motion. By Professor E. J. Marry. With 117 Illustrations. $1.75.

THE HISTORY OF THE CONFLICT BETWEEN RELIGION
AND SCIENCE. By J. W. Draper, M.D., LL.D. $1.75.

THE DOCTRINE OF DESCENT AND DARWINISM. By Pro-
fessor Oscar Scumipt (Strasburg University). With 26 Illustra-
tions. $1.50.

THE CHEMICAL EFFECTS OF LIGHT AND PHOTOGRAPHY.
By Dr. Hermann Voget (Polytechnic Academy of Berlin). Trans-
lation thoroughly revised. With 100 Illustrations. $2.00.

New York: D. APPLETON & CO., 1, 3, & 5 Bond Strect.

2

The International Scientifie Series.—(Continued.)

15.

16.

Ln

Ase

19.

20.

21.

22.

23.

24,

25.

26.

27.

28.

29.

FUNGI: Their Nature, Influences, Uses, ete. By M. C. Cooxz, M. A.,
LL.D. Edited by the Rev. M. J. Berkeley, M.A., F.L.S. With
109 Illustrations. $1.50.

THE LIFE AND GROWTH OF LANGUAGE. By Professor
Wituam Dwicut Wuirney, of Yale College. $1.50.

MONEY AND THE MECHANISM OF EXCHANGE, By W.
STantey JEvons, M.A., F.R.S. $1.75.

THE NATURE OF LIGHT, with a General Account of Physical
Optics. By Dr. Evcene Lomuer. With 188 Illustrations and a
Table of Spectra in Chromo-lithography. $2.00.

ANIMAL PARASITES AND MESSMATES. By Monsieur Van
BENEDEN. With 83 Illustrations. $1.50.

FERMENTATION. By Professor ScntrzensercEr. With 28 Illus-
trations. $1.50.

THE FIVE SENSES OF MAN. By Professor Bernstern. With 91
Illustrations. $1.75.

THE THEORY OF SOUND IN ITS RELATION TO MUSIC. By
Professor Pizrro Biaserna. With numerous Illustrations. $1.50.

STUDIES IN SPECTRUM ANALYSIS. By J. Norman Locxyer,
F.R.S. With 6 Photographic Illustrations of Spectra, and numer-
ous Engravings on Wood. §2.50.

A HISTORY OF THE GROWTH OF THE STEAM-ENGINE.
By Professor R. H. Tuursron. With 163 Illustrations. $2.50.

EDUCATION AS A SCIENCE. By Arrexanper Bain, LL.D,
$1.75.

STUDENTS’ TEXT-BOOK OF COLOR; Or, Modern Chromatics.
With Applications to Art and Industry. By Professor Oaprn N.
Roop, Columbia College. New edition. With 130 Illustrations.
$2.00.

THE HUMAN SPECIES. By Professor A. pe QuarrEFacres, Mem-
bre de l'Institut. $2.00.

THE CRAYFISH: An Introduction to the Study of Zodlogy. By T.
H. Huxtey, F.R.S. With 82 Illustrations. $1.75.

THE ATOMIC THEORY: By Professor A. Wurtz. Translated by
E. Cleminshaw, F.C.8. $1.50.

New York: D. APPLETON & CO., 1, 3, & 5 Bond Street,

30.

31.

30.

36.

37.

The International Scientific Series.—(Continued.) 3

ANIMAL LIFE AS AFFECTED BY THE NATURAL CONDI-
TIONS OF EXISTENCE. By Karu Semper. With 2 Maps and
106 Woodcuts. $2.00.

SIGHT: An Exposition of the Principles of Menocular and Binocular
Vision. By JosrrpH Lr Contr, LL.D. With 132 Illustrations.
$1.50.

. GENERAL PHYSIOLOGY OF MUSCLES AND NERVES. By

Professor J. Ros—entHAL. With 75 Illustrations. $1.50.

. ILLUSIONS: A Psychological Study. By Jamus Sutty. $1.50. _
. THE SUN. By C. A. Youne, Professor of Astronomy in the College

of New Jersey. With numerous Illustrations. $2.00.

VOLCANOES: What they Are and what they Teach. By Jonn W.
Jupp, F. R.S8., Professor of Geology in the Royal School of Mines.
With 96 Illustrations. $2.00.

SUICIDE: An Essay in Comparative Moral Statistics. By Henry
Morse, M. D., Professor of Psychological Medicine, Royal Uni-
versity, Turin. $1.75.

THE FORMATION OF VEGETABLE MOULD, THROUGH THE
ACTION OF WORMS. With Observations on their Habits. By
Cuar_es Darwin, LL. D., F.R.S. With Illustrations. $1.50.

. THE CONCEPTS AND THEORIES OF MODERN PHYSICS. By

J.B. Srautyo. $1.75.

. THE BRAIN AND ITS FUNCTIONS. By J. Luys. $1.50.
. MYTH AND SCIENCE. By Trro Vienour. $1.50.
. DISEASES OF MEMORY: An Essay in the Positive Psychology.

By Tu. Risot, author of ‘ Heredity.”’ $1.50.

. ANTS, BEES, AND WASPS. A Record of Observations of the

Habits of the Social Hymenoptera. By Sir Jonn Lussock, Bart.,
He tiaS:, WC. 1... lia, D., ete. $2.00.

. SCIENCE OF POLITICS. By Suznpon Amos. $1.75.
- ANIMAL INTELLIGENCE. By Grorcr J. Romanes. $1.75.
. MAN BEFORE METALS. By N. Jony, Correspondent of the Insti-

tute. With 148 Illustrations. $1.75.

New York: D. APPLETON & CO., 1, 3, & 5 Bond Street.

4

og

47.
48.

49.

50.

51.

53.

54.

55.

The International Scientific Series.—(Continued.)

THE ORGANS OF SPEECH AND THEIR APPLICATION IN
THE FORMATION OF ARTICULATE SOUNDS. By G. H.

von Meyer, Professor in Ordinary of Anatomy at the University of
Zurich. With 47 Woodcuts. $1.75.

FALLACIES: A View of Logic from the Practical Side. By ALFRrep
Sipewick, B. A., Oxon. $1.75.

ORIGIN OF CULTIVATED PLANTS. By Atpnonsz pE CanpoLie. .
$2.00.

JELLY-FISH, STAR-FISH, AND SEA-URCHINS. Being a Re-
search on Primitive Nervous Systems. By Grorae J. Romanes.
$1.75.

THE COMMON SENSE OF THE EXACT SCIENCES. By the
late Witt1am Kinepon Cuirrorp. $1.50.

PHYSICAL EXPRESSION: Its Modes and Principles. By Francis
Warner, M.D., Assistant Physician, and Lecturer on Botany to the
London Hospital, etc. With 51 Illustrations. $1.75.

. ANTHROPOID APES. By Rosert Harrmann, Professor in the

University of Berlin. With 63 Illustrations. $1.75.

THE MAMMALIA IN THEIR RELATION TO PRIMEVAL
TIMES. By Oscar Scumipr. $1.50.

COMPARATIVE LITERATURE. By Hutrcurson Macavray Pos-
neTT, M. A., LL. D., F. L.8., Barrister-at-Law ; Professor of Clas-
sics and English Literature, University College, Auckland, New
Zealand, author of ‘‘ The Historical Method,’ ete. $1.75.

EARTHQUAKES AND OTHER EARTH MOVEMENTS. By Jonny
Mine, Professor of Mining and Geology in the Imperial College of
Engineering, Tokio, Japan. With 38 Figures.

New York: D. APPLETON & CO., 1, 3, & 5 Bond Street.

HARTHQUAKES >

OTHER EARTH MOVEMENTS

BY
JOHN MILNE

PROFESSOR OF MINING AND GEOLOGY IN THE IMPERIAL COLLEGE OF ENGINEERING,
TOKIO, JAPAN

WITH THIRTY-EIGHT FIGURES

NEW YORK

DD. APPLETON AND COMPANY
1, 8, anv 5 BOND STREET

1886

PREFPAGE.

OE

In the following pages it has been my object to give a
systematic account of various Earth Movements.

These comprise Farthquakes, or the sudden violent
movements of the ground; Harth Tremors, or minute move-
ments which escape our attention by the smallness of their
amplitude; Harth Pulsations, or movements which are
overlooked on account of the length of their period; and
lastly, Harth Oscillations, or movements of long period
and large amplitude which attract so much attention
from their geological importance.

It is difficult to separate these Earth Movements from
each other, because they are phenomena which only
differ in degree, and which are intimately associated in
their occurrence and in their origin.

Because Earthquakes are phenomena which have at-
tracted a universal attention since the earliest times, and
about them so many observations have been made, they
are treated of at considerable length.

As very much of what might be said about the other
Earth Movements is common to what is said about Earth-

al PREFACE.

quakes, it has been possible to make the description of
these phenomena comparatively short.

The scheme which has been adopted will be under-
stood from the following table :—

I, EARTHQUAKES,

—"

. Introduction.
2. Seismometry.
(a) Theoretically.
(6) As deduced from experiments.
(c) As deduced from actual Earth-
quakes.
((a) On land.
* ((2) In the ocean.

5. Determination of Earthquake origins.

3. Earthquake Motion .

4. Earthquake Effects

(a) In space.
(b) In time (geological time, his-
torical time, annual, seasonal,

6. Distribution of ee a |
| diurnal, &c.)

7. Cause of Earthquakes.
8. Earthquake prediction and warning.

TI. EARTH TREMORS.

JJI. EARTH PULSATIONS.
1V. EARTH OSCILLATIONS.

In some instances the grouping of phenomena according
to the above scheme may be found inaccurate, as, for
example, in the chapters referring to the effects and causes
of Earthquakes.

This arises from the fact that the relationship between
Earthquakes and other Earth phenomena are not well
understood. Thus the sudden elevation of a coast line
and an accompanying earthquake may be related, either
as effect and cause, or vice versa, or they may both be the
effect of a third phenomenon.

PREFACE. Vil

Much of what is said respecting Earthquake motion
will show how little accurate knowledge we have about
these disturbances. Had I been writing in England, and,
therefore, been in a position to make references to libraries
and persons who are authorities on subjects connected
with Seismology, the following pages might have been
made more complete, and inaccuracies avoided. A large
proportion of the material embodied in the following
pages is founded on experiments and observations made
during an eight years’ residence in Japan, where I have
had the opportunity of recording an earthquake every
week.

The writer to whom I am chiefly indebted is Mr.
Robert Mallet. Not being in a position to refer to
original memoirs, I have drawn many illustrations from
the works of Professor Karl Fuchs and M.S. di Rossi.
These, and other writers to whom reference has been
made, are given in an appendix.

For seeing these pages through the press, my thanks
are due to Mr. Thomas Gray, who, when residing in Japan,
did so much for the advancement of observational Seis-
mology.

For advice and assistance in devising experiments, I
tender my thanks to my colleagues, Professor T. Alexander,
Mr. T. Fujioka, and to my late colleague, Professor John
Perry.

For assistance in the actual observation of Earth-
quakes, I have to thank my friends in various parts of
Japan, especially Mr. J. Bissett and Mr. T. Talbot, of
Yokohama. For assistance in obtaining information from

Viil PREFACE,

Italian sources I have to thank Dr. F. Du Bois, from
German sources Professor C. Netto, and from Japanese
sources Mr. B. H. Chamberlain. For help in carrying
out experiments, I am indebted to the liberality of the
British Association, the Geological Society of London, the
Meteorological and Telegraph departments of Japan, and
to the officers of my own institution, the Imperial College

of Engineering.

And, lastly, I offer my sincere thanks to those gentle-
men who have taken part in the establishment and
working of the Seismological Society of Japan, and to my —
publishers, whose liberality has enabled me to place the
labours of residents in the Far East before the European
public.

JoHN MILNE.

TOKIO, JAPAN; June 30, 1883

CO her iN Ts,

CHAPTER IL.

INTRODUCTION.

PAGE
Relationship of man to nature—The aspect of a country is de-

pendent on geological phenomena—LHarthquakes an important
geological phenomenon—Relationship of seismology to the
sciences and arts—EHarth movements other than earthquakes—
Seismological literature—( Writings of Perrey, Mallet, Eastern
writings, the Philosophical Transactions of the Royal Society,
the ‘Gentleman’s Magazine,’ the Bible, Herodotus, Pliny, Hop-
kins, Von Hoff, Humboldt, Schmidt, Seebach, Lasaulx, Fuchs,
Palmieri, Bertelli, Seismological Society of Japan)—Seismo-
logical terminology . ° , . : : “ a |

CHAPTER II.

SEISMOMETRY.

Nature of earthquake vibrations—Many instruments called seismo-
meters only seismoscopes— Eastern seismoscopes, columns, pro-
jection seismometers+ Vessels filled with liquid—Palmieri’s
mercury tubes—The ship seismoscope—The cacciatore—Pendu-
lum instruments of Kreil, Wagner, Ewing, and Gray—Bracket
seismographs—West’s parallel motion instruament—Gray’s con-
ical pendulums, rolling spheres, and cylinders—Verbeck’s ball
and plate seismograph—The principle of Perry and Ayrton—
Vertical motion instruments—Record receiver—Time- recording
apparatus—The Gray and Milne seismograph ., . pee c.. aualtey

A CONTENTS.

CHAPTER III.

EARTHQUAKE MOTION DISCUSSED THEORETICALLY.
PAGE

Ideas of the ancients (the views of Travagini, Hooke, Woodward,
Stuckeley, Mitchell, Young, Mallet)—Nature of elastic waves
and vibrations—Possible causes of disturbance in the earth’s
crust—The time of vibration of an earth particle—Velocity and
acceleration of a particle—Propagation of a disturbance as de-
termined by experiments upon the elastic moduli of rocks—The
intensity of an earthquake—Area of greatest overturning mo-
ment— Earthquake waves— Reflexion, refraction, and interference
of waves—Radiation of a disturbance A : . e « Al

CHAPTER IV.
EARTHQUAKE MOTION AS DEDUCED FROM EXPERIMENT.

Experiments with falling weights—Experiments with explosives
—Results obtained from experiments—Relative motion of two
adjacent points—The effect of hills and excavations upon the
propagation of vibrations—The intensity of artificial disturb-
ances— Velocity with which earth vibrations are propagated—
Experiments of Mallet—Experiments of Abbot—Experiments
in Japan—-Mallet’s results—Abbot’s results—Results obtained
in Japan . . . - . . . ° ° e . On

CHAPTER Y.

EARTHQUAKE MOTION AS DEDUCED FROM OBSERVATION
ON EARTHQUAKES.

Result of feelings—The direction of motion—Instruments as in-
dicators of direction—Duration of an earthquake—Period of
vibration— The amplitude of earth movements—Side of greatest
motion—Intensity of earthquakes—Velocity and acceleration of
an earth particle—Absolute intensity of an earthquake— Radi-
ation of an earthquake—Velocity of propagation < ° « 6@

CONTENTS. xl

CHAPTER VI.

EFFECTS PRODUCED BY EARTHQUAKES UPON BUILDINGS.
PAGE

The destruction of buildings is not irregular—Cracks in buildings—-
Buildings in Tokio—Relation of destruction to earthquake
motion—Measurement of relative motion of parts of a building
shaken by an earthquake—Prevention of cracks— Direction of
cracks--The pitch of roofs—Relative pcsition of openings in a
wall—The last house in a row—The swing of buildings—Prin-
ciple of relative vibrational periods . 2 : ° ° « 96

CHAPTER, VII.
EFFECTS PRODUCED UPON BUILDINGS (continued).

Types of buildings used in earthquake countries—In Japan, in Italy,
in South America, in Caraccas—Typical houses for earthquake
countries— Destruction due to the nature of underlying rocks—
The swing of mountains— Want of support on the face of hills—
Earthquake shadows—Destruction due to the interference of
waves—Earthquake bridges— Examples of earthquake effects—

k Protection of buildings—General conclusions - : : 122
CHAPTER VIII.

u

vs

E EFFECTS OF EARTHQUAKES ON LAND.

. 1. Cracks and fissures—Materials discharged from fissures—Ex-

be planation of fissure phenomena. 2. Disturbances in lakes, rivers,

i springs, wells, fumaroles, &c.—Explanation of these latter phe-

a

nomena. 3. Permanent displacement of ground—On coast lines
—Level tracts—Among mountains—Explanation of these move-
ments , ° ° : : . : . . ° ° - 146

=o

CHAPTER IX.

DISTURBANCES IN THE OCIAN,

Sea vibrations—Cause of vibratory blows—Sca waves: preceding
earthquakes; succeeding earthquakes—Magnitude of waves—

xi CONTENTS.

PAGE
Waves as recorded in countries distant from the origin-—Records
on tide gauges—Waves without earthquakes-—Cause of waves—
Phenomena difficult of explanation—Velocity of propagation—
Depth of the ocean—Examples of calculations—Comparison of
velocities of earthquake waves with velocities which ought to
exist from the known depth of the ocean , - . : . 163

CHAPTER X.
DETERMINATION OF EARTHQUAKE ORIGINS.

Approximate determination of an origin—Earthquake-hunting in
Japan— Determinations by direction of motion—Direction in-
| dicated by destruction of buildings—Direction determined by —
: rotation—Cause of rotation—The use of time observations—
Errors in such observations —Origin determined by the method
of straight lines—The method of circles, the method of hyper-
bolas, the method of co-ordinates—Haughton s method— Differ-
ence in time between sound, earth, and water waves-—Method
of Seebach . - : : : 5 . ° . ° . 187

CHAPTER XI.
THE DEPTH OF AN EARTHQUAKE CENTRUM.

The depth of an earthquake centrum-—Greatest possible depth of
an earthquake—Form of the focal cavity . ° ° ° . 213

CHAPTER XII.

DISTRIBUTION OF EARTHQUAKES IN SPACH AND TIME.

General distribution of earthquakes—Occurrence along lines—Hx-
amples of distribution—Italian earthquake of 1873—In Tokio—
Extension of earthquake boundaries—Seismic energy in relation
to geological time; to historical time—Relative frequency of
earthquakes—Synchronism of earthquakes—Secondary earth-
quakes . ° . * . : ; ° : « + «226

CONTENTS. Xiil

CHAPTER XIIL

PAGE
DISTRIBUTION OF EARTHQUAKES IN TIME (confinued) . 234

CHAPTER XIV.

DISTRIBUTION OF EARTHQUAKES IN TIME (continued).

The occurrence of earthquakes in relation to the position of the
heavenly bodies—-Earthquakes and the moon—Earthquakes and
the sun; and the seasons; the months—Planets and meteors—
Hours at which earthquakes are frequent—Earthquakes and
sun spots—Harthquakes and the aurora . : a : . 250

CHAPTER XV.

BAROMETRICAL FLUCTUATIONS AND EARTHQUAKES—
FLUCTUATIONS IN TEMPERATURE AND EARTHQUAKES. 266.

CHAPTER XVI.
RELATION OF SEISMIC TO VOLCANIC PHENOMENA.

Want of synchronism between earthquakes and volcanic eruptions—
Synchronism between earthquakes and volcanic eruptions—
Conclusion . : : ° . : p : ° ° « 270

CHAPTER XVII.

THE CAUSE OF EARTHQUAKES.

Modern views respecting the cause of earthquakes—Earthquakes
due to faulting—To explosions of steam—To volcanic eviscera-
tion—To chemical degradation—Attractive influence of the
heavenly bodies—The effect of oceanic tides—Variation in at-
mospheric pressure—Fluctuation in temperature—Winds and
earthquakes— Rain and earthquakes—Conclusion . : « 217

XIV CONTENTS,

CHAPTER XVIII.

PREDICTION OF EARTIQUAKES.
PAGE
General nature of predictions—Prediction by the observation of un-
usual phenomena (Alteration in the appearance and taste of
springs; underground noises; preliminary tremors; Harthquake
prophets—warnings furnished by animals, &c.)—Harthquake
warning . ’ : 4 : . : ° ° ° » 207

CHAPTER XIX.

EARTH TREMORS.

Artificially produced tremors—Observations of Kater, Denman, -
Airy, Palmer, Paul—Natural tremors—Observations of Zollner,
M. d’Abbadie, G. H. and H. Darwin—Experiments in Japan—
With seismoscopes, microphones, pendulums—Work in Italy—
Bertelli, Count Malvasia, M. S. di Rossi—Instruments employed
in Italy—Tromometers, microseismographs, microphones—Re-
sultsobtained in Italy—In Japan—Cause of microseismicmotion 306

CHAPTER XX.
EARTH PULSATIONS,

Definition of an earth pulsation—Indications of pendulums—Indi-
cations of levels—Other phenomena indicating the existence of
earth pulsations— Disturbances in lakes and oceans—Phenomena
resultant on earth pulsations—Cause of earth pulsations . - 326

CHAPTER XXI.
EARTH OSCILLATIONS.

Evidences of oscillation—Hxamples of oscillation—Temple of Ju-
piter Serapis—Observations of Darwin—Causes of oscillation . 344

APPENDIX e > RB) ® a e . e ° e e 349

INDEX e 4 e ° @ , e ’ e e 0 ¢ e 359

HARTHQUAKHES.

CHAPTER I.
INTRODUCTION.

Relationship of man to nature—The aspect of a country is dependent
on geological phenomena—Earthquakes an important geological
phenomenon—Relationship of seismology to the sciences and arts—
Earth movements other than earthquakes—Seismological literature
—(Writings of Perrey, Mallet, Eastern writings, the Philosophical
Transactions of the Royal Society, the ‘Gentleman’s Magazine,’ the
Bible, Herodotus, Pliny, Hopkins, Von Hoff, Humboldt, Schmidt,
Seebach, Lasaulx, Fuchs, Palmieri, Bertelli, Seismological Society
of Japan)—Seismological terminology.

In bygone superstitious times lightning and thunder were
regarded as supernatural visitations. But as these phe-
nomena became better understood, and men learned how
to avoid their destructive power, the superstition was
gradually dispelled. Thus it is with Earthquakes: the
more clearly they are understood, the more confident in
the universality of law will man become, and the more
will his mental condition be advanced.

In his ‘History of Civilisation in England,’ Buckle
has laid considerable stress upon the manner in which
earthquakes, volcanoes, and other of the more terrible
forms iu which the workings of nature reveal themselves

2 . EARTHQUAKES,

to us, have exerted an influence upon the imagination
and understanding; and just as a sudden fright may
affect the nerves of a child for the remainder of its life,
we have in the annals of seismology records which indi-
cate that earthquakes have not been without a serious
influence upon the mental condition of whole communi-
ties. 3

To a geologist there are perhaps no phenomena in
nature more interesting than earthquakes, the study of
which is called Seismology. Coming, as shocks often will,
from a region of volcanoes, the study of these disturbances
may enable us to understand something about the nature
and working of a volcano. As an earthquake-wave travels
along from strata to strata, if we study its reflections and
changing velocity in transit, we may often be led to the
discovery of certain rocky structures buried deep beneath
our view, about which, without the help of such waves, it
would be hopeless ever to attain any knowledge.

By studying the propagation of earthquake-waves the
physicist is enabled to confirm his speculations respecting
the transmission of disturbances in elastic media. For
the physicist earthquakes are gigantic experiments which
tell him the elastic moduli of rocks as they exist in
nature, and when properly interpreted may lead him to

_ the proper comprehension of many ill-understood pheno-

mena. It is not impossible that seismological investiga-
tion may teach us something about the earth’s magnetism,
and the connection between earthquakes and the ‘ earth
currents’ which appear in our telegraph wires. These
and numerous other kindred problems fall within the
domain of the physicist.

It is of interest to the meteorologist to know the con-
nections which probably exist between earthquakes and
the fluctuations of the barometer, the changes of the

INTRODUCTION. 3

thermometer, the quantity of rainfall, and like phenomena
to which he devotes his attention.

Next we may turn to the more practical aims of seis-
mology and ask ourselves what are the effects of earth-
quakes upon buildings, and how, in earthquake-shaken
countries, the buildings are to be made to withstand them.
Here we are face to face with problems which demand
the attention of engineers and builders. To attain what
we desire, observation, common sense, and subtle reason-
ing must be brought to bear upon this subject.

In the investigation of the principle on which earth-
quake instruments make their records, in the analysis of
the results they give, in problems connected with astro-
nomy, with physics, and with construction, seismology
offers to the mathematician new fields for investiga-
tion.

A study of the effects which earthquakes produce on
the lower animals will not fail to interest the student of
natural history.

A study like seismology, which leads us to a more
complete knowledge of earth-heat and its workings, is to
be regarded as one of the corner-stones of geology. The
science of seismology invites the co-operation of workers
and thinkers in almost every department of natural
science.

We have already referred to the influence exerted by
earthquakes over the human mind. How to predict
earthquakes, and how to escape from their dangers, are
problems which, if they can be solved, are of extreme
interest to the world at large.

In addition to the sudden and violent movements
which we call earthquakes, the seismologist has to in-
vestigate the smaller motions which we call earth-tremors.
From observations which have been made of late years,

4 EARTHQUAKES,

it would appear that the ground on which we dwell is
incessantly in a state of tremulous motion.

A further subject of investigation which is before the
seismologist is the experimental verification of the exist-
ence of what may be called ‘earth-pulsations.’ These
are motions which mathematical physicists affirmed the
existence of, but which, in consequence of the slowness of
their period, have hitherto escaped observation.

The oscillations, or slow changes in the relative posi-
tions of land and sea, might also be included; but this
has already been taken up as a separate branch of geology.

These four classes of movements are no doubt inter-
dependent, and seismology in the widest sense might
conveniently be employed to include them all. In suc-
ceeding chapters we will endeavour to indicate how far
the first three of these branches have been prosecuted,
and to point out that which remains to be accomplished.
It is difficult, however, to form a just estimate of the
amount of seismological work which has been done, in con-
sequence of the scattered and uncertain nature of many
of the records. Seismology, as a science, originated late,
chiefly owing to the facts that centres of civilisation are
seldom in the most disturbed regions, and that earthquake-
shaken countries are widely separated from each other.

As every portion of the habitable globe appears to
have been shaken more or less by earthquakes, and as
these phenomena are so terrible in their nature, we can
readily understand why seismological literature is ex-
tensive. In the annals of almost every country which has
a written history, references are made to seismic disturb-
ances.

An idea of the attention which earthquakes have re-—
ceived inay be gathered from the fact that Professor Alexis
Perrey, of Dijon, who has published some sixty memoirs

INTRODUCTION. ee

on this subject, gave, in 1856, a catalogue of 1,837 works
devoted to seismology.! In 1858 Mr. Robert Mallet
published in the Reports of the British Association a list
of several hundred works relating to earthquakes. Sixty-
five of these works are to be found in the British Museum.
So far as literature is concerned, earthquakes have re-
ceived as much attention in the East asin the West. In
China there are many works treating on earthquakes, and
the attention which these phenomena received may be
judged of from the fact that in a.D. 136 the Government
appointed a commission to inquire into the subject.
Even the isolated empire of Japan can boast of at least
sixty-five works on earthquakes, seven of which are earth-
quake calendars, and twenty-three earthquake mono-
graphs.” Besides those treating especially of earthquakes,
there are innumerable references to such disturbances in
various histories, in the transactions of learned societies,
and in periodicals. To attempt to give a complete cata-
logue of even the books which have been written would
be to enter on a work of compilation which would occupy
many years, and could never be satisfactorily finished.

In the ‘ Philosophical Transactions of the Royal Society,’
which were issued in the eighteenth century, there are about
one hundred and eighty separate communications on earth-
quakes ; and in the ‘Gentleman’s Magazine’ for 1755 there
are no less than fifty notes and articles on the same sub-
ject. The great interest shown in earthquakes about the
years 1750-60 in England, was chiefly due to the terrible
calamity which overtook Lisbon in 1755, and to the fact
that about this time several shocks were experienced in
various parts of the British Islands. In 1750, which may

1 Mémoires de VAcadémie Imp. de Dijon, vols. xiv. and xv., 2nd
Series, 1855-56.
* Trans. Seis. Soc. of Japan, vol. iii. p 65.

6 EARTHQUAKES,

be described as the earthquake year of Britain, ‘a shock
was felt in Surrey on March 14; on the 18th of the
same month the whole of the south-west of England was
disturbed. On April 2, Chester was shaken; on June 7,
Norwich was disturbed; on August 23, the inhabitants
of Lancashire were alarmed; and on September 30 ludi-
crous and alarming scenes occurred in consequence of
a shock having been felt during the hours of Divine
service, causing the congregations to hurry into the open
air’! As might be expected, these occurrences gave rise
to many articles and notes directing attention to the
subject of earthquakes.

Seismic literature has not, however, at all times been
a measure of seismic activity: thus, in Japan, the earth-
quake records for the twelfth and sixteenth centuries
scarcely mention any shocks. At first sight it might be
imagined that this was owing to an absence of earthquakes;
but it is sufficiently accounted for by the fact that at that
time the country was torn with civil war, and matters
more urgent than the recording of natural phenomena
engaged the attention of the inhabitants. Professor Rock-
wood, who has given so much attention to seismic dis-
turbances in America, tells us that during the recent
contest between Chili and Peru a similar intermission is
observable. We see, therefore, that an absence of records
does not necessarily imply an absence of the phenomena
to be recorded.

Perhaps the earliest existing records of earthquakes
are those which occur in the Bible. The first of these,
which we are told occurred in Palestine, was in the reign
of Ahab (8.c. 918-897).?. One of the most terrible earth-
quakes mentioned in the Bible is that which took place ~
in the days of Uzziah, king of Judah (B.c. 811-759),

1 Gentleman's Magazine, 1753. ? Tl Kings xix iy 2.

INTRODUCTION. 7

whicn shook the ground and rent the Temple. The awful
character of this, and the deep impression produced on
men’s minds, may be learned from the fact that the time
of its occurrence was subsequently used as an epoch from
which to reckon dates.

The writings of Herodotus, Pliny, Livy, &., «&ce.,
show the interest which earthquakes attracted in early
ages. These writers chiefly devoted themselves to refer-
ences and descriptions of disastrous shocks, and to theories
respecting the cause of earthquakes.

The greater portion of the Japanese notices of earth-
quakes is simply a series of anecdotes of events which
took place at the time of these disasters. We also find
references to superstitious beliefs, curious occurrences,
and the apparent connection between earthquake dis-
turbances and other natural phenomena. In these respects
the literature of the East closely resembles that of the
West. The earthquake calendars of the East, however,
form a class of books which can hardly be said to find their
parallel in Europe;! while, on the other hand, the latter
possesses types of books and pamphlets which do not
appear to have a paralle] elsewhere. These are the more
or less theological works—‘ Moral Reflections on FEarth-
quakes,’ ‘Sermons’ which have been preached on earth-
quakes, ‘Prayers’ which have been appointed to be
Read? ©;

Speaking generally, it may be said that the writings
of the ancients, and those of the Middle Ages, down to
the commencement of the nineteenth century, tended to
-the propagation of superstition and to theories based on

1‘ Notes on the Great Earthquake of Japan.’ J. Milne, Trans. Seis.
Soc. of Japan, vol. iii.

2 See Mallet’s List of Works on Earthquakes, Report of the British
Association, 1858, p. 107,

2

8 EARTHQUAKES.

speculations with few and imperfect facts for their
foundation.

Among the efforts which have been made in modern
times to raise seismology to a higher level, is that of
Professor Perrey, of Dijon, who commenced in 1840 a
series of extensive catalogues embracing the earthquakes
of the world. These catalogues enabled Perrey, and
‘subsequently Mallet in his reports to the British Asso-
ciation, to discuss the periodicity of earthquakes, with
reference to the seasons and to other phenomena, in a
more general manner than it had been possible for pre-
vious workers to accomplish. The facts thus accumulated
also enabled Mallet to discuss earthquakes in general,
and the various phenomena which they present were sifted
and classified for inspection. Another great impetus
which observational seismology received was Mr. Mallet’s
report upon the Neapolitan earthquake of 1857, in which
new methods of seismic investigation were put forth.
These have formed the working tools of many subsequent
observers, and by them, as well as by his experiments
on artificially produced disturbances, Mallet finally drew
the study of earthquakes from the realms of speculation
by showing that they, like other natural phenomena,
were capable of being understood and investigated.

In addition to Perrey and Mallet, the nineteenth
century has produced many writers who have taken a
considerable share in the advancement of seismology.
There are the catalogues of Von Hoff, the observations of
Humboldt, the theoretical investigations of Hopkins, the
monographs of Schmidt, Seebach, Lasaulx, and others;
the books of Fuchs, Credner, Vogt, Volger; the records
and observations of Palmieri, Bertelli, Rossi, and other
Italian observers. To these, which are only a few out of
a long list of names, may be added the publications of the

INTRODUCTION. g

Commission appointed for the observation of earthquakes
by the Natural History Society of Switzerland, and the
volumes which have been published by the Seismological
Society of Japan.

Before concluding this chapter it will be well to
define a few of the more ordinary terms which are used
in describing earthquake phenomena. It may he ob-
served that the English word earthquake, the German
erdbeben, the French tremblement de terre, the Spanish
terremoto, the Japanese jishin &c., all mean, when
literally translated, earth-shaking, and are popularly
understood to mean a sudden and more or less violent
disturbance.

Seismology (cecpds an earthquake, Aoyos a dis-
course) in its simplest sense means the study of earth-
quakes. To be consistent with a Greek basis for seis-
mological terminology, some writers have thrown aside
the familiar expression ‘ earthquake,’ and substituted the
awkward word ‘seism.’ |

The source from which an earthquake originates is
called the ‘ origin,’ ‘ focal cavity,’ or ‘centrum.’

The point or area on the surface of the ground above
the origin is called the ‘epicentrum.’ The line joining
the centrum and epicentrum is called the ‘seismic
vertical.’

The radial lines along which an earthquake may be
propagated from the centrum are called ‘ wave-paths.’

The angle which a wave-path, where it reaches the
surface of the earth, makes with that surface is called the
‘angle of emergence’ of the wave. This angle is usually
denoted by the letter e.

As the result of a simple explosion at a point in
a homogeneous medium, we ought, theoretically, to ob-
tain at points on the surface of the medium equidistant

10 EARTHQUAKES,

from the epicentrum, equal mechanical effects. These
points will lie on circles called ‘isoseismic’ or ‘ coseismic’
circles. ‘The area included between two such circles is an
‘isoseismic area.’ In nature, however, isoseismic lines
are seldom circles. Elliptical or irregular curves are the
common forms.

The isoseismic area in which the greatest disturbance
has taken place is called the ‘ meizoseismic area.’ Seebach
calls the lines enclosing this area ‘ pleistoseists.’

These last-mentioned lines are wholly due to Mallet
and Seebach.

Many words are used to distinguish different kinds of
earthquakes from each other. All of these appear to be
very indefinite and to depend upon the observer's feelings,
which, in turn, depend upon his nervous temperament
and his situation. |

In South America.small earthquakes, consisting of a
series of rapidly recurring vibratory movements not suffi-
ciently powerful to create damage, are spoken of as trem-
belores.

The terremotos of South America are earthquakes
of a destructive nature, in which distinct shocks are per-
ceptible. It may be observed that shocks which at one
place would be described as terremoto would at another
and more distant place probably be described as trembe-
lores.

The succussatore are the shocks where there is con-
siderable vertical motion. The terrible shock of Reo-
bamba (February 4, 1797), which is said to have thrown’
corpses from their graves to a height of 100 feet, was an
earthquake of this order. |

The vorticossi are “boats which have a igi or
rotatory motion.

Another method of describing earthquakes would be

INTRODUCTION, bal:

to refer to instrumental records. When the vibrations of
the ground have only been along the line joining the
observer and the epicentrum, the disturbance might be
ealled ‘ euthutropic.’ <A disturbance in which the promi-
nent movements are transverse to the above direction
might be called ‘ diagonic.’ If motions in both of these
directions occur in the records, the shock might be said
to be ‘ diastrophic.’- If there be much vertical movement,
the shock might be said to be ‘anaseismic.’? Some disturb-
ances could only be described by using two or three of
these terms,

12 EARTHQUAKES,

CHAPTER II...
SEISMOMETRY.

Nature of earthquake vibrations—Many instruments called seismo-
meters only seismoscopes—Eastern seismoscopes, columns, projec-
tion seismometers—Vessels filled with liquid—Palmieri’s mercury
tubes—The ship seismoscope-——The cacciatore—Pendulum instru-
ments of Kreil, Wagner, Ewing, and Gray—Bracket seismographs—
West’s parallel motion instrument—Gray’s conical pendulums,
rolling spheres, and cylinders—Verbeck'’s ball and plate seismograph
—The prin.iple of Perry and Ayrton—Vertical motion instruments
—Record receivers — Time-recording apparatus — The Gray and
Milne seismograph,

BEFORE we discuss the nature of earthquake motion, the
determination of which has been the aim of modern seis-
mological investigation, the reader will naturally look for
an account of the various instruments which have been
employed for recording such disturbances. <A description
of the earthquake machines which have been used even in
Japan would form a bulky volume. All that we can do,
therefore, is to describe briefly the more prominent fea-
tures of a few of the more important of these instruments.
In order that the relative merits of these may be better
understood, we may state generally that modern research
has shown atypical earthquake to consist of a series of
small tremors succeeded by a shock, or series of shocks,
separated by more or less irregular vibrations of the
ground. The vibrations are often both irregular in period

SEISMOMETRY. 13

and in amplitude, and they have a duration of from a few
seconds to several minutes. We will illustrate the records
of actual earthquakes in a future chapter, but in the
meantime the idea that an earthquake consists of a single
shock must be dismissed from the imagination.

To construct an instrument which at the time of an
earthquake shall move and leave a record of its motion,
there is but little difficulty. Contrivances of this order
are called seismoscopes. If, however, we wish to know
the period, extent, and direction of each of the vibrations
which constitutes an earthquake, we have considerable
difficulty. Instruments which will in this way measure
or write down the earth’s motions are called setsmometers
or seismographs. |

Many of the elaborate instruments supplemented with
electro-magnetic and clockwork arrangements are, when
we examine them, nothing more than elaborate seismo-
scopes which have been erroneously termed seismographs.

The only approximations to true seismographs which
have yet been invented are without doubt those which
during the past few years have been used in Japan. It
would be a somewhat arbitrary proceeding, however, to
classify the different instruments as seismoscopes, seismo-
meters, and seismographs, as the character of the record
given by certain instruments is sometimes only seismo-
scopic, whilst at other times it is seismometric, depending
on the nature of the disturbance. Many instruments, for
instance, would record with considerable accuracy a single
sudden movement, but would give no reliable information
regarding a continued shaking.

Eastern Seismoscopes.—The earliest seismoscope of
which we find any historical record is one which owes its
origin to a Chinese called Choko. It was invented in the
year A.D. 136. A description is given in the Chinese

14 EARTHQUAKES.

history called ‘Gokanjo,’ and the translation of this de-
scription runs as follows :— of

‘In the first year of Yoka, A.D. 136, a Chinese called
Chéko invented the seismometer shown in the accompany-
ing drawing. This instrument consists of a spherically
formed copper vessel, the diameter of which is eight feet.
It is covered at its top, and in form resembles a wine-

WY

=F

RY

‘\

:

bottle. Its outer part is ornamented by the figures of
different kinds of birds and animals, and old peculiar-
looking letters. In the inner part of this instrument a
column is so suspended that it can move in eight direc-
tions. Also, in the inside of the bottle, there is an
arrangement by which some record of an earthquake is
made according to the movement of the pillar. On the
outside of the bottle there are eight dragon heads, each

SEISMOMETRY. 15.

of which holds a hall in its mouth. Underneath these
heads there are eight frogs so placed that they appear to
watch the dragon’s face, so that they are ready to receive
the ball if it should be dropped. All the arrangements
which cause the pillar to knock the ball out of the dragon’s
mouth are well hidden in the bottle.’

‘When an earthquake occurs, and the bottle is shaken,
the dragon instantly drops the ball, and the frog which
receives it vibrates vigorously ; any one watching this in-
strument can easily observe earthquakes.’

With this arrangement, although one dragon may
drop a ball, it is not necessary for the other seven dragons
to drop their balls unless the movement has been in all
directions; thus we can easily tell the direction of an
earthquake.

‘Once upon a time a dragon dropped its ball without
any earthquake being observed, and the people there-
fore thought the instrument of no use, but after two
or three days a notice came saying that an earthquake
had taken place at Rosei. Hearing of this, those who
doubted the use of this instrument began to believe
in it again. After this ingenious instrument had been
invented by Choko, the Chinese Government wisely
appointed a secretary to make observations on earth- |
quakes.’

Not only is this instrument of interest on account of
its antiquity, but it is also of interest on account of the
close resemblance it bears to many of the instruments of
modern times. :

Another earthquake instrument also of Eastern origin
is the magnetic seismoscope of Japan.

On the night of the destructive earthquake of 1855,
which devastated a great portion of Tokio, the owner of a
spectacle shop in Asakusa observed that a magnet dropped

16 EARTHQUAKES,

some old iron nails and keys which had been attached to.
it. From this occurrence the owner thought that the
magnet had, in consequence of its age, lost its powers.
About two hours afterwards, however, the great earth-
quake took place, after which the magnet was observed to
have regained its powers. This occurrence led to the
construction of the seismoscope, which is illustrated in a
book called the ‘ Ansei-Kembun-Roku,’ or a description
of the earthquake of 1855, and examples of the instru-
ment are still to be seen in Tokio. These instruments
consist of a piece of magnetic iron ore, which holds up a
piece of iron likeanail. This nail is connected, by means
of a string, with a train of clockwork communicating with
analarum. If the nail falls a catch is released and the
clockwork set in motion, and warning given by the ring-
ing of a bell. It does not appear that this instrument
has ever acted with success.

Columns.—One of the commonest forms of seismo-
scope, and one which has been very widely used, consists
of a round column of wood, metal, or other suitable
material, placed, with its axis vertical, on a level plane,
and surrounded by some soft material such as loose sand
to prevent it rolling should it be overturned. The fall
of such a column indicates that a shaking or shock has
taken place. Attempts have been made by using a
number of columns of different sizes to make these in-
dications seismometric, but they seldom give reliable
information either as to intensity or direction of shock.
The indications as to intensity are vitiated by the fact
that a long-continued gentle shaking may overturn a
column which would stand a very considerable sudden
shock, while the directions in which a number of columns
fall seldom agree owing to the rotational motion imparted —
to them bythe shaking. Besides, the direction of motion

SEISMOMETRY. 17

of the earthquake seldom remains in the same azimuth
throughout the whole disturbance.

‘An extremely delicate, and at the same time simple
form of seismoscope may be made by propping up strips
of glass, pins, or other easily overturned bodies against
suitably placed supports. In this way bodies may be
arranged, which, although they can only fall in one direc-
tion, nevertheless fall with far less motion than is neces-
sary to overturn any column which will stand without
lateral support.

Projection Seismometers.—Closely related to the seis-
moscopes and seismometers which depend on the overturn-
ing of bodies. Mallet has described two sets of apparatus
whose indications depend on the distance to which a body
is projected. In one of these, which consisted of two
similar parts arranged at right angles, two metal balls
rest one on each side of a stop at the lower part of two
inclined \_/ like troughs. In this position each of the
balls completes an electric circuit. By a shock the balis
are projected or rolled up the troughs, and the height to
which they rise is recorded by a corresponding interval in
the break of the circuits. The vertical component of the
motion is measured by the compression of a spring which
carries the table on which this arrangement rests. In the
second apparatus two balls are successively projected, one
by the forward swing, and the other by the backward
swing of the shock. Attached to them are loose wires
forming terminals of the circuits. They are caught in a
bed of wet sand in a metal trough forming the other end
of the circuit. The throw of the balls as measured in
the sand, and the difference of time between their suc-
cessive projections as indicated by special contrivances
connected with the closing of the circuits, enables the
observer to calculate the direction of the wave of shock,

18 EARTHQUAKES.

its velocity, and other elements connected with the dis-
turbance. It will be observed that the design of this
apparatus assumes the earthquake to consist of a distinct
isolated shock.

Oldham, at the end of his account of the Cachar
earthquake of 1869, recommends the use of an instru-
ment based on similar principles. In his instrument
four balls like bullets are placed in notches cut in the
corners of the upper end of a square stake driven into
the ground.

Vessels filled with liquid.—Another form of simple
seismoscope is made by partially filling a vessel with
liquid. The height to which the Jiquid is washed up the
side of the vessel is taken as an indication of the intensity
of the shock, and the line joining the points on which
maximum motion is indicated, is taken as the direction
of the shock. If earthquakes all lasted for the same
length of time, and consisted of vibrations of the same
period, such instruments might be of service. These
instruments have, however, been in use from an early
date. In 1742 we find that bowls of water were used to
measure the earthquakes which in that year alarmed the
inhabitants of Leghorn. About the same time the Rev.
S. Chandler, writing about the shock at Lisbon, tells us
that earthquakes may be measured by means of a sphe-
rical bowl about three or four feet in diameter, the inside
of which, after being dusted over with Barber’s puff, is
filled very gently with water. Mallet, Babbage, and De la

-Béche have recommended the same sort of contrivance,

but, notwithstanding, it has justly been criticised as ‘ridi-
culous and utterly impracticable.’ !
An important portion of Palmieri’s well-known instru-
ment consists of horizontal tubes turned up at the ends
1 Quarterly Review, vol. lxili. p. 61.

SEISMOMETRY. 19

and partially filled with mercury. To magnify the
motion of the mercury, small floats of iron rest on its
surface. These are attached by means of threads to a
pulley provided with indices which move in front of a
scale of degrees. We thus read off the intensity of an
earthquake as so many degrees, which means so many
millimetres of washing up and down of mercury in a tube.
The direction of movement is determined by the azimuth
of the tube which gives the maximum indication, several
tubes being placed in different azimuths.

This form of instrument appears to have been sug-
gested by Mallet, who gives an account of the same in
1846. Inasmuch as the rise and fall of the mercury in
such tubes depend on its depth and on the period of the
earthquake together with its duration, we see that although
the results obtained from a given instrument may give us
means of making approximate comparisons as to the rela-
tive intensity of various earthquakes, it is very far from
yielding any absolute measurement.

Another method which has been employed to magnify
and register the motions of liquid in a vessel has been to
float upon its surface a raft or ship from which a tall mast
projected. By a slight motion of the raft, the top of the
mast vibrated through a considerable range. This motion
of the mast as to direction and extent was then recorded
by suitable contrivances attached to the top of the mast.

A very simple form of liquid seismoscope consists of a
circular trough of wood with notches cut round its side.
This is filled with mercury to the level of the notches.
At the time of an earthquake the maximum quantity of
mercury runs over the notches in the direction of greatest
motion. This instrument, which has long been used in
Italy, is known as a Cacciatore, being named after its
inventor. It is a prominent feature in the collection

20 EARTHQUAKES.

of apparatus forming the well-known seismograph of
Palmieri. |

Pendulum wmstruments. —Mallet speaks of pendulum
selsmoscopes and seismograplis as ‘ the oldest probably of
seismometers long set up in Italy and southern Europe.’
In 1841 we find these being used to record the earthquake
disturbances at Comrie in Scotland.

These instruments may be divided into two classes :
first, those which at the time of the shock are intended to
swing, and thus record the direction of movement ; and
second, those which are supposed to remain at rest and
thus provide ‘ steady points.’

To obtain an absolutely ‘steady point’ at the time of
an earthquake, has been one of the chief aims of all recent
seismological investigations.

With a style or pointer projecting down from the
steady point to a surface which is being moved back-
ward and forward by the earth, such a surface has written
upon it by its own motions a record of the ground to
which it is attached. Conversely, a point projecting up-
wards from the moving earth might be caused to write a
record on the body providing the steady point, which in
the class of instruments now to be referred to is supposed
to be the bob of a pendulum. It is not difficult to get a
pendulum which will swing at the time of a moderately
strong earthquake, but it is somewhat difficult to obtain
one which will not swing at such a time. During the
past few years, pendulums varying between forty feet in
length and carrying bobs of eighty pounds in weight, and
one-eighth of an inch in length, and carrying a gun-shot,
have been experimented with under a great variety of
circumstances. Sometimes the supports of these pendu-
lums have been as rigid as it is possible to make a struc-
ture from brick and mortar, and at other times they have

SEISMOMETRY. 21

intentionally been made loose and flexible. The indices
which wrote the motions of these pendulums have been
as various as the pendulums themselves. A small needle
sliding vertically through two small holes, and resting its
lower end on a surface of smoked glass, has on account of
its small amount of friction been perhaps one of the
favourite forms of recording pointers.

The free pendulums which have been employed, and
which were intended to swing, have been used for two
purposes: first, to determine the direction of motion from
the direction of swing, and second, to see if an approxi-
mation to the period of the earth’s motion could be
obtained by discovering the pendulum amongst a series
of different lengths which was set in most violent motion,
this probably being the one which had its natural period
of swing the most nearly approximating to the period
of the earthquake oscillations.

Inasmuch as all pendulums when swinging have a
tendency to change the plane of their oscillation, and also
as we now know that the direction of motion during an
earthquake is not always constant, the results usually
obtained with these instruments respecting the direction
of the earth’s motion have been unsatisfactory. The
results which were obtained by series of pendulums of
different lengths were, for various reasons, also unsatis-
factory.

Of pendulums intended to providea steady point, from
which the relative motion of a point on the earth’s surface
could be recorded, there has been a great variety. One
of the oldest forms consisted of a pendulum with a style
projecting downwards from the bob so as to touch a bed
of sand. Sometimes a concave surface was placed beneath
the pendulum, on which the record was traced by means
of a pencil. Probably the best form was that in which a

22 EARTHQUAKES,

needle, capable of sliding freely up and down, marked the
relative horizontal motion of the earth and the pendulum
bob on a smoked glass plate.

It generally happens that at the time of a moderately
severe earthquake the whole of these forms of apparatus
are set in motion, due partly to the motion of the point
of support of the pendulum, and partly to ype friction of
the writing point on the plate.

Among these pendulums may be mentioned those of
Cavallieri, Faura, Palmieri, Rossi, and numerous others.
It is possible that the originators of some of these pen-
dulums may have intended that they should record by
swinging. If this is so, then so far as the determination
of the actual nature of earthquake motion is concerned,
they belong to a lower grade of apparatus than that in
which they are here included.

A great improvement in pendulum apparatus is due to
Mr. Thomas Gray of Glasgow, who suggested applying so
much frictional resistance to the free swing of a pen-
dulum that for small displacements it became ‘dead beat.’
By carrying out this suggestion, pendulum instruments
were raised to the position of seismographs. ‘The manner
of applying the friction will be understood from the
following description of a pendulum instrument which is
also provided with an index which gives a magnification
of the motion of the earth.

BBBB is a box 113 em. high and 30 cm. by 18 cm.
square. Inside this box a lead ring R, 17 cm. in diameter
and 3 cm. thick, is suspended as a pendulum from the screw _
s. This screw passes through a small brass plate P P, which
can be moved horizontally over a hole in the top of the
box. These motions in the point of suspension allow the
pendulum to be adjusted.

Projecting over the top of the pendulum there is a

SEISMOMETRY. 23

wooden arm W carrying two sliding pointers H H, resting
on a glass plate placed on the top of the pendulum.
These pointers are for the

e ° e ‘Ss
purpose of giving the fric- Pp p
tional resistance before re- ri ee

ferred to. If this friction B Ep
plate is smoked, the fric-
tion pointers will write
upon it records of large
earthquakes independently
of the records given by the
proper index, which only
gives satisfactory records
in the case of shocks of

fir
ordinary intensity. Cross-
ing the inside of the pen-
dulum R there is a brass
bar perforated with a small
conical hole at M. A stiff wal

wire passes through M and
forms the upper portion of
the index I, the lower por-
tien of which is a thin Rig. 2.

piece of bamboo. Fixed

upon the wire there is a small brass ball which rests on the
upper side of a second brass plate also perforated with a
conical hole, which plate is fixed on the bar 0 0 crossing
the box.

If at the time of an earthquake the upper part of the
index I remains steady at M, then by the motion at 0, the
lower end of the index which carries a sliding needle at
G, will magnify the motion of the earth in the ratios
MoO: 0G. In this instrument 0 G is about 17 cm.

The needle G works upon a piece of smoked glass. In

ae Rees MT kets lf ii AMET ay TUM UI Th

24 EARTHQUAKES.

order to bring the glass into contact with the needle with-
out disturbance, the glass is carried on a strip of wood
K, hinged at the back of the box, and propped up in front
by a loose block of wood y. When y is removed the glass
drops down with kK out of contact with the needle. The
box is carried on bars of wood c Cc, which are fixed to the
ground by the stakes a A.

The great advantage of a pendulum seismograph
working on a stationary plate is, that the record shows
at once whether the direction of motion has been con-
stant, or whether it has been variable. The maximum
extent of motion in various directions is also easily ob-
tained. |

The disadvantage of the instrument is, that at the
time of a large earthquake, owing perhaps to a slight
swing in the pendulum, the records may be unduly
magnified.

On such occasions, however, fairly good records may be
obtained from the friction pointers, provided that the
plates on which they work have been previously smoked.
It might perhaps be well to use two of these instruments,
one having a comparatively high frictional resistance, and
hence ‘dead beat’ for large displacements.

Many attempts have been made to use a pendulum
seismograph in conjunction with a record-receiving sur-
face, which at the time of the earthquake should be kept
in motion by clockwork. In this way it was hoped to
separate the various vibrations of the earthquake, and
thus avoid the greater or less confusion which occurs when
the index of the pendulum writes its backward and for-
ward motion on a stationary plate. Hitherto all attempts
in this direction, in which a single multiplying index
was used, have been unsuccessful because of the moving
plate dragging the index in the direction of its motion for a

SEISMOMETRY. 25

short distance, and then allowing it to fall back towards
its normal position.

In connection with this subject we may mention the
pendulum seismographs of Kreil, Wagener, Ewing, and
Gray.

In the bob of Kreil’s pendulum there was clockwork,
which caused a disc on the axis of the pendulum to con-
tinuously rotate. On this continually revolving surface a
style fixed to the earth traced an unbroken circle. At the
time of an earthquake, by the motion of the style, the
circle was to be broken and lines drawn. The number
and length of these lines were to indicate the length and
intensity of the disturbance.

Gray’s pendulum consisted of a flat heavy dise carrying
on its upper surface a smoked glass plate. This, which
formed the bob of the pendulum, was supported by a
pianoforte steel wire. When set ready to receive an earth-
quake, the wire was twisted and the bob held by a catch so
arranged that at the time of the earthquake the catch
was released, and the bob of the pendulum allowed to turn
slowly by the untwisting of the supporting wire. Resting
on the surface of this rotating dise were two multiplying
indices arranged to write the earth’s motions as two com-
ponents.

In the instruments of Wagener and Ewing, the clock-
work and moving surface do not form part of the pen-
dulum, but rest independently on a support rigidly
attached to the earth. In Wagener’s instrument one index
only is used, while in Ewing’s two are used for writing
the record of the motion.

A difficulty which is apparent in all pendulum
machines is that when the hob of such a pendulum is de-
flected it tends to fall back to its normal position. To
make a pendulum perfect it therefore requires some com-

26 EARTHQUAKES.

pensating arrangement, so that the pendulum, for small
displacements, shall be in neutral equilibrium, and the
errors due to swinging shall be avoided.

Several methods have been suggested for making the
bob of an ordinary pendulum astatic for small displace-
ments. One method proposed by Gray consists in fixing
in the bob of a pendulum a circular trough of liquid, the
curvature of this trough having a proper form. Another
method which was suggested, was to attach a vertical
spiral spring to a point in the axis of the pendulum a
little below the point of suspension, and to a fixed point
above it, so that when the pendulum is deflected it would
introduce a couple.

Professor Ewing has suggested an arrangement so that
the bob of the pendulum shall be partly suspended by a
stretched spiral spring, and at the same time shall be
partly held up from below by a vertically placed strut, the
weight carried by the strut being to the weight carried by
the spring in the ratio of their respective lengths. As to
how these arrangements will act when carried into practice
yet remains to be seen.

Another important class of instruments are inverted
pendulums. ‘These are vertical springs made of metal
or wood loaded at their upper end with a heavy mass
of metal. An arrangement of this sort, provided at its
upper end with a pencil to write on a concave surface,
was employed in 1841 to register the earthquakes at
Comrie in Scotland. In Japan they were largely em-
ployed in series, each member of a series having a
different period of vibration. The object of these arrange-
ments was to determine which of the pendulums, with a
given earthquake, recorded the greatest motion, it being
assumed that the one which was thrown into the most
violent oscillation would be the one most nearly approxi-

SEISMOMETRY. 27

mating with the period of the earthquake. The result
of these experiments showed that it was usually those
with a slow period of vibration which were the most
disturbed.

Bracket Seismographs.—A group of instruments of
recent origin which have done good work, are the bracket
seismographs. These instruments appear to have been
independently invented by several investigators: the
germ from which they originated probably being the well-
known horizontal pendulum of Professor Zollner. In
Japan they were first employed by Professor W. 8. Chaplin.
Subsequently they were used by Professor Ewing and Mr.
Gray. They consist essentially of a heavy weight sup-
_ ported at the extremity of a horizontal bracket which is
free to turn on a vertical axis at its other end. When the
frame carrying this axis is moved in any direction except-
ing parallel to the length of the gate-like bracket, the
weight causes the bracket to turn round a line known as
the instantaneous axis of the bracket corresponding to
this motion of the fixed axis. Any point in this line may
therefore be taken as a steady point for motions at right
angles to the length of the supporting bracket. Two of
these instruments placed at right angles to each other
have to be employed in conjunction, and the motion of
the ground is written down as two rectangular components.
In Professor Ewing’s form of the instrument, light pro-
longations of the brackets form indices which give
magnified representations of the motion, and the weights
are pivoted round a vertical axis through their centre.

In the accompanying sketch B is a heavy weight
pivoted at the end of a small bracket C4 xk, which bracket
is free to turn on a knife-edge, K, above, and a pivot 4,
below, in the stands. At the time of an earthquake B
remains steady, and the index Pp, forming a continuation

28 EARTHQUAKES.

of the bracket, magnifies the motion of the stand, in the
ratio of AC: CN.

Fia. 3.

In an instrument called a double-bracket seismograph,
invented by Mr. Gray, we have two brackets hinged to
each other, and one of them to a fixed frame. The planes
of the two brackets are placed at right angles, so as to
give toa heavy mass supported at the end of the outer
bracket two degrees of horizontal freedom.

In all bracket machines, especially those which carry
a pivoted weight, it is doubtful whether the weight pro-
vides a truly steady point relatively to the plate on which
the record is written for motion parallel to the direction
of the arm.

Parallel-motion Instrument.—A machine which writes
its record as two components, and which promises great
stability, is one suggested by
Professor C. D. West. Like
the bracket machines it con-
sists of two similar parts
placed at right angles to each
other, and is as follows: A
bar of iron A is suspended
from both sides on pivots at
cc by a system of light arms hinging with each other at

=
Fia. 4.

SEISMOMETRY, 29

the black dots, between the upper and lower parts of the
rigid frame BC. The arms are of such a length that for
small displacements parallel to the length of the bar, cc
practically move in a straight line, and the bar is in
neutral equilibrium. A light prolongation of the bar d
works the upper end of the light index e, passing as a
universal joint through the rigid support Fr. A second
index e’ from the bar at right angles also passes through F.
The multiplying ends of these indices are coupled to-
gether to write a resultant motion on a smoked glass
plate s.

Conical Pendulums.—Another group of instruments
which have also yielded valuable records are the conical
pendulum seismographs. The idea of using the bob of
a conical pendulum to give a steady point in an earth-
quake machine was first suggested and carried into
practice by Mr. Gray. The seismograph as employed
consists of a pair of conical pendulums hung in planes at
right angles to each other. The bob of each of these
pendulums is fixed a short distance from the end of a
light lever, which forms the writing index, the short end
resting as a strut against the side of a post fixed in the
earth. The weight is carried by a thin wire or thread,
the upper end of which is attached to a point vertically
above the fixed end of the lever.

Rolling Spheres and Cylinders.—After the conical
pendulum seismographs, which claim several important
advantages over the bracket machines, we come to a
group of instruments known as rolling sphere seismo-
graphs. Here, again, we have a class of instruments for
the various forms of which we are indebted to the
ingenuity of Mr. Gray.

The general arrangement and principle of one of
these instruments will be readily understood from the

30 EARTHQUAKES.

accompanying figure. Ss is a segment of a large sphere
with a centre near c. Slightly below this centre a heavy
weight B, which may be a lead ring, is pivoted. At the
time of an earthquake c is steady, and the earth’s motions
are magnified by the pointer CAN in the proportion of
CA: AN. The working of this pointer or index is similar
to that of the pointer in the pendulum.

Fig. 5.

Closely connected with the rolling sphere seismo-
graphs, are Gray’s rolling cylinder seismographs.

These are two cylinders resting on a surface plate
with their axes at right angles to each other. Near to
the highest point in each of these cylinders, this point
remaining nearly steady when the surface plate is moved
backwards and forwards, there is attached the end of a
light index. These indices are again pivoted a short
distance from their ends on axes connected with the
surface plate. In order that the two indices may be
brought parallel, one ‘is cranked at the second pivot.

SEISMOMETRY. 31

Ball and Plate Seismograph.-— Another form of
seismograph, which is closely related to the two forms of
apparatus just described, is Werbeck’s ball and plate
seismograph. This consists of a surface plate resting on
three hard spheres, which in turn rests upon a second
surface plate. When the lower plate is moved, the
upper one tends to remain at rest, and thus may be used
as a steady mass to move an index.

The Principle of Perry and Ayrton.—An instru-
ment which is of interest from the scientific principle it
involves is a seismograph suggested by Professors Perry
and Ayrton, who propose to support a heavy ball on
three springs, which shall be sufficiently stiff to have an
exceedingly quick period of vibration. By means of
pencils attached to the ball by levers, the motions of the
ball are to be recorded on a moving band of paper. The
result would be a record compounded of the small vibra-
tions of the springs superimposed on the larger, slower,
wave-like motions of the earthquake, and, knowing the
former of these, the latter might be separated by analysis.
Although our present knowledge of earthquake motion
indicates that the analysis of such a record would often
present us with insuperable difficulties, this instrument
is worthy of notice on account of the novelty of the
principle it involves, which, the authors truly remark, has
in seismometry been a ‘ neglected’ one.

Instruments to record Vertical Motion.—The instru-
ments which have been devised to record vertical motion
are almost as numerous as those which have been de-
vised to record horizontal motion. The earliest form of
instrument employed for this purpose was a spiral
spring stretched by weight, which, on account of its
inertia, was supposed at the time of a shock to remain
steady. No satisfactory results have ever been obtained

3

32 EARTHQUAKES,

from such instruments, chiefly on account of the incon-
venience in making a spring sufficiently long to allow of
enough elongation to give a long period of vibration.
Similar remarks may be applied to the horizontally
placed elastic rods, one end of which is fixed toa wall,
whilst the opposite end is loaded with a _ weight.
Such contrivances, furnished with pencil on the weight
to write a record upon a vertical surface, were used in
1842 at Comrie, and we see the same principle applied in
a portion of Palmieri’s apparatus. Contrivances like
these neither give us the true
amplitude of the vertical mo-
tion, insomuch as they are
readily set in a state of oscil-
lation; nor do they indicate
the duration of a disturbance,
for, being once set in motion,
they continue that motion in
virtue of their inertia long
after the actual earthquake
has ceased. They can only
be regarded as seismoscopes.
The most satisfactory in-
4 strument which has yet been
devised for recording vertical
motion is Gray’s horizontal-
lever spring seismograph.
This instrument will be
better understood from the
ease accompanying sketch, A
vertical spring § is fixed at
its upper end by means of a nut n, which rests on the
top of the frame F, and serves to raise or lower the
spring through a short distance as a last adjustment for

nn”

él Gah ei

SEISMOMETRY, | 33

the position of the cross-arm A. The arm A rests at one
end on two sharp points, p, one resting in a conical hole
and the other in a v-slot; it is supported at B by the
spring Ss, and is weighted at c with a lead ring R. Over
a pin at the point C a stirrup of thread is placed which
supports a small trough, ¢ The trough ¢ is pivoted at a,
has attached to it the index 7 (which is hinged by means
of a strip of tough paper at h, and rests through a fine
pin on the glass plate g), and is partly filled with
mercury.

Another method of obtaining a steady point for
vertical motion is that of Dr. Wagener, who employs a
buoy partly immersed in a vessel of water. This was
considerably improved upon by Mr. Gray, who suggested
the use of a buoy, which, with the exception ofa long thin
style, was completely sunk.

Among the other forms of apparatus used to record
vertical motion may be mentioned vessels provided with
india-rubber or other flexible bottoms, and partially filled
with water or some other liquid. As the vessel is moved
up and down, the bottom tends to remain behind and
provides a more or less steady point. Pivoted to this is
a light index, which is again pivoted to a rigid frame in
connection with the earth. Instruments of this descrip-
tion have yielded good records.

Record Recewers.—A large number of earthquake
machines having been referred to, it now remains to con-
sider the apparatus on which they write their motions.
The earlier forms of seismographs, as has already been
indicated, recorded their movements in a bed of sand;
others wrote their records by means of pencils on sheets
of paper. Where we have seismographs which magnify
the motion of the earth, it will be observed that methods
like the above would involve great frictional resistances,

o4 EARTHQUAKES.

tending to cause motion in the assumed steady points of
the seismographs. One of the most perfect. instruments
would be obtained by registering photographically the
motions of the recording index by the reflection of a ray
of light. Such an instrument would, however, be difficult
to construct and difficult to manipulate. One of the best
practical forms of registering apparatus is one in which
the record is written on a surface of smoked glass. This
can afterwards be covered with a coat of photographer's
varnish, and subsequently photographed by the ‘ blue pro-
cess’ so well known to engineers.

To obtain a record of all the vibrations of an earth-
quake it is necessary that the surface on which the seis-
mograph writes should at the time of an earthquake be in
motion. Of record-receiving machines there are three
types. First, there are those which move continuously.
The common form of these is a circular glass plate like
an old form of chronograph, driven continuously by clock-
work. On this the pointers of the seismograph rest and
trace over and over again the same circles. At the time
of an earthquake they move back and forth across the
circles, which are theoretically fine lines, and leave a
record of the earthquake. Instead of a circular plate, a
drum covered with smoked paper may be used, which,
after the earthquake, possesses the advantage, after un-
rolling, of presenting the record in a straight line, instead
of a record written round the periphery of a circle, as is
the case with the circular glass plates. Such records are
easily preserved, but they are more difficult to photo-
graph. |

The second form of apparatus is one which is set in
motion at the time of a shock. This may be a con-
trivanee like one of those just described, or a straight
smoked glass plate on a carriage. By means of an elec-

po SO ee | a eS ee eee

SEISMOMETRY. 35

trical or a mechanical contrivance called a ‘starter,’ of
which many forms have been contrived, the earthquake
is caused to release a detent and thus set in motion the
mechanism which moves the record-receiver.

The great advantage of continuously-moving machines
is that the beginning and end of the shock can usually
be got with certainty, while all the uncertainty as to the
action of the ‘ starter’ is avoided. Self-starting machines
have, of course, the advantage of simplicity and cheap-
ness, while there is no danger of the record getting ob-
literated by the subsequent motion of the plate under the
index.

Time-recording Apparatus.—Of equal importance
with the instruments which record the motion of the
ground, are those instruments which record the time at
which such motion took place. The great value of time-
records, when determining the origin from which an earth-
quake originates, will be shown farther on. The most
important result which is required in connection with
time observations, is to determine the interval of time
taken by a disturbance in travelling from one point to
another. On account of the great velocity with which
these disturbances sometimes travel, it is necessary that
these observations should be made with considerable ac-
curacy. The old methods of adapting an apparatus to a
clock which, when shaken, shall cause the clock to stop,
are of little value unless the stations at which the obser-
vations are made are at considerable distances apart. This
will be appreciated when we remember that the disturb-
ance may possibly travel at the rate of a mile per second,
that its duration at any station may often extend over a
minute, and that one set of apparatus at one station may
stop, perhaps, at the commencement of the disturbance,
and the other near the end. A satisfactory time-taking

36 EARTHQUAKES.

apparatus will therefore require, not only the means for
stopping a clock, but also a contrivance which, at the same
instant that the clock is stopped, shall make a mark on a
record which is being drawn bya seismograph. In this
way we find out at which portion of the shock the time
was taken.

Palmieri stops a clock in his seismograph by closing
an electric circuit. Mallet proposes to stop a clock by
the falling of a column which is
attached by a string to the pen-
dulum of the clock. So long as.
the column is standing the string
is loose and the pendulum is free
to move; but when the column
falls, the string is tightened and
the penduium is arrested. The
difficulty which arises is to obtain
a column that will fall with a
slight disturbance. The best
' form of contrivance for causing a

Fig. 7. column to fall, and one which

| may also be used in drawing out

a catch to relieve the machinery of a record-receiver, is
shown in the accompanying sketch.

s is the segment of a sphere about 4°5 em. radius,
with a centre slightly above c. Lisa disc of lead about
7 cm. in diameter resting upon the segment. Above this
there is a light pointer, p, about 30 cm. long. On the
top of the pointer a small cylinder of iron, w, is balanced,
and connected by a string with the catch to be relieved.
When the table on which w PS rests is shaken, rotation
takes place near to C, the motion of the base s is magni-
fied at the upper end of the pointer, and the weight
is overturned. This catch may be used to relieve a

SEISMOMETRY. 37

toothed bar axled at one end, and held up above a pin
projecting from the face of the pendulum bob. When
this falls it catches the projecting pin and holds the
pendulum.

Another way of relieving the toothed bar is to hold
up the opposite end to that at which it is axled by resting
it on the extremity of a horizontal wire fixed to the bob
of a conical pendulum—for example, one of the indices of
a conical pendulum seismograph. The whole of this
apparatus, which may be constructed at the cost of a few
pence, can be made small enough to go inside an ordinary
clock case.

The difficulty which arises with all these clock-stop-
ping arrangements is that it is difficult for observers
situated at distant stations to re-start their clocks so that
their difference in time shall be accurately known. Even
if each observer is provided with a well-regulated chrono-
meter, with which he can make comparisons, the rating of
these instruments is for all ordinary persons an extremely
troublesome operation.

In order to avoid this difficulty the author has of late
years used a method of obtaining the time without
stopping the clock. To do this a clock with a central
seconds hand is taken, and the hour and minute hands
are prolonged and bent out slightly at their extremities
at right angles to the face, the hour hand being slightly
the longest. Each hand is then tipped with a piece of
soft material like cork, which is smeared with a glycerine
ink. A light flat ring, with divisions in it corresponding
to those on the face of the clock, is so arranged that at
the time of a shock it can be quickly advanced to touch
the inked pads on the hands of the clock and then with-
drawn. This isaccomplished by suitable machinery, which
is relieved either by an electro-magnet or some other

38 EARTHQUAKES,

contrivance which will withdraw a catch. In this way an
impression in the form of three dots is received on the disc,
and the time known without either stopping or sensibly
retarding the clock. |

For ordinary observers, if a time-taker is not used in
conjunction with a record-receiver, as good results as
those obtained by ordinary clock-stopping apparatus are
obtainable by glancing at an ordinary watch. Subse-
quently the watch by which the observation was made
should be compared with some good time-keeper, and the
local time at which the shock took place is then approxi-
mately known. 3

From what has now been said it will be seen that for
a complete seismograph we require three distinct sets of
apparatus—an apparatus to record horizontal motion, an
apparatus to record vertical motion, and an apparatus to
record time. The horizontal and vertical motions must
be written on the same receiver, and if possible side by
side, whilst the instant at which the time record is made
a mark must be made on the edge of the diagram which
is being drawn by the seismograph. Such a seismograph
has been constructed and is now erected in Japan. It is
illustrated in the accompanying diagram.

The Gray and Milne Seesmograph.—In this apparatus
two mutually rectangular components. of the horizontal
motion of the earth are recorded on a sheet of smoked
paper wound round a drum, D, kept continuously in motion
by clockwork, w, by means of two conical pendulum-seis-
mographs, c. The vertical motion is recorded on the
same sheet of paper by means of a compensated-spring
seismograph, S L M B.

The time of occurrence of an earthquake is deter-
mined by causing the circuit of two electro-magnets to be
closed by the shaking. One of these magnets relieves a

SEISMOMETRY, 39

mechanism, forming part of a time-keeper, which causes
the dial of the timepiece to come suddenly forwards on
the hands and-then move back io its original position.

|

uli

The hands are provided with ink-pads, which mark their
positions on the dial, thus indicating the hour, minute.
and second when the circuit was closed. The second

40 EARTHQUAKES,

electro-magnet causes a pointer to make a mark on the
paper receiving the record of the motion. This mark
indicates the part of the earthquake at which the circuit
was closed.

The duration of the earthquake is estimated from the
length of the record on the smoked paper and the rate of
motion of the drum. ‘The nature and period of the dif-
ferent movements are obtained from the curves drawn on
the paper.

Mr. Gray has since greatly modified this apparatus,
notably by the introduction of a band of paper sufficiently
long to take a record for twenty-four hours without repe-
tition. The record is written in ink hy means of fine
siphons. In this way the instrument, which is extremely
sensitive to change of level, can be made to show not only
earthquakes, but the pulsations of long period which have
recently occupied so much attention.

———

CHAPTER IIL
EARTHQUAKE MOTION DISCUSSED THEORETICALLY.

Ideas of the ancients (the views of Travagini, Hooke, Woodward,
Stuckeley, Mitchell, Young, Mallet)—Nature of elastic waves and
vibrations— Possible causes of disturbance in the Earth’s crust—
The time of vibration of an earth particle—Velocity and accelera-
tion of a particle—Propagation of a disturbance as determined by
experiments upon the elastic moduli of rocks—The intensity of an
earthquake—Area of greatest overturning moment—Earthquake
waves—Reflexion, refraction, and interference of waves—Radiation
of a disturbance.

Ideas of Early Writers.—One of the first accounts of
the varieties of motion which may be experienced at the
time of an earthquake is to be found in the classification
of earthquakes given by Aristotle.! It is as follows :—

1. Epiclints, or earthquakes which move the ground
obliquely.

2. Brastz, with an upward vertical motion like boil-
ing water.

3. Chasmatiz, which cause the ground to sink and
form hollows.

4, Rhectz, which raise the ground and make fissures.

5. Ostee, which overthrow with one thrust.

6. Palmatiz, which shake from side to side with a
sort of tremor.

From the sixth group in this classification we see that

'! De Mundo, ¢. iv.

42 - EARTHQUAKES.

this early writer did not regard earthquakes as necessarily
isolated events, but that some of them consisted of a
succession of backward and forward vibratory motions. He
also distinguishes between the total duration of an earth-
quake and the length of, and intervals between, a series
of shocks. Aristotle had, in fact, some idea of what
modern writers upon ordinary earthquakes would term
‘ modality.’ :

The earliest writer who had the idea-that an earth-
quake was a pulse-like motion propagated through solid
ground appears to have been Francisci Travagini, who,
in 1679, wrote upon an earthquake which in 1667 had
overthrown Ragusa. The method in which the pulses
were propagated he illustrated by experiments.

Hooke, who, in 1690, delivered discourses on earth-
quakes before the Royal Society, divides these phenomena

according to the geological effects they have produced ;

thus there is a genus producing elevations, a genus pro-
ducing sinkings,a genus producing conversions and trans-
portations, and a genus which produces what, in modern
language, we should term metamorphic action.
Woodward, in his ‘ Natural History,’ written in 1695,

speaks of earthquakes as being agitations and concussions »

produced by water in the interior of the earth coming in
contact with internal fires.

Stuckeley observed that an earthquake was ‘a tremor
of the earth,’ to be explained as a vibration in a solid.
The Rev. John Mitchell, writing in 1760, says that the
motion of the earth in earthquakes is partly tremulous
and partly propagated by waves.

From these few examples, to which might be added
many more, it will be seen that an earthquake disturb-
ance has usually been regarded as a concussion, vibration,
trembling, or undulatory movement. Further, it can be

EARTHQUAKE MOTION DISCUSSED THEORETICALLY. 43.

seen in narratives of earthquakes that it had been often
observed that these tremblings and shakings continued
over a certain period of time. Although it had been
noticed that large areas were almost simultaneously
affected by these disturbances, no definite idea appears
to have existed as to how earthquake motion was pro-
pagated. Usually it was assumed that the disturbance
- spread through subterranean channels.

The first true conception of earthquake motion and
the manner of its propagation is due to Dr. Thomas
Young, who suggested that earthquake motion was vibra-
tory, and it might be ‘propagated through the earth
nearly in the same manner as a noise is conveyed through
the air.’ The same idea was moulded into a more definite
form by Gay Lussac.

The first accurate definition of an earthquake is due to
Mr. Robert Mallet, who, after collecting and examining
many facts connected with earthquake phenomena, and
reasoning on these, with the help of known laws con-
nected with the production and propagation of waves of
various descriptions, formulated his views as follows :—

An earthquake is ‘the transit of a wave or waves of
elastic compression in any direction from vertically wp-
wards to horizontally, in any azimuth, through the crust
and surface of the earth, from any centre of impulse
or from more than one, and which may be attended with
sound and tidal waves, dependent upon the impulse and
wpon circumstances of position as to sea and land.’

In brief, so far as motion in the earth is concerned,
Mallet defined an earthquake as being a motion due to
the transit of waves of elastic compression. In many cases
it is possible that this is strictly true, but in succeeding
pages it will be shown that earthquake motion may also
be due tn the transit of waves of elastic distortion.

44. EARTHQUAKES.

To obtain a true idea of earthquake motion is a matter
of cardinal importance, as it forms the key-stone of many
investigations.

If we know the nature of the motion produced by an
earthquake, we are aided in tracking it to its origin, and
in reasoning as to how it was produced. If our knowledge
of the nature of the motion of an earthquake is incorrect,
it will be impossible for us intelligently to construct
buildings to withstand the effects of these disturbances.
We have thus to consider, in this portion of seismology, a
point of great scientific importance, and shall deal with it
at some length.

Nature of Elastic Waves and Vibrations.—When it is
stated that an earthquake consists of elastic waves of
compression and distortion, the student of physics has
a clear idea of what is meant and a knowledge of the
mechanical laws which govern such disturbances. The
ordinary reader, however, and the majority of the in-
habitants of earthquake countries, who of all people have
the greatest interest in this matter, may not have so clear
a conception, and it will, therefore, not be out of place to
give some general explanation on this point.

The ordinary idea of a wave is that it is a disturbance
similar to that which we often see in water. Waves like
these must not, however, be confounded with elastic waves.
A disturbance produced in water, say, for instance, by
dropping a stone into a pond, is propagated outwards by the
action of gravity. First, a ridge of water is raised up by
the stone passing beneath the surface. As this ridge falls
towards its normal position in virtue of its weight, it
raises a second ridge. This second ridge raises a third
ridge,and soon. The water moves vertically up and down,
whilst the wave itself is propagated horizontally.

To understand what is meant by elastic waves, it is

EARTHQUAKE MOTION DISCUSSED THEORETICALLY. 45

first necessary to understand what is meant by the term
elastic. In popular language the term elastic is confined
ta substances like india-rubber, and but seldom to rock-
like materials, through which earthquake waves are
propagated. India-rubber is called elastic because after
we remove a compressive force it has a tendency to spring
back to its original shape. The elastic force of the india-
rubber is in this case the force which causes it to resist a
change of form. Now, a piece of rock may, up to a
certain point, like the india-rubber, be compressed, and
when the compressing force is removed it will also tend to
resume its original form. However, as the rock offers
more resistance to the compressing force than the india-
rubber offers, we say that it is the more elastic. It may
be here observed that a substance like granite offers great
resistance, not only to compression or a change of volume,
but also to a change of form or shape; whereas a sub-
stance like air, which is also elastic, only offers resistance
to compression, but not to a change of shape.

With these ideas before us we will now proceed to
consider how, after a body has been suddenly compressed
or distorted, this disturbance is propagated through the
mass. For the elastic body let us take a long spiral
spring hung from the ceiling of a room and kept slightly
stretched by a weight. If we give this weight an up-
ward tap from below, say with a hammer, we shall observe
a pulse-like wave which runs up the spring until it reaches
the ceiling of the room. Here it will, so to speak, re-
bound, like a billiard ball from the end of a table, and
run towards the weight from which it started. Whilst
this is going on we may also observe that the weight is
moving up and down.

Here, then, we have two distinct things to observe—
one being the transmission of motion up to the ceiling,

46 EARTHQUAKES.

which we may liken to the transmission of an earthquake
wave between two distant localities on the earth’s surface,
and the other being the up and down motion of our
weight, which we may compare to the backward and for-
ward swinging which we experience at the time of an
earthquake. |

These two motions—namely, the pulse-like wave pro-
duced by the transmission of motion, and the backward
and forward oscillation of the weight or of any point on the
spring—must be carefully distinguished from each other.

First, we will consider the backward and forward motion
of the weight. The distance through which the weight
moves depends upon the force of the blow. The number
of up and down oscillations it makes, say in a second,
depends upon the stiffness of the spring. The weight,
supposing it to be always the same, will move more quickly
at the end of a stiff spring than at the end of a flaccid
one; that is to say, its velocity is quicker. As in any
given spring the number of up and down oscillations are
always the same in a given interval of time, if these
oscillations are of great extent, the weight must move
more quickly with large than with small oscillations.

At the time of an earthquake the manner in which
we are moved backward and forward is very similar to the
manner in which the weight is moved. If we stand ona
hard rock-like granite, we are to a great extent placed as
if we were attached to a stiff quickly-vibrating spring. If,
however, we are on a soft rock, it is more like being on a
loose flaccid spring.

All that has thus far been considered has been a back-
ward and forward kind of motion, where there is a recti-
linear conupression and extension amon gst the particles on
which we stand.

We might, however, imagine our rock, which for the

SS So ed a) See iin ? # tras Pee eee!

he ge Te eee, LO ad

EARTHQUAKE MOTION DISCUSSED THEORETICALLY. 47

moment we will consider to be a square column, to be
twisted, and thus have its shape altered. When the
twisting force is taken off it seems evident that the
column would endeavour to untwist itself or regain its
original form. Now the force which a body offers against
a change of volume may be very different from Ula which
it offers against a change of form.

In disturbances aan take place in the rocky crust
of our earth, it would seem possible that we may have
vibrations set up which are either compressions and ex-
tensions or twistings and distortions. These may take
place separately or simultaneously, or we may have resul-
tant motions due to their combination.

The following are examples of possible causes which
might give rise to these different orders of disturbance :—

1. Imagine a large area stretched by elevation until
it reaches the limit of its elasticity and cracks. After
cracking, in consequence of its elasticity, it will fly back
over the whole area like a broken spring, and each point
in the area will oscillate round its new position of equili-
brium. In this case there will be no waves of distortion
excepting near the end of the crack, where waves are
transmitted in a direction parallel to the fissure.

2. The ground is broken and slips either up, down,
or sideways, as we see to have taken place in the pro-
duction of faults. Here we get distortion in the direction
of the movement, and waves are produced by the elastic
force of the rock, causing it to spring back from its dis-
torted form. Im a case like this the production of a
fissure running north and south might give rise to north
and south vibrations, which would be propagated end on
towards the north and south, but broadside on towards
the east and west. With disturbances of this kind, on
account of the want of homogeneousness in the materials

48 EARTHQUAKES.

in which they are produced, we should expect to find

waves of compression and extension.

3. A truly spherical cavity is suddenly formed by the
explosion of steam in the midst of an elastic medium.
In this case all the waves will be those of compression,
each particle moving backward and forward along a radius.

Should the cavity, instead of being truly spherical, be
irregular, it is evident that, in addition to the normal
vibration of compression, transverse waves of distortion
will be more or less pronounced, depending upon the
nature of the cavity.

The combination of these two sets of vibrations may |

cause a point in the earth to move in a circle, an ellipse,
the form of a figure eight, and in other curves similar to
these, which are produced by apparatus designed to show
the combination of harmonic motion. From these ex-
amples it will be seen that we have therefore to consider
_ two kinds of vibrations—one produced by compression or
the alteration of volume, and the other produced by an
alteration in shape.

Now the resistance which a body offers, either to a
change in its volume or in its shape, is called its elasticity,
and the law which governs the backward and forward motion
of a particle under the influence of this elasticity may be
expressed as follows :

If ' be the time of vibration, or the time taken by a
particle to make one complete backward and forward swing,
p the density of the material of which this particle forms a
part, and E the proper modulus of elasticity of the mate-

rial, then, we
Toss) 2 97 hag ee
E

From this formula, T = 2 7 ai, : » we see that the

EARTHQUAKE MOTION DISCUSSED THEORETICALLY. 49

time of vibration of the earth during an earthquake, or
the rate at which we are shaken backwards and forwards,
varies directly as the square root of the density of the
material on which we stand, and inversely as the square
root of a number proportional to its elasticity.

Velocity and Acceleration of an Earth Particle-—
Another important: point, which the practical seismologist
has often brought to his notice, is the question of the
velocity with which an earth particle moves. According

tothe formula, T = 2 7 ve -- , we should expect that a

particle would make each semi-vibration in an equal time,
and from a knowledge of the density and elastic moduli
of a body this time might be calculated. Although the
time of a semi-oscillation may be constant, we must bear
in mind that, like the bob of a pendulum during each of
its swings, the particle starts from rest, increases in velo-
city until it reaches the middle portion of its half swing,
from which it gradually decreases in speed until it reaches
zero, when it again commences a similar motion in the
opposite direction.

These pendulum-like vibrations are sometimes spoken
of as simple harmonic motions. If we know the distance
through which an earthquake moves in making a single
swing, and the time taken in making this swing, on the
assumption that the motion is simple harmonic we can
easily calculate the maximum velocity with which the
particle moves.

Thus, if an earth particle takes one second to com-
plete a semi-oscillation, half of which, or the amplitude
of the motion, equals a, the maximum velocity equals
TX

Again, assuming the earth vibrations to be simple
harmonic, the maximum acceleration or rate of change in

50 - -RARTHQUAKES.

velocity will come about at the ends of each semi-oscilla-
tion; and if v be the maximum velocity of the particle,

and a the amplitude or half semi-oscillation, then the

72
maximum acceleration equals pi
a

Later on it will be shown, as the result of experiment,
that certain of the more important earth oscillations in
an earthquake are not simple harmonic motion. Never-
theless the above remarks will be of assistance in show-
ing how the velocity and other elements connected with
the motion of an earth particle, which are required by the
practical seismologist, may be calculated, irrespective of
assumptions as to the nature of the motion.

Propagation of a Disturbance.—We may next con-
sider the manner in which a disturbance, in which there
are both vibrations of compression and of distortion, is
propagated. The first or normal set of vibrations are pro-
pagated in a manner similar to that in which sound
vibrations are propagated. From a centre of disturbance
these movements approach an observer at a distant
station, so to speak, end on. The other vibrations have
a direction of motion similar to that which we believe to
exist in a ray of light. These would approach the ob-
server broadside on.

If the disturbance passed through a formation like a
series of perfectly laminated slates, each of these two sets
of vibration might be subdivided, and we should then
obtain what Mallet has termed ordinary and extraordinary
normal and transverse vibrations.

In consequence of the difference in the elastic forces
on which the propagation of these two kinds of vibration
depends, the normal vibrations are transmitted faster than
the transversal ones—that is to say, if an earthquake
originated from a blow, the first thing that would be

EARTHQUAKE MOTION DISCUSSED THEORETICALLY. 51

felt at a point distant from the origin of the shock would
be a backward and forward motion in the direction to and |
from the origin, and then, a short interval afterwards, a
motion transversal, or at right angles to this, would be
experienced.

From the mathematical theory of vibratory motions it
is possible to calculate the velocity with which a distur-
bance is propagated. As the result of these investigations
it has been shown that normal vibrations travel more
quickly than transverse vibrations.

- Deductions from experiments on small specimens are,
however, invalidated by the fact that the specimens used
for experiments are, of course, nearly homogeneous, whilst
the earthquake passes through a mass which is hetero-
geneous and more or less fissured. Mallet, by experiments
‘on the compressibility of solid cubes of these rocks,
obtained the inean modulus of elasticity,’ with the result
that ‘nearly seven-eighths of the full velocity of wave-
transit due to the material, if solid and continuous, is lost
by reason of the heterogeneity and discontinuity of the
rocky masses as they are found piled together in nature.’
The full velocities of wave-transit, as calculated by Mallet
from a theorem given by Poisson, were—

For slate and quartz transverse to lamination, 9,691 feet per second,

in line of lamina ion, 5,415 ,,

39 39 9

This more rapid transmission in a direction transverse
to the lamination, Mr. Mallet observes, may be more than
counterbalanced by the discontinuity of the mass trans-
verse to the same direction.

The Intensity of an Earthquake.—The intensity of
an earthquake is best estimated by the intensity of the
forces which are brought to bear on bodies placed on the
earth’s surface. These forces are evidently proportional

52 EARTHQUAKES.

to the rate of change of velocity in the body, and, as the
destructive effect will be proportional to the maximum
forces, we may consistently indicate the intensity of an
earthquake by giving the maximum acceleration to which
bodies were subject during the disturbance. On the
~ assumption that the motion of a point on the earth’s surface
is simple harmonic, the maximum acceleration is directly
as the maximum velocity and inversely as the amplitude

Vv a :
of motion, or as — where v indicates velocity and a
a

amplitude.

The next question of importance is to determine the
manner in which earthquake energy becomes dissipated—
that is, to compare together the intensity of an earth-
quake as recorded at two or more points at different
distances from the origin. First let us imagine the
origin of our earthquake to be surrounded by concentric
shells, each of which is the breadth of the vibration of a
particle. Going outwards from the centre, each successive
shell” will contain a greater number of particles, this
number increasing directly as the square of the distance
from the origin. Let the blow have its origin at the centre,
and give a vibratory movement to the particles in one of
the shells near the centre.

This shell may be supposed to possess a certain amount
of energy, which will be measured by its mass and the
square of the velocity of its particles. In transferring this
energy to the neighbouring shell which surrounds it,
because it has to set in motion a greater number of par-
ticles than it contains itself, the energy in any one particle
of the second layer will be less than the energy in any one
particle in the first layer ; the total energy in the second
shell, however, will be equal to the total energy in the first
shell. Neglecting the energy lost during the transfer, if

EARTHQUAKE MOTION DISCUSSED THEORETICALLY. 53

the energy in a particle of the first shell at any particular
phase of the motion be K,, and the energy in a particle of
the second shell x«,, these quantities are to each other
inversely as the masses of the shells—that is, inversely as
the squares of the mean radii of the shells.
K fine
I b 1 ane = ls e o e e lL
n symbols, eer (1)
Assuming that energy is dissipated,

27 hls 2 One See

3
V9

Ky hy

Ky Ty
where f<1 is the rate of dissipation of energy which is
assumed to be constant.

Area of greatest Overturning Moment.—Although
the rate of dissipation of the impulsive effects of an
earthquake may follow a law like that just enumerated,
it must be remembered that if the depth of the origin is
comparable with the radius of the area which is shaken,
the maximum impulsive effect as exhibited by the actual
destruction on the surface may not be immediately
above the origin where buildings have simply been lifted
vertically up and down, but at some distance from this
point, where the impulsive effort has been more oblique.

At the epicentrum we have the maximum of the true
intensity as measured by the acceleration of a particle, or
the height to which a body might be projected, but it
will be at some distance from this where we shall have
the maximum intensity as exhibited by an overturning
effort.

This will be rendered clear by the following diagram.

In the accompanying diagram let 0 be the origin of a
shock, and oc the seismic vertical equal to 7. Let the
direct or normal shock emerge at C,C,, C,, and at the
angles 6,, 0,, &c.

:

54 EARTHQUAKES.

Assuming that the displacement of an earth particle
at C equals CB, and at C, equals ¢,b,, and at C, equals
c, b,, &e., and let these displacements CB, ¢, b,, ¢,6,, &e.,
for the sake of argument, vary inversely as r, 7,, 7,, &e.

Fie. 9.

The question is to determine where the horizontal
component C A of these normal motions is a maximum.
First observe that the triangle 0 Cc is similar toa, B, ¢.

ASO 9S ml , and therefore the normal component
si

n @

sin @

c, b, at ©, is equal to c

Also-e, a= ¢,b,, cos 0.

Sie oie @cosO _ c¢_ sin 20
Pro h h 2 oe
and sin 26 is greatest when 26 = 90° or 0 = 45°.

That is to say, the horizontal component reaches a
maximum where the angle of emergence equals 45°.

This question has been discussed on the assumption
that the amplitude of an earth particle varies inversely as
its distance from the origin of the shock. Should we,
however, assume that this amplitude varies inversely as
the square of the distance from the origin, we are led to
the result that the area of greatest disturbance is nearer
to the point where the angle of emergence is 55° 44’ 9”,

EARTHQUAKE MOTION DISCUSSED THEORETICALLY. 55

Both of these methods are referred to by Mallet, but the
first is considered as probably the more correct.

Earthquake Waves.—Hitherto we have chiefly eon-
sidered earthquake vibrations; now we will say a few
words about earthquake waves. If we strike a long iron
rod at one end, we can imagine that, as in the long
spring, a pulse-like motion is transmitted. If the rod be
struck quickly, the pulses will rapidly succeed each other,
and if struck slowly the pulses will be at longer intervals.
. Each individual pulse, however, will travel along the rod
at the same rate, and hence the distance between any two
will remain constant; but that distance will depend on
the interval between the blows producing these pulses
being equal to the distance travelled by one pulse before
the next blow is struck.

From this we see that an irregular disturbance will
produce an irregular succession of motions; some will be
like long undulations in a wide deep ocean, whilst others
will be like ripples in a shallow bay. Again, consider
the bar to be struck one blow only, and then left to itself.
The bar will propagate a series of pulses along its length,
due to the out and in vibration of its end. These will
succeed each other at regular intervals, and will be mixed
up with the pulses we have previously considered.

From this we see that in an earthquake, if it be pro-
duced by one blow, the motion will be isochronous in its
character; but if it be due to a succession of blows at
regular intervals, the motion will be the resultant of a
series of isochronous motions, and will be periodical. If
the impulses are irregular, you have a motion which is
the resultant of a number of isochronous motions due to
each impulse, but these compounded together in a differ-
ent manner at each instant during the earthquake, aud
giving as a result a motion which is in no sense isochron-

ae

56 EARTHQUAKES.

ous. This approaches more nearly to the actual motions
we feel as earthquakes.

If we can imagine ‘the ground shaken by an earth-
quake, made of a transparent material which transmitted
less ight when compressed, and we could look down upon
a long extent of this at the time of an earthquake, we
should see a series of dark bands indicating strips of
country which were compressed. The distances between
these bands might be irregular. Keeping our attention
on one particular band, this would be seen to travel
forward in a direction from the source. If we kept our
eye on one particular point, it would appear to open and
shut, becoming light and dark alternately.

As to the existence of these elastic waves in actual
earthquakes we have no direct experimental evidence.
The only kind of wave with which we are familiar isa true
surface undulation, which, although having the appearance
of a water-wave, may nevertheless represent a district of
compression.

CHAPTER IV.
EARTHQUAKE MOTION AS DEDUCED FROM EXPERIMENT.

Experiments with falling weights—Experiments with explosives—Re-
sults obtained from experiments—Relative motion of two adjacent
points—The effect of hills and excavations upon the propagation of
vibrations—The intensity of artificial disturbances—Velocity with
which earth vibrations are propagated—Experiments of Mallet—
Experiments of Abbot—Experiments in Japan—Mallet’s results—
Abbot’s results—Results obtained in Japan.

Experiments with Falling Weights.—A series of ex-
periments, as the nature of the disturbance produced in
the surface of the earth when a heavy weight is allowed
to fall on it, was begun in November 1880 by Mr. T.
Gray and the author. These experiments were carried
out at the Akabane Engineering Works in Tokio. The
weight used was a ball of iron weighing about a ton,
which in the different experiments was allowed to fall
from heights varying between ten and thirty-five feet.
The position of the place where the ball was allowed to
fall was such that in one direction the vibrations were
transmitted up the side of a steep hill, in another direction
across a pond with perpendicular sides, and in another
direction across a level plain the material of which con-
sisted for the most part of hardened mud extending to a
very considerable depth. The vibrations produced by
the fall of the ball were transmitted through this hard
mud with considerable intensity to a distance of between
300 and 400 feet.

58 EARTHQUAKES,

The object of the experiment was to find the nature
of the vibrations produced in the crust of the earth by
such a blow, the velocity of transmission through this
comparatively soft material, the effect of hills and excava-
tions in cutting off such disturbances, and the law accord-
ing to which the amplitude of the vibrations diminishes
with the distance from the source.

A considerable variety of apparatus was used during
these experiments, but the most reliable results were
obtained from the records of a rolling sphere seismograph,
which wrote the vibrations on a stationary plate, and from
the records of two bracket seismographs, similar to Pro-
fessor Ewing’s horizontal lever seismographs, which gave
a record of the vibrations as two rectangular components
on a moving plate of smoked glass.

RY
WN

€)
\\'
Y K

Fie. 10.

The general result as to the nature of the disturbance
was that two distinct sets of vibrations were set up by the
blow. In one set the direction of motion was along a
line joining the point of observation with the point from
which the disturbance emanated; in the other set the

EARTHQUAKE MOTION DEDUCED FROM EXPERIMENT. 59

direction of motion was at right angles to that line. The
nature of the resultant motion will be gathered from fig.
10, which is taken from the records drawn by the rolling
sphere seismograph at a distance of 50 feet, 100 feet, and
200 feet respectively from the point where the ball struck
the ground. The direct or normal vibrations reached the
instrument first, and were followed at an interval depend-
ing on the distance of the instrument from the origin by
the transverse vibrations. From the records of these two
sets of vibrations as separated by the bracket seismographs,
combined with the known rate of motion of the glass
plate, the velocity of transmission was found to be, for
normal vibrations 446-438 feet per second, and for trans-
verse vibrations 357-353 feet per second.

The effect of the hill in cutting off the disturbance
seemed to be slight, but the direction of the vibrations
which ascended the side was mostly transverse. The
pond, on the other hand, seemed completely to cut off the
disturbance, which, however, gradually crept round the
side, so that only a comparatively small triangular area
was in shadow.

The amplitude of the vibrations diminished directly as
the distance increased for some distance from the origin,
but at greater distance the rate of diminution seemed to
be slower. The transverse vibration seemed to die out
less quickly than the normal vibrations.!

These experiments were afterwards very considerably
extended by the author. In these later experiments
charges of from one to two pounds of dynamite were
placed in bore-holes of various depths and exploded by
means of electricity. The results obtained confirmed the
conclusions already arrived at from the former experiments.
The experiments on velocity, however, seemed to indicate

1 See Phil. Trans. R. 8., Part III, 1882.

60 EARTHQUAKES.

that the higher the initial impulse the greater was the
velocity. The velocity of propagation of the transverse
vibrations seemed to approach more and more to that of
the directed vibrations as the distance from the origin of
disturbance increased. Fig. 11 shows the nature of the
record obtained from the explosion of two pounds of
dynamite at the bottom of a bore-hole eight feet deep.

0”

A
100 Feet

B
i 250 Feet
i
|
|
Mormal ___ HM a _
Bae
400 Feet
os he a

Fic. 11.—Records obtained at three stations of the motion of the
ground produced by the explosion of 2 lbs. of dynamite.

These records show the interval of time which elapsed be-
tween the arrival of the normal and the transverse vibra-
tions at points distant 100, 250, and 400 feet from the
bore-hole. In the case of the 100-feet station it will be
observed that the motion towards the origin is greater
than that from the origin. It is also to be noticed that
the period of vibration becomes greater as the distance
from the origin increases.

EARTHQUAKE MOTION DEDUCED FROM EXPERIMENT. 61

The Intensity of Artificial Disturbances.—The data
which we have at our disposal for determining the inten-
sity of an earth particle which has been caused to vibrate
by the explosion of a charge of dynamite are a series of
records similar to that given on p. 60. These disturb-
ances are practically surface movements, and may be com-
pared with the movements of an earthquake which spreads
over an area the radius of which is great as compared with
its depth.

To find the mean acceleration of an earth particle,
which quantity has been taken to represent intensity,
during any simple backward or forward motion of the
earth, it will be first necessary to determine the amplitude

of this motion and its maximum velocity, the mean accele-
2

ration being equal to 5

The second and third movements ina shock invariably
exhibited the greatest intensity, and to a distance of 400
feet from the origin, where about three pounds of dynamite
had been exploded in
a bore-hole about six
feet deep, these in-
tensities decreased
directly as the dis-
tance from the origin.
The less intense
movements also de-

creased directly as ashore Zs
i : a pit id i

the distance from the origin —,! 2 ER Tibe

origin to a certain Scale ae roe

point, but after that Fie, 12.

they decreased more slowly. A mean result of the more
prominent vibrations in four sets of experiments is shown
in the curve, fig. 12, where the horizontal measurements

62 EARTHQUAKES.

represent distance from the origin in feet, and the vertical
measurements mean acceleration in thousands of milli-
metres per second. |

This curve approximates to an equi-angular hyperbola.
The area between the curve and its asymptotes is propor-
tional to the whole energy of the shock. The area of the
Giagram is proportional to the energy given up to the
grcund by the explosion of three pounds of dynamite. If
we call the unit shock the effect produced by the explosion
of one pound of dynamite, the above artificial ae
had an intensity equal to three.

The only other investigations which have been made
in this interesting branch of observational seismology are
those by Mr. Robert Mallet,! and those by General Henry
L. Abbot.?

Mallet’s Results.—The velocity with which earth
vibrations were transmitted as deduced by Mr. Mallet

were as follows :—
Feet per second
In sand . - : ° : . 824-915
In contorted stratified ioek ks tz, and slate
at Holyhead . : : ‘ - 1,088°669
In discontinuous and much Siateerd granite 1,306-425
In more solid granite . : : : . 1,664°574

A striking result which was obtained by Mallet in his
experiments at Holyhead was that the transit velocity
increases with an increase in the intensity of the initial
shock. Thus with a charge of 12,000 pounds of powder
the transit rate was 1,373 feet per second, whilst with 2,100
pounds the transit rate was 1,099 feet per second. In

1 Report of the British Association, 1851.

2 «On the Velocity of Transmission of Earth Waves,’ by General
H. L. Abbot, American Journal of Science and Arts, vol. xv. Mar-h
1878; ‘Shock of the Explosion at Hallet’s Point,’ by Bvt. Brig.-Gen.

Henry L. Abbot, read before the Essayons Club of the Corps of
Engineers, Nov. 1876.

_ EARTHQUAKE MOTION DEDUCED FROM EXPERIMENT. 63

these experiments tremors were observed as preceding and
following the main shock.

Abbot’s Reswits.—The important results obtained by
General Abbot are contained in the following table :—

' a ° 5 q
re ee] s a mn 6 a ms o Ko}
: iS Date Cause of Shock eh = S. 8 SUA 8
Ag Bah | &F | gee
S 5a 3 if
1 | Aug. 18, 1876 200 lbs. of dynamite 5 + B | 5,280
2 |Sept. 24,1876) Hallet’s Point Explosion | 5:134 A |3,873
3 93 ” 39 - 8330 | B_ [8,300
4 2 ” 3 9:333 | A |4,521
5 99 - s i 12:'769 | B_ |5,309
6 | Oct. 10, 1876 70 lbs. dynamite 1360] A |1,240
7 | Sept. 6, 1877 400 ,, a 17169 A | 3,428
8 = ae : 1169 | B {8,814
9 |Sept. 12, 1877 200 ,, es 1:340 | A |6,730
10 99 ” «99 ” 1°340 | B 8,730
11 ” wos 455 1340; A [5,559
12 ” 9 99 ” 1°340 | B 8,415

A seismometer of type A means that the telescope
used in observing the tremor produced on the surface of
a vessel of mercury by the

_passage of. the shock had a
magnification of 6, whilst a
telescope of the type B had ©
a magnification of 12.

The mean velocity given
by six observations with type Fic. 18.

A is 4,225 feet per second,
while that given by the same number with type B is 7,475
feet per second.

If we assume that the first tremor observed in the
mercury is to determine the true rate of transmission,
General Abbot tells us that we must reject all observations
made with type A, inasmuch as they do not reveal the
velocity of the leading tremor. However, he also tells

64 EARTHQUAKES.

us that a still higher power above 12 might have detected
still earlier tremors. |

When gunpowder was the explosive, the observers
noted that the disturbance observed in the mercury took
a much longer time to reach a maximum than it did when
dynamite was employed.

It was also observed that explosions fired beneath deep
water gave a higher velocity than similar explosions which
took place beneath shallow water. In the latter case
much of the energy was probably expended in throwing a
jet of water into the air.

Another point which was observed appears to have
been that the rate varied with the initial shock. Thus:—

Feet per second
400 lbs. of dynamite gave . e ° . - 8,814
200 4, “ : - . . 4 8,730
LOR ss powder (deep) gave . : - : 8,415

Also it is probable that the rate of a wave diminished

with its advance. For,
Feet per second

200 lbs. of dynamite gave for 1 mile ° . 8,730

39 99 ” ” 5 miles ° F 5,250
50,000 ” 3 39 8 ” e e 8,300
29 ” ” 99 133 ” ° ° 5,300

General Abbot’s general conclusions are :—

1. A high magnifying power of telescope is essential
in seismometric observations.

2. The more violent the initial shock the higher is the
velocity of transmission.

3. This velocity diminishes as the general wave ad-
vances.

4. The movements of the earth’s crust are complex,
consisting of many short waves first, increasing and then
decreasing in amplitude; and with a detonating explosive
the interval between the first wave and the maximum

EARTHQUAKE MOTION DEDUCED FROM EXPERIMENT. 65

wave, at any station, is shorter than with a slow burning
explosive.

Results obtained in Japan.—From some experiments
made by the author in the grounds of: the Meteorological
Department in Tokio, the following results were obtained :—-

Velocity in Velocity in Velocity in Number of
No. of feet per second| feet per second | feet per second] Cartridges
Explosion for the first |for the second| for 400 ft. of Dynamite
200ft.(AtoB)|200ft.(BtoC)| (AtoC) (6 = 1 1b.)
I. 464 186 265 8°3
Vertical III. — Zt — 10°1
vibrations IV. 352 234 281 Gt
Vi 343 232 Ze 5:0
Normal { VI. — — 407 10:0
vibrations (| VII. _ — 516 12°5
oo | VIL. ae an 344 12°5
vibrations

The general results to be deduced from the above
appear to be :—
1. For vertical motion.

(a) For the first 200 feet. The velocity depends
upon the initial foree—the greater the charge of
dynamite the greater the velocity.

(6) For the second 200 feet. The above law only
appears in experiments IV. and V., but it must be
remembered that the origins of I. and III. were
farther removed from a than IV. and V.

The speed of the wave during the second 200 feet is
always less than during the first 200 feet.
2. For normal vibrations.

Here the speed between a and c is all that was
measured, but we again see that the greater
the initial force, or the nearer we are to the origin
of the disturbance, the greater is the velocity.
This velocity is greater than the velocity of the
vertical or transverse vibrations.

66 : EARTHQUAKES,

3. For transverse vibrations.
If we assume that the vertical vibrations are a
component of the transverse motions we see the
same law as before—namely, that the nearer we

are to the origin of the disturbance the greater

is the speed with which that disturbance is pro-
pagated.

It will be observed that the chief law here enunciated
respecting the decrease in speed of earth vibrations is the
same as that pointed out by General Abbot, from which it
only differs by its being in all cases proved without the
introduction of personal errors, for the same explosion,
along the same line of ground and for different kinds of
vibrations.

ee

CHAPTER V.

EARTHQUAKE MOTION AS DEDUCED FROM OBSERVATION ON
EARTHQUAKES.

Result of feelings—The direction of motion—Instruments as indicators
of direction— Duration of an earthquake— Period of vibration—The
amplitude of earth movements—Side of greatest motion—Intensity
of earthquakes—Velocity and acceleration of an earth particle—
Absolute intensity of an earthquake—Radiation of an earthquake—
Velocity of propagation.

Result of Feelungs.—As the result of our experiences,
and by observations upon the movements produced in
various bodies, we can say that an ordinary earthquake
consists of anumber of backward and forward motions of the
ground following each other in quick succession. Scm:2-
times these commence and die out so gently that those
who have endeavoured to time the duration of an earth-
quake have found it difficult to say when the shock com-
menced and when it ended. This was a difficulty which
Mr. James Bissett in Yokohama, and the author in Tokio,
had to contend against when, in 1878, they commenced
to time shocks between these two places.

Sometimes these motions gradually increase to a
maximum and then die out as gradually as they com-
menced.

Sometimes the maximum comes suddenly, and at
other times during an earthquake our feelings distinctly
tell us that there are several maxima.

68 EARTHQUAKES.

These have been the experiences of many observers,
and have been recorded by writers since the earliest times.
Mallet devotes a chapter to a consideration of the tremu-
lous motion that precedes and follows a shock, and he
tells us that a single shock is an absolute impossibility.
In speaking of earthquakes, he says: ‘ The almost universal
succession of phenomena recorded in earthquakes is, first
a trembling, then a severe shock, or several in quick suc-
cession, and then a trembling gradually but rapidly be-
coming insensible.’

A quantitative and exact knowledge a the nature of
earthquake motion has only been oad of late years.
The chief results which investigators have aimed at have
been the measurement of the amplitude, the period, the
direction, and the duration of the motions which constitute
an earthquake. Attention has also been given to the
velocity with which a disturbance is propagated.

The Direction of Motion.—One of the most ordinary
observations which are made about an earthquake is its ©
direction. If we were to ask the inhabitants of a town
which had been shaken by an earthquake the direction
of the motion they experienced, it is not unlikely that
their replies would include all the points of the compass.
Many, in consequence of their alarm, have not been able
to make accurate observations. Others have been de-
ceived by the motion of the building in which they were
situated. Some tell us that the motion had been north
and south, whilst others say that it was east and west. A
certain number have recognised several motions, and ~
amongst the rest there will be a few who have felt a

_ wriggling or twisting. Leaving out exceptional cases, the

general result obtained from personal observation as to the
direction of an earthquake of moderate intensity is ex-
tremely indefinite, and the only satisfactory information

FARTHQUAKE MOTION DEDUCED FROM OBSERVATION. 69

to be obtained is that derived from instruments or from
the effects of the earthquake exhibited in shattered build-
ings and bodies which had been overturned or projected.

By the direction in which walls, columns, and other
objects had been overthrown or fractured, Mallet was
enabled to determine the position of the origin of the
Neapolitan earthquake. Similar phenomena have many
times been taken advantage of by other investigators of
earthquake phenomena. Effects produced upon struc-
tures are, however, only to be observed as the results of
a destructive earthquake, at which time cities may be
regarded as collections of seismometers. (See chapter on
Effects in Buildings.)

To determine the direction of movement during a
small earthquake, the most satisfactory method appears
to be an appeal to instruments.

Instruments as Indicators of Direction.—The rela-
tive values of different kinds of instruments, such as
columns, pendulums, and the like, as indicators of direc-
tion have already been discussed.

_ By the use of pendulum seismographs it has been
shown that during an earthquake the ground may move
in one, two, or several directions (see p. 21); and it is,
generally speaking, only in those cases where we ex-
perience a decided shock in the disturbance that we can
determine with any confidence the direction in which the
motion has been propagated. Such directions are usually
indicated by the major axis of certain more or less ellip-
tical figures which have been drawn, which in themselves
appear to indicate the combination of two rectilinear
movements.

Results similar to those indicated by the records of
pendulum seismographs have also been obtained upon

moving plates with a double bracket seismograph. Thus,

70 EARTHQUAKES,

in the earthquake which shook Tokio at 6 a.m. on July 5,
1881, there were indications of the following motions : —

Near the commencement of the shock the motion was
N. 112° E. One anda half second after this, the direc-
tion of motion appears to have been N. 50° E. In three-
fourths of a second more it gradually changed to a
direction N. 146° E., and after a similar interval to N.
62° E. Half a second after this it was N. 132° E., and
four seconds later the motion was again in the original
direction—namely, N. 112° E.

These particular directions of motion have been
selected because they were so definitely indicated.

The commonest type of earthquake which is experi-
enced in Japan, and probably also in other earthquake-
shaken districts, is the compound or diastrophic form.

That earthquakes often have motions compounded of
two sets of vibrations, has also been proved by the ana-
lysis of the records obtained from two component seismo-
graphs. From an analysis of a record of this description,
Professor Ewing has shown that in the earthquake felt in
Tokio on March 11, 1881, there were approximate circular
(somewhat spiral) movements.

This leads us to the consideration of the twisting and
wriggling motions which are said to be experienced by
some observers. Motions like these, which by the Italians
and Mexicans are called vorticosi, are usually supposed to
be the cause of objects like chimneys and gravestones
being rotated. These phenomena, it will be seen from
what is said in the chapter upon the effects produced in
buildings, can be more easily explained upon the supposi-
tion of a simple rectilinear movement.

That at the time of an earthquake there may be
motion in more than one direction has been recognised
since the time of Aristotle; and it is possible that two sets

con aati

EARTHQUAKE MOTION DEDUCED FROM OBSERVATION. 71

of rectilinear motion, as, for instance, the normal and
transverse movements, may have led observers to imagine
that tuere has been a twisting motion taking place, and
this especially when the two sets of movements have
quickly succeeded each other.

Persons inside flexible buildings may possibly have
experienced more or less of a rotatory motion, although
the shock was rectilinear; the building assuming such a
motion in consequence of its construction and its position
with regard to the direction of the shock.

In the case of destructive earthquakes, especially at
points situated practically above the origin, the universal
testimony, Mallet tells us, is that a twisting, wriggling
motion in different planes, attended by an up-and-down
movement of greater range, is experienced. To such dis-
turbances the word sussultatore is sometimes applied.
Mallet has given many elliptical and other closed curves
to illustrate the nature of such motions.

Duration of an Earthquake.—When reading accounts

of earthquakes it is often difficult to determine the length
of time a shaking was continuous. In Japan, in A.D. 745,
there was a shaking which is said to have lasted sixty
hours; and in A.D. 977 there were a series of shakings
lasting 300 days. Often we meet with records of disturb-
- ances which have lasted from twenty to seventy days.

At San Salvador, in 1879, more than 600 shocks were
felt within ten days; in 1850, at Honduras, there were
108 shocks in a week; in 1746, at Lima, 200 shocks were
felt in twenty-four hours; at the island of St. Thomas, in
1868, 283 shocks were felt during about ten hours.

Disturbances like these, which succeed each other with
sufficient rapidity to cause an almost continual trembling
in the ground, may be regarded as collectively forming
one great seismic effort which may last a minute, an hour,

4

72 EARTHQUAKES.

a day, a week, or even several years. Strictly speaking,
they are a series of separate earthquakes, the resultant
vibrations of which more or less overlap. Whenever a
large earthquake occurs it is generally succeeded by a
large number of smaller shocks.

The seismic disturbance as regards time is, as Mallet
remarks, very often ‘like an occasional cannonade during
a continuous but irregular rattle of musketry.’ In the
New Zealand earthquake of 1848, shocks continued for
nearly five weeks, and during a large portion of the time
there were at least 1,000 shocks per day.!

The earthquake of Lisbon, which in five minutes
destroyed the whole town, was followed by a series of
disturbances lasting over several months. . After Basle
had, on October 18, 1356, been laid in ruins, it is stated
shocks followed each other for a period of a year. The
Calabrian earthquake was continued with considerable
strength for a year, and it is said that the earth did not
come completely to rest for ten years. During this can-
nonade the heavy shocks announced, as they do in most
earthquake countries at the present day, a series of weaker
disturbances. In certain exceptional cases this order of
events has been inverted, and slight shocks have an-
nounced the coming of heavy ones. Fuchs gives an ex-
ample of this in the earthquake of Broussa, when the first
shock was on February 28, 1855. On March 9 and 23
there were heavier shocks, but the heaviest did not arrive
until March 28.

Under certain conditions it is possible to have a
sensible vibration produced in the ground which is
practically of unlimited duration; thus, for instance, it
has been noticed that the falling of water at certain large
waterfalls, by its continuous rhythmical impact on the

1 West. Rev., July 1849.

3
a

EARTHQUAKE MOTION DEDUCED FROM OBSERVATION. 73

rocks, produces in them tremors which are to be observed
at great distances. Of this the author convinced himself
at the Falls of Niagara, where he observed the reflected -
and ever-moving image of the sun in a pool of water.
Under favourable circumstances almost continual conden-
sation of steam might take place in volcanic foci, each
condensation giving rise to a blow sufficiently powerful
to produce vibrations in the surrounding ground. Those
who have stood near a large geyser, like the one in
Iceland, when it makes an ineffectual effort to erupt,
will recognise how powerful such a cause might be.
Humboldt has remarked shocks on Vesuvius and Pichincha
which were periodic, occurring twenty to thirty seconds
before each ejection of vapour and ashes. |

Earthquakes like these may be of vast extent, gradu-
ally spreading further and further outwards. This
spreading of earth vibrations may be observed ata large —
factory containing heavy machinery or a steam hammer.
After the machinery comes to rest, it is probably some
time before the ground returns to rest. Examples of
disturbances of this nature are spoken of under the head
of Earth Tremors.

The record of the duration of an ordinary earthquake
as observed at a given point is dependent upon the sensi-
bility of our instruments.

Continuous motions perceptible to our senses without
the aid of instruments usually last from thirty seconds to

about two or three minutes, In Japan the shocks, as

timed by watches, usually last from twenty to forty seconds.
Occasionally a continuous shaking is felt for more than
one and a half minutes, and cases have been recorded where
the motion has continued for as much as four minutes and
thirty-three seconds.

Seismometers having a multiplication of 6 to 12

74 FARTHQUAKES.

usually indicate that motion continues longer than is
perceptible to the senses.
Period of Vibratton.—When an earthquake contains

several prominent vibrations which might be called the

shocks of the disturbance, our feelings tell us that these
have occurred at unequal intervals.

About the time which is taken for the complete back-
ward and forward oscillation of the ground which consti-
tutes the shock a little has already been said. This was
deduced from the records of disturbances as drawn by
selsmographs. From the same sources we can readily
obtain the period of all the prominent vibrations in a dis-
turbance. 7

In any given earthquake there are irregularities in
period, and different earthquakes differ from each other.
About the early attempts to determine the period of
earth vibrations something has been said in the chapter
on Earthquake Instruments. _

In the earthquake of March 11 (referred to on p. 70)
we find that both components commenced with a series
of small vibrations, about five or six to the second; next
came the shock, consisting of two complete vibrations
executed in two seconds. In this it is to be observed
that the motion eastwards was performed much more
quickly than the motion westwards. Next, by reference
to the east and west component, it is seen that there are
a number of large vibrations, about one per second, on
which a number of smaller motions are superposed. As
the motion proceeds, these become less and less definitely
pronounced and more irregular in their intervals, until
finally the motion dies away.

This earthquake, as recorded at the author’s house in
Tokio, lasted about one and a half minute.

- The same earthquake, as recorded by Professor Ewing

EARTHQUAKE MOTION DEDUCED FROM OBSERVATION. 75

at a station situated about one and a half mile dis- |
tant, but on flat ground, appears to have lasted four and
a half minutes. The largest wave had a period of 0:7
second. |

In the earthquake of March 8, 1881, there were on
an average 1:4 vibrations per second. These vibrations
were executed in a direction transverse to the line joining
the observing station and the locality from which the
disturbance must have originated as determined by time
_ observations. It can, therefore, be assumed that these
vibrations, having so slow a period, were transverse
motions, this slowness or sluggishness being due to the
fact that the modulus for distortion is less than the
modulus which governs the propagation of normal vibra-
tions.

The Amplitude of Karth Movements.—In making esti-
mates of the distances through which we are moved back-
ward and forward at the time of an earthquake, if we judge
by our feelings, we may often be misled. If a person is
out of doors and walking, an earthquake may take place
sufficiently strong to cause chimneys to fall and unroof
houses, which, so far as the actual shaking of the ground
is coucerned, will be passed by unnoticed. On the other
hand, to persons indoors, especially on an upper story, it is
impossible even for a tremor to pass by without creating
considerable alarm by the angular movement that has
- been taken up by the building.

Many observers have endeavoured to make actual
measurements of the maximum extent through which the
earth moves at the time of an earthquake. Among the
reports of the British Association for 1841 is the report
of a committee which had been appointed ‘for obtaining
instruments and registers to record shocks of earth-
quakes in Scotland and Ireland. We read that in one

76 FARTHQUAKES.

earthquake which had been measured the displacement
of the ground had been half an inch, and in another it had
been less than half an inch. The instruments used to
make these observations depended upon the inertia of
pendulums which at the time of the disturbance were
supposed to remain at rest. Observations similar to these
have been made in Japan. One long series were made
by Mr. E. Knipping for Dr. G. Wagener. They ex-
tended from November 1878 to April 1880, and were as
follows :-— |

Number of Maximum horizontal
Earthquakes motion of the ground
10 - . . : ° ‘0 to 015 mm.
7 ° e ° e C) 15 9 0°5 tb)
8 F : ° . ° PD ian, ben ORneieg
2 “ - - 5 2°55, more Ge

With his apparatus for vertical motion Dr. Wagener
also made observations on the absolute vertical motion.
This seldom reached °02 mm. The greatest value was that
observed for the destructive shock of Feb. 22, 1880,
which was °56 mm.

By means of a number of instruments distributed at
various localities round Tokio, the chief of which were
pendulums with friction pointers to render them ‘ dead.
beat,’ and with magnifying apparatus to show the actual
motion of the ground, the author arrived at results
similar to those obtained by Dr. Wagener—namely, that
the earth’s maximum horizontal motion at the time of a
small earthquake was usually only the fraction of a milli-
metre, and it seldom exceeded three or four millimetres.
When we get a motion of five or six millimetres, we
usually find that brick and stone chimneys have been
shattered.

The results obtained for vertical motion were also very
small. In Tokio it is seldom that vertical motion can be

EARTHQUAKE MOTION DEDUCED FROM OBSERVATION. 77

detected, and when it is recorded it is seldom more than a
millimetre.

These results, which were put forward some years ago,
have since received confirmation by the use of a variety
of instruments in the hands of different observers.

Mallet, in his account of the Neapolitan earthquake of
1857, approximated to the amplitude of.an earth particle
by observing the width, at the level of the centre of
gravity, of fissures formed through and remaining in great
masses of very inelastic masonry.

Taking stations situated on or very nearly on the same
line passing through the seismic vertical (epicentrum),
Mallet observed the amplitude increased as some function
of the distance, as will be seen from the following table :—

Station Polla La Sala Certosa |Tramutola} Sarconi

Distance from Seismic

Vertical in geographi- ; 3°45 | 11-60 16°50 20:60 | 26:7

cal miles.

Amplitude in inches Die 205 3°5 4:0 4:5 4°75

The possibility of a law such as this having an exist-
ence for places at a distance from the seismic vertical
comparable with the vertical depth of the centrum will be
shown farther on.

With regard to the maximum displacement of an
earth particle, Mallet was of opinion that there was evi-
dence to show that it had in some cases been over one
foot. M. Abella, in an earthquake which occurred in the
Philippines in 1881, made a rough observation of the
motion of the earth to a distance of about two metres.
This, as might be expected, was beyond the elastic limits
of the material, and caused fissures to be formed, which
were seen to open and shut.

Intensity of Earthquakes.—In speaking of the strength

78 EARTHQUAKES,

of an earthquake, we usually employ terms like ‘weak,’
‘strong,’ ‘violent,’ &c. Although these expressions, ac-
companied by illustration of the effects which an earth-
quake has produced, convey a general idea of the strength
of a shock as felt at some particular locality, our ideas are
nevertheless wanting in definiteness ; and if we endeavour
to compare one shock with another, as a whole, our want
of exactness is augmented. We have seen that Palmieri’s
seismograph indicates intensity by a certain number of
degrees, which, to a certain extent, is a measure of the
violence of the motion as indicated at a particular locality.
The degrees, as before stated, refer to the height to which,
in consequence of the shaking, a certain quantity of
mercury was washed in a tube, which is a function of the
depth of mercury in the tube, and also of the duration of
the disturbance.

From this it seems possible that a very slow motion
of small amplitude, continuing over a sufficient period of
time, might, if it agreed with the period of the mercury,
indicate an earthquake of many degrees of intensity,
whilst residents in the neighbourhood might not have
noticed the disturbance ; and, on the other hand, a short
but intense shock creating considerable destruction might
have been recorded as of only a few degrees of intensity.

Although objections like these might be raised to such
a method of recording intensity, in practice it would
appear that such results are not pronounced, and the
indications of the instrument usually give us approximate
indications of relative intensity.

In writing about the Neapolitan earthquake of 1857,
Mallet says that.‘ area alone affords no test of seismic
- energy.’

The area over which a shock is felt will depend not
only upon the initial force of the disturbance, but also

EARTHQUAKE MOTION DEDUCED FROM OBSERVATION. 79

upon the focal depth of a shock, the form and position of
that focus, the duration of the disturbance, and the nature
and arrangement of the materials which are shaken.
| From observations in Japan, it is clearly shown that
massive mountain ranges exert a considerable influence
upon the extension of seismal disturbances. On one side
of a large range of mountains large cities might be laid in
ruins, whilst on the other side the disturbance creating
this destruction might not be noticed.

Velocity and Acceleration of an Earth Particle.—
We now pass on to methods of determining the intensity of
an earthquake which are less arbitrary than those which
have just been discussed. These methods have already
been discussed when speaking of artificial disturbances,
where it was shown that the intensity of an earthquake as
measured by its destructive effects greatly depended upon
the suddenness with which the backward and forward
motions of the ground were commenced or ended.

Amongst the earlier investigators of seismic phe-
nomena who observed that there existed a connection
between the distance to which bodies had been projected
during an earthquake and the suddenness or initial
velocity with which the ground had been moved beneath
them, was Professor Wenthrop of Cambridge, Massachu-
setts, who noted that bricks from his chimneys had, by the
New England earthquake of 1755, been thrown thirty feet.
From this and the known height of the chimney, he calcu-
lates that the bricks had been projected with an initial
velocity of twenty-one feet per second.!

The calculations made by Mallet respecting the
maximum velocity of an earth particle at the time of the
Neapolitan earthquake in 1857 depended upon the over-
throw, projection, and fracture of bodies,

1 Phil. Trans., L., 1755.
5

80 EARTHQUAKES.

The principles which guided him in making these
calculations will be understood from the following illus-
tration.

If a column, ABCD, receive a shock or be suddenly

moved in the direction of the

Cc B
arrow, the centre of gravity,
G, of this column will revolve
round the edge, and tend to
O

describe the path ao. If it
L passes 0, the column will fall.
The work done in such a case
as this is equal to lifting the
~ column through the height
oh. |
If Ga=a, the angle
GAh= 4, and the weight
of the body = w, then the above work equals
wa (1 — cos ¢).
This must equal the work acquired—that is to say, the
kinetic energy of rotation of the body, or
Ww'K? —
wa (l—cos $) = al
Where w is the angular velocity of the body at start-
ing, K the radius of gyration round A, and g the velocity
acquired by a falling body in one second. Whence _
w* K2 = 2 ga.(1 — cos $), =
put w, the angular velocity, is equal to the statical couple
applied, divided by the moment of inertia, or,
va cos h
ar

D Aine
Fia. 14.

w= ;

squaring and substituting

K? l1l—e
Y= 29g x. — x i= cos b

EARTHQUAKE MOTION DEDUCED FROM OBSERVATION. 81

and since the length of the corresponding pendulum is
2

K
oe. ~
Geos eer
cos* ¢.

To apply this to any given case we must find the value
._ 72
of I or of *.
a

. Mallet finds these values for the cube, solid and hollow
rectangular parallelopipeds, solid and hollow cylinders,
&e. In these formule we have a direct connection be-
tween the dimensions and form of a body and the velocity
with which the ground must move beneath it to cause its
overthrow. 5

Not only is the case discussed for horizontal forces,
but also for forces acting obliquely. Similar reasonings
_ are applied to the productions of fractures in walls, but
as there is uncertainty in our knowledge of the co-
efficient of force necessary to produce fracture through
joints across beds of masonry, the deductions ought not
to be applied as the measures of
velocity. Where the fractures
occur at the base or in horizontal
planes, or in those of the con-
tinuous beds of the masonry, or
- through homogeneous bodies, the
uncertainty is not so great, and for
eases like these Mallet gives several

Se
illustrations. he distance to -.° Fig. 15.

which bodies had been projected,

as, for example, ornaments from the tops of pedestals,
coping-stones from the edges of roofs, were also used as
means of determining the angle at which the shock had

82 EARTHQUAKES.

emerged, or, if this be known, for determining the velo-
city.

Thus by a shock in the direction 0 ©, a ball, a, on the
top of a pedestal would describe a trajectory to the point Cc.
Let the angle which 0 c makes with the horizon be e, the
vertizal height through which the ball has fallen be 0,
and the horizontal distance of projection be a; then

9

a2
b=atane + Tee
H being the height due to the velocity of projection.
whence

2u+/4u(u+b)—-@

a

Tane=

act a? 9
~ 2 cos? e(b — a tan e)
For the back motion or subnormal wave in the direc-
tion C 0,
out /futetb)—@
a

Be Lng) ;
2 cos? e(b + a tan e)

Tane=

A serious error which may enter into calculations of
this description when practically applied has been pointed
out when speaking of columns as seismometers. It was
then shown that such bodies before being overthrown
may often be caused to rock, and therefore that their final
overthrow may not have any direct connection with the
impulse of the succeeding shock.

Another point to which attention must be drawn
respecting the above calculations is that if there was no
friction or adherence between the projected body and its

a
we

;

EARTHQUAKE MOTION DEDUCED FROM OBSERVATION. 83

pedestal, in consequence of its inertia it would be left
behind by the forward motion of the shock, and simply
drop at the foot of its support. In the case of frictional
adherence it would be carried forward by the velocity ac-
quired before this adherence was broken, and thrown in a
direction opposite to that given in the figure—that is to
say, in the direction of the shock.!

The Absolute Intensity of the Force exerted by an
Earthquake.—No doubt it has occurred to many who have
experienced an earthquake that the power which gave
birth to such a disturbance must have been enormously
great. The estimates which we shall make of the abso-
lute amount of energy represented by an earthquake
cannot, on account of the nature of the factors with
which we deal, be regarded as accurate. They may, how-
ever, be of assistance in forming estimates of quantities
about which we have at present no conception. One
method of obtaining the result we seek is that which was
employed by Mallet in his calculations respecting the
Neapolitan earthquake. Although disbelieving in the
general increment of temperature as we descend in the
earth at an average rate of 1° F. for every fifty or sixty
feet of descent, for want of better means, Mallet assumes
this law to be true, and, knowing from a variety of
observations the depth of various parts of the cavity from
which the disturbance sprang, he calculates the tem-
peratures of this cavity in various parts as due to its
depth beneath the surface. Next, it is assumed that
steam was suddenly admitted into this cavity, which might
exert the greatest possible pressure due to the maximum
temperature. This was calculated as being about 684
atmospheres.

_ 1 The solution is taken from Mallet’s Account of the Neapolitan
Harthquake, vol. i. p. 155.

84 - EARTHQUAKES.

Next, he determined the column of limestone necessary
to balance such a pressure, which is about 8,550 feet in
height. As the least thickness of strata above this cavity
was 16,700 feet, the pressure of 684 atmospheres was not
sufficient to blow away its cover, but if suddenly admitted
or generated in the cavity it might have produced the
wave of impulse by the sudden compression of the walls
of the cavity.

The pressure of 684 atmospheres is equivalent to
about 4°58 tons on the square inch, and, as the total area
of the walls of the cavity is calculated at twenty-seven
square miles, the total accumulated pressure would be
more than 640,528 millions of tons. Mallet, however,
shows that it is probable that the temperature of the
focal cavity was much greater than that due to the
hypogeal increment, and that therefore the pressure may
have been greater.

The capability of producing the earthquake impulse,
however, depends on the suddenness with which the steam
is flashed off. According to the experiments of Boutigny
and others, Mallet tells us that the most sudden produc-

- tion of steam would take place at a temperature of 500°—

550° C., which is but a few degrees below that calculated
for the mean focal depth.

Assuming the above calculated pressure to be true,
and knowing the co-efficient of compression of the
materials on which it acted, the volume of the wave at a
given moment near the instant of starting—that is, at the
focus—can be calculated, and from this the wave amplitude
on reaching the surface may be deduced.

Proceeding backwards, if we have observed the wave

amplitude, calculated the depth of the focus, and know.

the co-efficient of expansion, then the total compression

a ee ea ae

EARTHQUAKE MOTION DEDUCED FROM OBSERVATION. 85

may be calculated and the temperature due to the pressure
producing this may be arrived at. In this way earthquakes
may be used as a means of calculating subterranean
temperature at depths that can never be attained experi-
mentally.

A method of proceeding which is probably more
definite than that adopted by Mallet would be the
application of the method indicated when speaking of
the intensity of artificial disturbances.

If for a given earthquake the origin of which is known
we have determined by seismographs the mean acceleration
of an earth particle at two or more stations at different
distances from that origin, we are enabled to construct
a curve of intensity the area between which and its
asymptotes was shown to bea measure of the total intensity
of the shock. Comparing this area with that of a unit
disturbance produced, say, by the explosion of a pound of
dynamite, one may approximately calculate in terms of
this unit the initial intensity of the earthquake.

Radiation of an Earthquake.—The tremors preceding
the more violent movements of an earthquake may be
due, as Mallet has suggested,! to the free surface waves
reaching a distant point before the direct vibrations.

The fact that earth vibrations produced by striking a
blow on or near the surface of the ground are wholly
cbliterated in reaching a cutting or valley, there being no
underground waves of distortion to crop up on the oppo-
site side of the valley, indicates that the disturbance is
one that travels on the surface; the same fact is illus-
trated when we endeavour to transmit vibrations through
the side of a hill into a tunnel.

In the tunnel, although the distance may be small,

1 Neapolitan Earthquake, ii. p. 300.

86 EARTHQUAKES.

no sensible effects are produced, whilst the same disturb-
ance may be recorded at a long distance from its origin
on the surface of the ground outside the tunnel.

Lastly, we may refer to the experiences of miners
underground.

Occasionally it has happened that miners when deep
underground, as in the Marienberg in the Saxon Erzge-
birge, have felt shocks which have not been noticed on the
surface. These observations are rare, and it is possible
that they may be explained by the caving in of subter-
ranean excavations.

The usual experience is, that if a shock is felt
underground it is also felt on the surface, as for example
in the lead mines in Derbyshire at the time of the
Lisbon disturbance (1755).

The most frequent observation, however, is that a
shock may be felt on the surface while it is not remarked
by the miners beneath the surface, as at Fahlun and
Presburg in November, 1823.

At the Comstock Lode in Colorado about twelve
years ago many earthquakes were felt. On one par-
ticular day twenty-four were counted. Superintendent
Charles Foreman told the author when he visited
Virginia City in 1882, that special observations were
made to determine whether these shocks were felt
as severely deep down in the mines as on the surface,
where they were on the verge of being destructive.
The universal testimony of many observers was that in
most cases they were not felt at all underground, and
when a shock was felt it was extremely feeble. At
Takashima Colliery, in Japan, it is seldom that shocks
are felt underground.

The explanation of these latter observations appears
to be either that, in consequence of a smaller amplitude

EARTHQUAKE MOTION DEDUCED FROM OBSERVATION. 87

of motion in the solid rocks beneath the surface as
compared with the extent of moticn on the surface, the
disturbances are passed by unnoticed, or else the dis-
turbance is, at a distance from its origin, practically
confined to the surface.

Velocity of Propagation of an Earthquake.—Although.
many have written upon earthquakes and have endea-
voured to give to us the velocity with which they were
propagated, the subject is one about which we have as
yet but little exact information.

The importance of this branch of investigation is
- undoubtedly great. By knowing the velocity with which
an earthquake has travelled in various directions we are
assisted in determining the locality of its origin; we may
possibly make important deductions respecting the
nature of the medium through which it has passed;
perhaps also we may learn something regarding the
intensity of the disturbance which created the earth-
quake. In the Report of the British Association for
1851 Mallet gives the table on next page, in which are
placed together the approximate rates of transit of shocks
of several earthquakes which he discusses. Some of
_ these, it will be observed, are records of disturbances
which must have passed through or across the bed of the
ocean.

In Mallet’s British Association Report for 1858, he
gives data compiled by Mr. David Milne! respecting the
Lisbon earthquakes of 1755 and 1761, from which data
the tables of velocities (p. 89) have been calculated,
omitting those which Mr. Mallet has marked as un-
certain.

The distances are marked in degrees of seventy

1 See Hdinburgh Phil. Trans., vol. xxxi.

| 88 EARTHQUAKES.

‘| Formation constituting Range

. Occasion and Place ae ae on surface as far as known or Authority
ea conjectured
Rev. John Mitchell’s| 1,760 |Sea bottom, probably on | Mitchell
guesses trom the slates, secondary and
Lisbon earthquakes crystalline rocks
Von Humboldt’s| 1,760 | From observations in va-} Humboldt
guesses from South} to rious South American
America 2,464 | rocksin great part vol-
canic
Lishon Earthquake
of 1761.
Lisbon to Corunna {1,994 | Transition, carboniferous| ‘ Annual
and granitoid Register ’
Lisbon to Cork 5,228 | Transition, carboniferous he
crystalline slates and
granitoid, probably,
under sea bottom
Lisbon to Santa Cruz| 3,261 |The same with many SS
alterations
Antilles.
Pointe a Pitre t0|6,586 | Probably volcanic rocks| Stier and
Cayenne (doubtful) under sea bottom Perrey’s me-
morandum,
Dijon
India.
-Cutch to Calcutta,|1,173 | Alluvial, secondary, grani- ‘Royal
1819 toid and later igneous Asiatic
: rocks Journal ’
India, Nepauls, and
basin of the Ganges,
1834 :—
Rungpur to Arrah 2,314 : .
4 B. Deep alluvia, with occa-| ‘ Royal
aa to Gorack- |3,520 sional transition, car-} Asiatic
boniferous granitoid,} Journal’
Rungpur to Monghyr| 9°0 Bs ‘
Rungpur to Calcutta|1,210 BURR IE ES Oe
Ships ‘Rambler’ and|1,056 |Sea bottom resting on| ‘ Nautical

‘Millwood,’ at sea,
1851; between Jat.
16° 30’ N.L., 54° 30’
W., and lat. 23° 30’
N.L., 58° 0’ W.

unknown rock

Magazine ’

EARTHQUAKE MOTION DEDUCED FROM OBSERVATION. 89

THE LISBON EARTHQUAKE OF NOVEMBER 1, 1755.

Moment ob- | Distance from | Velocity in feet
served of shock |presumedorigin| per second

Localities

Ing Tay. ° ’
Presumed focus of shock, } 9 93 a en
lat. 30°, long. 11° W.
A ship at sea in lat. 38°, |)
long. 10° 47’ W. sell oes Ota a
Colares - : 9 30 1 30 1,325
Lisbon . : - Z Sa it eo 1,020
Oporto . ° ° . 9 38 2 30 1,030
Ayamonte ° - 9° 50 4 0 916
Cadiz a “ 9 48 a. O 1,236
Tangier and Ween é A 9 46 DSU 1,478
Madrid A 9 43 6 O 1,855
Funchal : - - LO oT 8 30 _ 1,382
Portsmouth - - . HOF’ 73 12 30 1,431
Havre : - - F 10 23 13 (OO 1,339
Reading “ ; . LOS 27 13 30 1,304
| Yarmouth. 5 _ 10 42 Te alg, 1,174
Amsterdam . ‘ ; 10 6 17 <0 2,444
Loch Ness E ‘ 10 42 18 O 1,409

THE LISBON EARTHQUAKE OF MARCH 31, 1761.'

_ 9 = i locity in feet
Locality ae ee eet eee i eoeond
hoy me ° t

Presumed focus, lat. 43°, il 51

long. 11° W. a ea
Ship at sea in lat. 43°,

many leagues from coast \ ll 52 0 30 3,091

of Portugal
Ship in lat. 44° and about

80 leagues from coast ~ ett HL be gee pele
erea a F 11 dl 2 30 2,076
Ship lat. 44° 8’ and 80

leagues NNW. of mee \ 11 58 3 30 3,091

Finisterre
Lisbon - ; ; noon 4 30 3,091
Madeira . : - : 16 10 O 4,122
Cork . 3 - , : 12 11 9 30 2,937

English miles each, and the time is reduced to Lisbon
time.
_ These tables, owing to the nature of the eae

1 See Report of British Association, 1858, p. 10.

90 EARTHQUAKES.

which Mallet had at his disposal, are but rude approxi-
mations to the truth. Two interesting facts are, how-
ever, observable: the first being that the velocities for
the earthquake of 1761 are much higher than those
obtained for the earthquake of 1755; and, secondly, that in
both cases the velocities as determined from the observa-
tions of ships at sea closely approximate to each other,
in all cases being nearly the same as that with which a
sound wave would travel through water.

The great differences in transit velocity obtained for
different earthquakes is a point worthy of attention.

Seebach’s velocity is a true transit velocity, and its
determination is dependent on the assumption that the
shock radiated from the centrwm and not from the epi-
centrum. Seebach’s method is explained when speaking
about the determination of origins.

Some interesting observations on the velocity with
which the earthquake of October 7, 1874, was propagated,
are given by M.S. di Rossi.!

_ One assumption is that the disturbance radiated from
an origin to surrounding points of observation, whilst
another is that the disturbance followed natural fractures,
the direction of which is derived from the crest of certain
mountain ranges. These velocities are as follows, Maradi

_ being at or near the origin of the disturbance :—

Velocity in feet per second with Velocity in feet per second by propagation
direct radiation along mountain chains
Modigliana ° . 820] By the Valley of Marenzo . 1,080
Bologna . ° - 6567 ,, 9 Saveno - 1,080
Horii. 5 5 o (O74. “5 Montone . 1,080
Modena . 4 e LOLS A. <5 ss Panaro F { me
Firenze . 5 AO Oe a Sieve . 5 540

Compiobbi i Bu BOM Se ss Be 5 Bau

1 Meteorologia Endogena, i. p. 306.

ear

EARIHQUAKE MOTION DEDUCED FROM OBSERVATION. 91

Another set of interesting results are those of
P. Serpieri on the earthquake of March 12, 1873. The
curious manner in which this shock radiated is described
in the chapter on the Geographical Distribution of Earth-
quakes (see p. 231). Two large areas appear to have been
almost simultaneously struck, so that, there being no time
for elastic yielding, the velocities calculated between places
situated on either of the areas are exceedingly great.!

From Ragusa to Venice the velocity was 2,734 feet per second

» Spoleto ss Hs 4 Oils x

» Perugia to Orvieto » 601 ,,- -

” ” », Ancona 99 1,640 5, ”
1,640

32 29 99 Rome 39 { or 2,186 99 29

The following are examples of approximate earth-
quake velocities which have been determined in Japan.

The Tokio Earthquake of October 25, 1881.—From re-
cords respecting this earthquake it appears to have been
felt over the whole of Yezo and the northern and eastern
coast of Nipon, a little farther south than Tokio. It was
severest at Nemuro and Hakodate, and at the former place
a little damage was done. From these facts, together
with the indications of instruments recording direction of
movement and a general inspection of the time records,
it seems that the disturbance must have originated beneath
the sea on the east coast of Yezo at a very long distance
to the north-east of Tokio, from which place it passed in
a practically direct line on to Yokohama.

As the disturbance was felt at Yokohama twenty-one
seconds later than at Tokio, and the distances between ~
these two places is about sixteen geographical miles, for
this portion of its course the disturbance must have
travelled at a rate of at least 4,300 feet per second. If

} See remarks on the Earthquake ‘ Push,’ p. 162.

92° 4.0, 023”, ABARPHQUAKES,

‘we assume that the shock, after having reached Hakodate,

travelled on at the same rate as it did between Tokio and
Yokohama in order to reach Saporo, where the shaking
was felt eighteen seconds after Hakodate, it must have
had about thirteen geographical miles to travel after
Hakodate was shaken before Saporo felt its effect.

_ Drawing from Hakodate a tangent to the eastern side
of a circle of thirteen miles radius described round
Saporo, the origin of the disturbance must be on the line
bisecting this tangent at right angles. As it also lies on
a line drawn through Tokio and Yokohama, it les in a
position about 41 N. lat. and 144° 15’ E. long., which
is a position somewhat nearer to Nemuro than Hakodate,
as we should anticipate. If this be taken as approximately
indicating the origin, then the shock, after reaching
Hakodate from the Hakodate homoseist, travelled about
218 miles to reach Tokio in 128 seconds, which gives a
velocity of 10,219 feet per second.

The method here followed is equivalent to that of the
hyperbola and one direction (see p. 204). The hyperbola
is described on the assumption that the velocity deduced
from the time taken to travel between Tokio and Yokohama
is correct, and also that the earth waves travelled with
approximately the same velocity in the vicinity of Saporo
as near Tokio. The probability, however, is that they
travelled more quickly. If this be so, then the origin is
thrown somewhat to the south-east and the velocity
between the Hakodate homoseist and Tokio reduced.
Thus, if the velocity in the Saporo district be double that

observed in the Tokio district, the origin is shifted about

twenty-eight miles to the south-west, and the last-men-
tioned velocity is reduced to about 9,000 feet per second.

If we work by the method of circles, and assume the
velocity to have been constant in all directions, then this

ae ae Oe cape ir ae ae

EARTHQUAKE MOTION DEDUCED FROM OBSERVATION. 93.

velocity must have been about 6,000 feet per second. If
we assume that the indications of direction obtained from
seismographs and other sources give to us by this intersec-
tion a proper origin, the velocity in some directions may
have been as much as 17,000 feet per second.

An origin thus determined, or even if determined by
the method of circles, is in discord with the fact that
places like Nemuro, in the north-east of Yezo, were nearer
to the origin than any of the other places which have been
mentioned. |

The conclusion which we are therefore led to with
regard to this shock, assuming of course that the time
observations are tolerably correct, is that the velocity of
propagation was variable, being greater when measured
between points near to the origin than between points at
a distance. The velocities estimated vary between 4,000
and 9,000 feet per second.

In the case of the earthquake which has just been
discussed, we have an example of a disturbance which must
have passed between Tokio and Yokohama in what was
almost a straight line from the origin. As this direction
ought to give the maximum time of transit if all earth-
quakes are propagated with the same velocity, the fol-_
lowing table is given of the interval between the time of
observation of several shocks at these two stations :—

From YOKOHAMA TO TOKIO. FRoM TOKIO TO YOKOHAMA.
1880 December 20th 36seconds ,; 1882 October 25th . ° 21 seconds
1881 January 7th 14-31 _,, 1883 February 6th . 23 ,,

>» March 8th EGO 7 ts, » March 1 B73) 3
Py ” 17th . 66 9 99 Ln & tenes: . 63 9
» November 15th 31 a os er Stee 2a 35
1882 February 16th 22 BS +3 ar Wektela 7 226 p

As these are observations which have been made with
the assistance of a telegraphic signal daily employed to

94 EARTHQUAKES.

correct and rate the clocks from which the observations.
were obtained, they may be regarded as being tolerably
correct.

The disturbance of February 6, the two shocks of
March 1, appear, like that of October 25, to have passed in
almost a direct line from an origin in the N.N.E, through
Tokio on to Yokohama. Their velocities of propagation
as calculated from the above intervals are approximately
3,900, 1,900, and 1,400 feet per second. The shock of
February 16 appears to have had its origin near to a point
in Yedo Bay about eight miles east of Yokohama.
Assuming this to be the case, the shock between the
Yokohama homoseist and Tokio travelled at the rate of
2,454 feet per second, but between the Tokio homoseist and
Chiba at the rate of 750 feet per second ; that is to say, the
velocity of propagation rapidly decreased as the disturbance
spread outwards.

At Yokohama it was recorded at 5.31.54, at Tokio at
5.32.16, and at Chiba at 5.33.48. These times are given
in Tokio mean time.

The shock of March 11, which was recorded at Tokio
at 7.51.22 p.m. and at Yokohama at 7.51.33 P.M., appears,
from the indications of instruments which were exception-
ally definite in their records, to have originated in the N.E.
corner of Yedo Bay, about nineteen miles S.S.W. from
Chiba. This shock was rather severe, fracturing several
chimneys. From the Tokio homoseist it appears to have
travelled on to Yokohama at the rate of about 2,200 feet
per second. Assuming these observations to be approa-
mately accurate, if we take them with the records of
previous observers they lead us to the following conclu-
sions :—

1. Different earthquakes, although they may travel

across the same country, have very variable velocities,

fi i
epee eee ee ee Oe ee _

|
|
4
;
}

_ EARTHQUAKE MOTION DEDUCED FROM OBSERVATION. 95

_ varying between several hundreds and several thousands

of feet per second.
«2, The same earthquake travels more quickly across

i districts near to its origin than it does across districts

| which are far removed.

| -—s-3«.' The greater the intensity of the shock the greater

me is the velocity.

96 EARTHQUAKES,

CHAPTER VI.

EFFECTS PRODUCED BY EARTHQUAKES UPON BUILDINGS.

Buildings in Tokio—Relation of destruction to earthquake motion—
Measurement of relative motion of parts of a building shaken by an
earthquake—Prevention of cracks—Direction of cracks—The pitch
of roofs—Relative position of openings in a wall—The last house
ina row—The swing of buildings—Principle of relative vibrational
periods.

:
|
The destruction of buildings is not irregular—Cracks in buildings—
|

THE subject of this chapter is, from a practical point of
view, one of the most important with which a seismologist
I | has to deal. We cannot prevent the occurrence of earth-
| | quakes, and unless we avoid earthquake-shaken regions,
| we have not the means of escaping fromthem. What we
| can do, however, is in some degree to protect ourselves.
| By studying the effects produced by earthquakes upon
buildings of different construction and variously situated,
we are taught how to avoid or at least to mitigate calamities
which, in certain regions of the world, are continually
repeated. The subject is an extensive one, and what is
here said about it must be regarded only as a contribution
to the work of future writers who may give it the atten-
tion it deservedly requires.

The Destruction produced by Earthquakes is not
urregular.—lIf we were suddenly placed amongst the
ruins of a large city which had been shattered by an
earthquake, it is doubtful whether we should at once

EFFECTS PRODUCED UPON BUILDINGS. 97

recognise any law as to the relative position of the masses
of débris and the general destruction with which we are
surrounded. The results of observation have, however,
shown us that, amongst the apparently chaotic ruin pro-
duced by earthquakes, there is in many cases more or
less law governing the position of bodies which have
fallen, the direction and position of cracks in walls, and
the various other phenomena which result from such
destructive disturbances. 3

Mallet, at the commencement of his first volume, de-
scribing the Neapolitan earthquake of 1857, discusses the
general effect produced by various shocks upon differently
constructed buildings. First he shows that, if we have
a rectangular building, the walls at right angles to the
shock will be more likely to be overthrown than those
which are parallel to it. Experience teaches a similar
lesson. Thus Darwin, when speaking of the earthquake
at Concepcion in 1835,' tells us that the town was built in
the usual Spanish fashion, with all the streets running at
right angles to each other. One set ranged S.W. by W.
and N.E. by E. and the other N.W. by N. and S.E. by 8.
The walls in the former direction certainly stood better
than those in the latter. The undulations came from
the 8.W. |

In Caraccas it is said that every house has its laga
securo, or safe side, where the inhabitants place their
fragile property. This laga securo is the north side, and
it was chosen because about two out of every three de-
structive shocks traversed the city from west to east, so
that the walls in these sides of a building have been
stricken broadside on.?

1 See Researches in Geology and Natural History, p. 374.
2 «The City of Harthquakes,’ H. D. Warner, Atlantic Monthly, March,
1883. halle . ; ev ee eae

98 EARTHQUAKES.

Cracks in Buildings.—Results like the above come
from destructive earthquakes rather than from movements
such as those we have to deal with ordinarily. Whena
building is subjected to a slight movement it is assumed
that the walls at right angles to the direction of the shock
move backwards and forwards as a whole, and there is
little or no tendency for them to be fractured at their
weaker parts, these weaker parts being those over the
various openings. The walls, however, which are parallel
to the direction of the movement are, so to speak, extended
and contracted along their length, and in consequence
they may be expected to give way over the various open-
ings. This tendency for extension and contraction of a
wall along its length may be supposed, for instance, to be
due to the different portions of a wall, owing to differences
in dimensions and elasticity, having different periods of
natural vibration, or possibly for two portions of a long
line of wall to be simultaneously affected by portions of
waves in different phases.

As an illustration of the giving way of a building in —
the manner here suggested we may take the case of a
large brick structure which was recently being erected in
Tokio. This building, at the time of the earthquake, was
only some fourteen or fifteen feet above the surface of the
ground. ‘The length of the building stretched from N.W.
to 8.E., and it was intersected by many walls at right
angles to this direction. Through all the walls of this
building there were many arched openings. In the
central part of the transverse walls, which walls were
fully five feet in thickness, the arches which joined them |
together were 4 feet 4 inches in thickness. The arches
therefore formed a comparatively lightly constructed link
between heavy masses of brickwork.

On March 3, 1879, at 4.43 P.M., an earthquake was

EFFECTS PRODUCED UPON BUILDINGS. 99

felt throughout Tokio, the strength of which, as judged
by our feelings, was above that of an average shock. As
registered by one of Palmieri’s instruments, it had a
direction 8.S.W. to N.N.E. and an intensity of 11°. On
the same day there were several smaller shocks having
the same direction, and these were succeeded by others
on the 9th of the month.

Immediately after these shakings it was discovered
that almost every arch in the internal walls of the build-
ing here referred to had been cracked across the crown
in a direction about N. 40° W. All the other arches of
the building, of which there were a great number in walls
at right angles to the direction of the shock, were found
not to have sustained any injury. To this statement,
however, there was one exception, which was subsequently
proved to have been due to a settlement taking place.

After examining these cracks the only cause to which
they could be attributed was the series of shakings which
they had just experienced. It seemed as if the heavy
walls right and left of the arches had been in vibration
without synchronism in their periods, and as a conse-
quence the arches which connected them had been torn
asunder.

Although the time at which the cracks were formed
and the peculiar positions in which they were only to be
found pointed distinctly to their origin, to be certain that
they were not due to settlement of the foundations, hori-
zontal lines were ruled upon the brickwork and from time
to time subsequently observed.

The points to which the various cracks extended were
also marked and observed. Beneath the walls as founda-
tions there were beds of concrete about three feet thick
and about ten feet. im width. These had been under the
pressure of the partially built walls for two years before

100 - EARTHQUAKES,

the arches had been put in. As these foundations were
unusually strong, being intended to carry so very much
greater weight than that to which they had been subjected,
if any settlement had been detected it would have been a —
matter of surprise.

Some weeks after the formation of these cracks it was
observed that they gradually closed. This was probably
due to the gradual falling inwards of the two broken por-
tions of the arch, their position when open being one of
instability.

Had this building been more complete at the time of
the shock, and the heavy walls been tied together at
higher points, although the archways would have been
points of weakness, it is quite possible that fracture would
not have taken place. This illustration shows us that when
a building is shaken in a definite direction there will be

some rule as to the positions in
which fractures occur. As an-
other example, we may take the
observations of Alexander Bittner
upon the buildings of Belluno
after the shock of June 29, 1873
(see Beitrige zur Kenntniss des
Erdbebens von Belluno am 29
Juni, 1873, p.40. Von Alexander
Bittner. Aus dem LXIX. Bande
der Sitzungsb. der K. Akad. der
Wissensch., II. Abth., April-
Fig. 16.—Cracks in a corner Heft. Jahrg. 1874).
sel ae Speaking generally, he re-
| marks that ‘Houses similarly
situated-have suffered in corresponding walls and corners
in a similar manner. In Belluno there is a certain kind
of damage which is repeated everywhere, making a pecu-

EFFECTS PRODUCED UPON BUILDINGS. 101

e liar system of splits in the S.W. and N.E. corners of
_ the houses.’ This is well shown in the accompanying

a sketch, which evidently illustrates the effect of a shock
oblique to the direction of two walls at right angles to

each other.

= Buildings in Tokio.—For the purpose of finding out
what has been the effect produced by earthquakes upon
_ the buildings of Tokio, and at the same time for ascer-
_ taining whether blocks of buildings ranging in different

_ directions suffered to the same extent, the author ex-

amined, in company with Mr. Josiah Conder, a large

i number of foreign-built houses in the district of the Ginza.

_ The chief reason for choosing this was because it was the

2a only district where a

a of different construc-
tions, the effects pro-

earthquakes are very

q many differences that
it becomes almost an —

large number of simi-
lar buildings could be
_ found. By examining
houses or buildings

duced upon them by

often likely to show so

Fic. 17.—Brick = buildings i in Tokio, skye
showing fractures.

=. impossibility to deter- - ~
- mine what the general ative has been—unsymmetrical
construction involving unsymmetrical ruin. :
A number of similarly constructed buildings in one
locality may be regarded as a number of seismographs,
the effect upon any one of them being judged of by the
average of the general effect which has been produced
upon the whole. The general form of two of these houses
which were examined is shown in fig. 17. In this figure

102 EARTHQUAKES,

the general character of the fractures which have been
produced can also be seen. The housesare built of brick,
and are in many cases faced with a thin coat of white
plaster. Projecting from the level of the upper floor
there is a balcony fronted by a low balustrade. This is
supported by small beams which at their outer extremity
are carried on a row of cylindrical columns. This forms
a covered way in front of each row of houses. The roofs
are covered with thick tiles. It will be observed that the
arches of the upper windows spring sharply from their
abutments, and at their crown they carry a heavy key-
stone. The lower openings, which have a span of 9
feet, have evidently been constructed in imitation of the
open front of an ordinary Japanese house. These arch-
ways curve out gently from their abutments. The out-
side walls have a thickness of 134 inches.

The results obtained from a careful examination of
174 houses in streets running N.E. and 156 houses in
streets running N.W., all of these houses being similar,
were as follows :-—

1. In the upper windows nearly all the cracks ran
from the springing, which formed an angle with the
abutment.

2. Inthe lower arches, whichcurved intothe abutments,
not a single crack was observed at the springway. The
cracks in these arches were near the crown, where beams
projected to carry the balcony. In many instances the
eracks proceeded from such beams, even if there were no
arch beneath. That cracks should occur in peculiar
positions, as is here indicated, is shown in the illustrations
which accompany the accounts of many earthquakes.

3. The houses which were most cracked were in the
streets running parallel to the direction in which the
greater number and most powerful set of shocks cross
the city.

EFFECTS PRODUCED UPON BUILDINGS. 103

The results showed that, in order to avoid the effects
of small shocks, all walls containing principal openings
should be placed as nearly as possible at right angles to
the direction in which the shocks of the districts usually
travel. The blank walls, or those containing unimportant
openings, would then be parallel to the direction of the
shocks—that is, presuming our building to be made up of
two sets of walls at right angles to each other.

Another point of importance would be to build arch-
ways curving into the supporting buttresses; the archways
over doors and windows which we find in earthquake
countries do not appear to be in any way different from
those which are built in countries free from earthquakes.
In the one country these structures have simply to with-
stand vertical pressures applied statically; in the other,
they have to withstand more or less horizontal stresses,
applied suddenly.

Relation of Destruction to Bartlquake Motion.—The
relations which exist between the overturning and pro-
jection of bodies and the motion of the ground have
already been discussed. It may be interesting to call
attention to the fact that in the formule showing three
relationships, it was the shape rather than the weight
of a body which determined whether it should be over-
turned or projected by a motion at its base.

As an interesting proof that light bodies may be over-
turned as easily as heavy ones, Mallet refers to the over-
turning of several large haystacks as one of the results
of the Neapolitan earthquake.

If masses of material are displaced or fractured, then
Mallet remarks that the maximum velocity will exceed
s/2yh, where his the amplitude of the wave. Should the
maximum velocity be less than this quantity, the masses
which are acted upon will be simply raised and lowered,
6

104 EARTHQUAKES.

and there will be no relative displacements even if the
emergence of the wave be nearly or quite vertical.

When we get a vertical wave acting upon an irregular
mass of masonry, the heavier portions of the masonry, by
their inertia, tend to descend relatively to the remaining
portions, and in this way vertical fissures will be pro-
duced. For this reason it would not be advisable to use
heavy materials above archways, heavy roofs, or heavy
floors. The vertical fissures, Mallet remarks, would have
their widest opening at the base.

In considering cases of fracture produced by earth-
quake motion, it must be remembered that these are due
to stresses applied suddenly, and that if the same amount -
of stress had been slowly applied to a building, fractures
might not have occurred.

If a disturbance is horizontal, and has a direction
parallel to the length of a wall, the wall is carried forward
at its foundations. This motion is opposed by the inertia
of the upper portion of the wall and the various loads it
carries. The wall being elastic, distortion takes place,
and cracks, which are widest at the top, will be formed.
In a uniform wall the two most prominent fissures ought
to be near the ends.

If the horizontal backward and forward movement has
a direction oblique to the plane of the wall, the wall will
be either overthrown, fractured, or have a triangular frag-
ment thrown off towards the origin from the end last
reached. |

Should the wave emerge steeply, diagonal fissures at
right angles to the direction of transit will be formed, or
else triangular pieces will be projected.

The accompanying figures are reduced from Mallet’s
‘Account of the Neapolitan Earthquake of 1857.’

Taking a b as the general direction of the fractures in

105

‘Gorey ezusqog ‘yornyo yerpoyyeO—'sT “PTT

EFFECTS PRODUCED UPON BUILDINGS.

106 EARTHQUAKES.

fig. 18, then ¢ d will represent the direction in which the
shock emerged, which is at an angle of 23°-20’ to the
horizon. It might be argued that the direction of these
fractures was due to the direction in which surface undu-
lations had travelled, or to the relative strengths and

=
= ite ap on

quake of 1857.

proportions of different portions of the building. The
directions of cracks in a building are undoubtedly due to a
complexity of causes, but for buildings situated in the
region of shock the impulsive effect of the shock is pro-

EFFECTS PRODUCED UPON BUILDINGS. 107

bably the most important function to be considered.
The method of applying the directions of emergence,
- deduced from observations on fractures, to determine the
origin of a disturbance will be referred to in Chapter X.

Mallet observed that, although two ends of a building
might be nearly the same, the fissures and joints do not
occur at equal distances from the ends, nor are they
equally opened.

The end where the joints are the most opened is that
which was first acted upon, and this phenomenon may be
sufficiently well pronounced to indicate the direction in
which we must look to find the origin of a disturbance.
Amongst possible explanations for this disposition of frac-
tures in a wall, Mallet suggests that they may be due to
real differences in the two semiphases of the wave of
shock, the second semiphase being described with a some-
what slower velocity than the first. This, it will be ob-
served, is contrary to the indications of seismographs.
Fig. 19, of the cathedral at Paterno, shows the effect

of a subnormal shock striking a wall obliquely and pro-
jecting one of its corners.

MEASUREMENTS OF THE RELATIVE MOTION OF PARTS OF A
BUILDING AT THE TIME OF AN EARTHQUAKE.

In 1880 a series of observations was made in Tokio
to determine whether at the time of an earthquake the
various parts of the arched openings which we see in many
buildings synchronised in their vibrations, or, for want of
synchronism, were caused to approach and recede from
each other. The arches experimented on were heavy
brick arches forming the two corridors of the Imperial
College of Engineering. The direction of one set of these
corridors is N. 40° E. and that of the other N. 50° W.

108 EARTHQUAKES.

The thickness of the walls in which these arches are
placed is 1 ft. 11 in. They are built of Japanese bricks
bound together with ordinary lime. The span of the
arches is 8 ft. 3 in., and the height of the arch from the
sprivging-line to the crown 4 ft. 1 in. The height of
the abutments is 7 ft. 14 in. The voussoirs of the arch
are formed of a light grey soft voleanic rock, and on their
faces show a depth of 12 inches. The width of the inter-
mediate columns between the arches is 4 ft. 6% in.

To determine whether at the time of an earthquake
there was any variation in the dimensions of these arches,
a light stiff deal rod, about 2 in. by 4 in. in cross section,
was placed across the springing-line of the arch. One end
of this was firmly fixed to the top of one abutment by
means of a spike; on the other end, which was to indicate
any horizontal movement if the abutments approached
each other, there was fixed a pointer made out of a piece
of steel wire. This rested on a piece of smoked glass fixed
to the ledge on which the loose end of the rod was
resting. If the abutments approached or receded from
each other a line would be drawn measuring the extent
of the motion. Asa further indication of motion, a second
smoked glass plate was fixed on the transverse rod, which
plate was marked on by a pointer attached to a vertical
rod hanging down from the crown of the arch.

As a general result of these experiments it may be
said that the portions of the building which were examined
usually either did not move at all, or else they practically
synchronised in their movements. When they did move,
the extent of motion was small, and the small differences
in movement which were observed were in every proba-
bility far within the elastic limits of the structure.

Observations on Cracks.—To determine whether the
walls of a building which have once been cracked, when

coe fae

“

Ave
ger

.
3

heey e

jd

EFFECTS PRODUCED UPON BUILDINGS. 109

subjected to a series of shocks, similar to those which they
experienced before being cracked, still continued to give
way, the extremities of a considerable number of cracks in
the N.E. end of the museum buildings of the Engineering
College were marked with pencil. Although since the
time of marking there had been many severe shocks, these
eracks did not visibly extend. These marks were made
on the outside wall of the building. On the inside, one of
these same cracks showed itself as a fissure about + inch
in width. Across this crack a horizontal steel wire
pointer was placed. One end of this wire was fixed in
the wall; the other end, which was pointed, rested on
the surface of a smoked glass plate placed on the other
side of the crack. After small earthquakes there was no
indication of motion having taken place, but after a shock
on February 21, as indicated by a line upon the smoked
glass plate, it was seen that the sides of the crack had
approached and receded from each other through a distance
of about +. inch.

By similar contrivances placed on cracks in a neigh-.
bouring building exactly similar results were obtained,
namely, that during small earthquakes the two sides of
the crack had retained their relative positions, but at the
time of a large shock this position had been changed.

In this building it was also observed that the cracks
in many instances increased their length.

By attaching levers to the end of the pointers to
multiply any motion that might take place, no doubt the
indications would be more frequent and more definite. It
would also be easier to rote the relative distances of motion
in two directions, namely, how far the cracks had closed
and how far they had opened. As to whether motion
would occur or not, much would no doubt depend upon
the direction of the earthquake.

110 EARTHQUAKES,

Prevention of Fractures.—One conclusion which may
perhaps be drawn from these observations is, that a
cracked building at the time of an earthquake shows a
certain amount of flexibility. Whether a building which
had been designed with cracks or joints between those
parts which were likely to have different periods of vibra-
tion would be more stable, so far as earthquake shakings
are concerned, than a similar building put up in an
ordinary manner, is a matter to be decided by experi-
ment. Certainly some of the cracks which have been
examined indicate that if they had not existed, the strain
upon the portion of the building where they occur would
have been extremely great.

Direction of Cracks.—In looking at. the oneal pro-
duced by small earthquakes it is interesting to note the
manner of their extension. The basements of the
buildings which have been most carefully examined are,
for a height of two or three feet, built of large rectan-
gular blocks of a greyish-coloured volcanic rock. In
these parts the cracks pass in and out between the joints
of the stone, indicating that the stones have evidently
been stronger than the mortar which bound them to-
gether, and as a consequence the latter had to give way.
Above this basement when the cracks enter the brickwork,
they no longer exclusively confine themselves to the
joints, but run in an irregular line through all they meet
with, sometimes across the bricks and sometimes through
the mortar joints. In places where they have traversed —
the brickwork, we can say that the mortar has been
stronger than the bricks. This traversing of the bricks
rather than the joints is, I think, the general rule for
the direction of the cracks in the brickwork of Tokio
buildings.

The Pitch of Roofs.—From observation of the effects

EFFECTS PRODUCED UPON BUILDINGS. Ill

produced by earthquakes, it appears to us that the houses
which lost the greater number of tiles appear to be those
with the steepest pitch, and those where the tiles were
‘simply laid upon the roof and not in any manner fastened
down. It would seem that destruction of this sort might
to a great extent be obviated by giving the roofs a less
inclination and fixing the tiles with nails. It was also
noticed that the greatest disturbance amongst the tiles
was upon the ridges of the roofs. Destruction of this sort
might be overcome by giving especial attention to these
portions during the construction of the roof.

Relative Position of Openings in Walls.—From what
has been said about the fractures in the buildings of Tokio
it will have been seen that, with but few exceptions, they
have all taken place above openings like doorways and
windows. If architecture demands that openings like
arches should be placed one above another in heavy walls
of this kind, as in fig. 17, there will be lines of weakness
running through the openings parallel to the dotted lines.
As arches are only intended to resist vertical thrusts,
special construction must be adopted to make them strong
enough to resist horizontal pulls. For instance, a flat
arch would offer more resistance to horizontal pulls than
an arch put together with ordinary voussoirs, there being
in the former case more friction to prevent the component
parts sliding over each other. Or again, above each arch
an iron girder or wooden lintel might be inserted in the
brick or stone arch. It was suggested to me by my col-
league, Mr. Perry, that the best form calculated to give a
wall uniform strength, would be to build it so that the
openings of each tier would occupy alternate positions,
that is to say, along lines parallel to the struts and ties of
a girder. In this way we should have our materials so
arranged that they would offer the same resistance to hori-

112 EARTHQUAKES.

zontal as to vertical movements. Such a wall is shown in
fig. 20 : the dotted lines running through the openings, and
all similar lines parallel to the former, representing lines
| of weakness. If we
compare this with fig.
21, we shall see that in
the case of a horizontal
movement ab or of a
vertical movement cd,
we should rather ex-
pect to find fractures
in a house built like
fig. 21 than ain- one
built like fig. 20. If,
however, these two buildings were shaken by a shock
which had an angle of emergence of about 45° in the
direction ef, the effects might be reversed. Usually,
however, and always in a town like Tokio which is visited
by shocks originating at a distance, the movements are
practically horizontal ones, and, therefore, buildings.
erected on the principles illustrated by fig. 20 should be
much superior, so far as resisting earthquakes is concerned,
to buildings constructed in the ordinary manner, as in
fig. 21. Fractures following a vertical line of weakness are
shown in the accompanying drawing, fig. 22, of the Church
of St. Augustin, at Manilla, shattered by the earthquakes
of 1880.

The last Howse in a Row.—When an earthquake shock
enters a line of buildings, and proceeds in a direction
coincident with that of the buildings, we should expect
that the last of these houses, being unsupported on one
side, would be in the position of the last person in Tyndall’s
row of boys. From this it would seem that the end house
in a row would show the greatest tendency to fly away
from its neighbours. If the last house stood upon the

FiG. 20. Hore 2k

EFFECTS PRODUCED UPON BUILDINGS, 113

edge of a deep canal or a cliff, there would be a layer of
ground, equal in thickness to the depth of the canal or to
the height of the cliff, as the case may be, which would
also be in a position to be thrown forward. The effect

5 = :
= Ape ee ra
Ceca 2 sae, ie —
Nee te ae =
cae i to eh An~ LU. ee ae ne
a “= aye == L—
~~ Ba Te
aa —

July 18-20, 1880.

which is sometimes produced upon an end building is
shown in fig. 23, which is taken from the photograph of a
house shattered in 1868 at San Francisco.

114 EARTHQUAKES.

The Swing of Buildings.—The distance through
which buildings are moved at the time of an earthquake
depends partly on their construction and partly on the
extent, nature, and duration of the movement com-
municated to them at their foundations. By violent
shocks buildings may be completely overthrown. In the
ease of small earthquakes, the upper portion of a house
may frequently move through a much greater distance
than the ground at its foundation. For instance, during

Fic. 23.—Webber House, San Francisco. Oct. 21, 1868.

the Yokohama earthquake of February, 1880, when the
maximum amplitude of the earth’s motion was probably
under 3 of an inch, from the slow swing of long Japanese
pictures, from three to six feet in length, which oscillated
backwards and forwards on the wall, it is very probable
that the extent through which the upper portion of
houses moved was very considerable. In some instances
these pictures seem to have swung as much as two feet,
and from the manner in which they swung they evi-
dently synchronised with the natural swing of the house.

EFFECTS PRODUCED UPON BUILDINGS. 115

From this it would seem that such a house must have
rocked from side to side one foot out of its normal
perpendicular position. That the motion was great is
testified by nearly all who tried to stand at the time of
the shock, it having been impossible to walk steadily
across the floor of a room in an upper story. The houses
here referred to are either those which are purely
Japanese, or else those which are framed of wood and
built on European models, a class of building which is
very common in Tokio and Yokohama.

Perry and Ayrton calculated the period of a complete
natural vibration of different structures. For a square
house whose outer and inner sections were respectively
30 and 26 feet, and whose height was 30 feet, the period
calculated would be about ‘06 second.

At the time of the above earthquake many houses
seem to have moved like inverted pendulums. On the
morning after the shock my neighbour, who was living
upstairs in a tall wooden house with a tile roof, told me
that he endeavoured to count the vibrations, and was of
the impression that to make a complete swing it took
about 2 seconds.

Assuming now that the distance through which the
top of a wooden house moved was about 1 foot, and the
number of vibrations which it made per second was
about °5, then the greatest velocity of a point on the top
of such a house must have been about 6 feet per second.

Mallet, who made observations upon the vibrations of
various structures, tells us that Salisbury spire moves to
and fro in a gale more than 3inches. A well-constructed
brick and mortar wall, 40 feet high and 1 foot 6 inches
thick, was observed to vibrate in a gale 2 feet trans-
versely before it fell.

An octagonal chimney with a heavy granite capping,

116 EARTHQUAKES.

160 feet high, was observed instrumentally to vibrate at
the top nearly 5 inches.’

At the time of a severe earthquake it does not seem
impossible but that a building may be swung completely
over. The accompanying illustration, fig. 24, taken from
a photograph,? apparently indicates a movement of this
description.

Fic. 24.—Stud Mill at Haywards, California. Oct. 21, 1868.

Principle of relative Vibrational Period.—If a lath
or thin pole loaded at one end with a weight fixed to
the ground, so as to stand vertically, be shaken by an
earthquake it will be caused to rock to and fro like
an inverted pendulum. _The period of its swing will be
chiefly dependent on its dimensions, its elasticity, and its
load. In a building we have to consider the vibration of
-a number of parts, the periods of which, if they were

1 Mallet, Dynamics of Earthquakes. | 2 Stud Mill at Haywards.

o> Sa de aR 4, (tet ee VE Pe
Voy So ae ss re :

EFFECTS PRODUCED UPON BUILDINGS. 117

independent of each other, would be different. On
account of this difference in period, whilst one portion of
a building is endeavouring to move towards the right,
another is pulling towards the left, and, in consequence,
either the bonds which join them or else they themselves
are strained or broken. This was strikingly illustrated
by many of the chimneys in the houses at Yokohama,
which by the earthquake of February 20, 1880, were
shorn off just above the roof. The chimneys were shafts of
brick, and probably had a slower period of vibration than
the roof through which they passed, this latter vibrating
with the main portion of the house, which was framed of
wood. :

A particularly instructive example of this kind which
came under my notice is roughly sketched in fig. 25.

This is a chimney standing alone, which, for the sake
of support, was strapped by an iron band to an adjoining
building. It would seem that at
the time of the shock, the building
moving one way and the chimney
another, the swing of the heavy
building gave the chimney a sharp
jerk and cut it off. The upper
portion, being then loose upon the
lower part, rotated under the in-
fluence of the oscillations in manner
similar to that in which grave-
stones are rotated.

Mallet made observations similar to these in Italy.
He tells us that a buttress may often not have time to
transmit its stability to a wall. The wall and the
buttress have different periods of vibration, and therefore
they exert impulsive actions on each other. Effects like
these were strikingly observable in many of the rural

Fig. 25.

118 EARTHQUAKES.

Italian churches where the belfry tower is built into one
of the quoins of the main rectangular building.

Not only have we to consider the relative vibrations —

of the various parts of a building amongst themselves,
but we have to consider the relation of the natural
vibrations of any one of them or the vibration of the
building as a whole, with regard to the earth, the
vibrations of which it must be remembered are not
strictly periodic.

Some of the more important results dependent upon
the principle of ‘relative vibrational periods’ may be
understood from the following experiments :—

In fig. 26 a, B, and C are three flat springs made out of
strips of bamboo, and loaded at the top with pieces of
lead. At the bottom they are
fixed into a piece of board DE,
and the whole rests on a table
FG. The legs of this table
being slightly loose, by placing

D E the fingers on the top of it,
ae Fic. 26. G — aquick short backward and for-
ward movement can be pro-
duced. The weights on a and Bare the same, but they are
larger than the weight on c. Consequently the periods of
A and B are the same, but different to the period of c.
The dimensions of these springs are as follows: height,
18 inches; a and B each carry weights equal to 320
grammes, and they make one vibration per second ; C has
a weight of 199 grammes, and makes 0°75 vibrations per
second.

Furst Experiment.—It will be found that by giving the
table a gentle backward and forward movement, the extent
of which movement may be so small that it will be diffi-
cult to detect it with the eye, either a and B may be

A B Cc

EFFECTS PRODUCED UPON BUILDINGS. 119

made to oscillate violently whilst c remains still; or vice
versa, C may be caused to oscillate whilst a and B remain
still. In the one case the period of shaking will have
been synchronous with the natural period of A and B,
whilst in the latter it will have been synchronous with
that of c. This would seem to show us that if the
natural period of vibration of a house, or of parts of it, at
any time agree with the period of the shock, it may be
readily thrown into a state of oscillation which will be
dangerous for its safety.

Second Experiment.—Bind a and B together with a
strip of paper pasted between them. (The paper used
was three-eighths of an inch broad and would carry
a weight of nearly three pounds.) If the table be now
shaken as before, A and B will always have similar move-
ments, and tend to remain at the same distance apart,
and as a consequence the strip of paper will not be broken.
From this experiment it would seem that so long as the
different portions of a building have almost the same
periods of vibration, there will be little or no strain upon
the tie-rods or whatever contrivance may be used in
connecting the different parts.

Third Experiment.—Join a and ©, or B and Cc with a
strip of paper in a manner similar to the last experiment.
If the table be now shaken with a period approximating
either to that of a and 8, or with that of c, the paper will
be suddenly snapped.

This indicates that if we have different portions of a
building of such heights and thicknesses that their natural
periods of vibration are different, the strain upon the
portions which connect such parts is. enormous, and it
would seem, as a. consequence, that either the vibrators
themselves, or else their connections, must, of a necessity,
give way. ‘This was very forcibly illustrated in the Yoko-

120 EARTHQUAKES,

hama earthquake of February 1880 by the knocking over
of chimneys. The particular case of the chimneys is,
however, better illustrated by the next. experiment.

Fourth Expervment.—Take a little block of wood
three-quarters of an iuch square and about one inch high,
and place it on the top of a, B, or c. It will be found
that, although the spring on which it stands is caused to
swing backwards and forwards through a distance of three
inches, the little block will retain its position.

This little block we may regard as the upper part of a
chimney standing on a vibrating stack, and we see that,
so long as this upper portion is light, it has no tendency
to fall. ,

Fifth Expervment.—Repeat the fourth experiment,

having first placed a small leaden cap on the top of the _

block representing the chimney. (The cap used only
weighed a few grammes.) When vibration commences
it will be found that the block quickly falls. This would
seem to indicate that chimneys with heavy tops are more
likely to fall than light ones.

Siath Eauperiment.— Bind a and B together with a
strip of paper and stand the little block upon the top of
either. It will be found that the block will stand as in
the fourth experiment.

Seventh Experiment.—Bind a and C, or B and C
together, and place the block upon the top of either of
them. When vibration commences, although the paper

- may not be broken, the little block will quickly fall.

Eighth Experiment.—Take two pencils or pieces of
glass tube and place them under the board DE. If the
table FG be now shaken in the direction DE, it will be
found that the springs will not vibrate.

In a similar manner if a house or portion of a house
were carried on balls or rollers, as has already been sug-

Pie. Ln a eS St he "ore 4 Ke ae ae

ey een Pa en

EFFECTS PRODUCED UPON BUILDINGS. 121

gested, it would seem that the house might be saved from
much vibration.

Ninth Experiment.—Set any of the springs in violent
vibration by gently shaking DE instead of the table, and
then suddenly cease the actuating motion. It will be
observed that at the moment of cessation the board and
the springs will have a sudden and very decided motion
of translation in the same direction as that in which the
springs were last moving, and although the springs were
at the time swinging through a considerable arc, all
motion will suddenly cease. |

This shows, that ifa house is in a state of vibration
the strain at the foundations must be very great.

It would not be difficult to devise other experiments
to illustrate other phenomena connected with the principle
of relative vibrational periods, but these may perhaps be
sufficient to show to those who have not considered this
matter its great importance in the construction of build-
ings. Perhaps the greater portion of what is here said
may by many be regarded as self-evident truisms hardly
worth the trouble of demonstration. Their importance,
however, seems to be so great that I hope that their
discussion has not been altogether out of place.

I may remark that in the rebuilding of chimneys
in Yokohama the principles here enunciated were taken
advantage of by allowing the chimneys to pass freely
through the roofs without coming in contact with any of
the main timbers.

In putting up buildings to resist the effects of an
earthquake, besides the idea of making everything strong
because the earthquake is strong, there are several

principles which, like the one just enunciated, might

advantageously be followed which as yet appear to have

- received but little attention.

122 EARTHQUAKES,

CHAPTER VII.

EFFECTS PRODUCED UPON BUILDINGS (continwed).

Types of buildings used in earthquake countries—In Japan, in Italy,
in South America, in Caraccas—Typical houses for earthquake
countries—Destruction due to the nature of underlying rocks—
The swing of mountains—Want of support on the face of hills—
Earthquake shadows—-Destruction due to the interference of waves
—FEarthquake bridges—Examples of earthquake effects—Protection
of buildings—General conclusions.

Types of buildings used in earthquake countries.—
In Japan there are excellent opportunities of studying
various types of buildings. The Japanese types, of course,
form the majority of the buildings. The ordinary Japanese
house consists of a light framework of 4 or 5 inch scan-
tling, built together without struts or ties, all the timbers
crossing each other at right angles. The spaces are filled
in with wattle-work of bamboo, and this is plastered over
with mud. This construction stands on the top of a row
of boulders or of square stones, driven into the surface soil
to a distance varying from a few inches to a foot. The
whole arrangement is so light that it is not an uncommon
thing to see a large house rolled along from one posi-
tion to another on wooden rollers. Jn buildings such as
these after a series of small earthquake shocks, we could
hardly expect to find more fractures than in a wicker
basket.

The larger buildings, such as temples and pagodas, are

v= a” a
+r 7
=

EFFECTS PRODUCED UPON BUILDINGS. 123

also built of timber. These are built up of such a multi-
tude of pieces and framed together in such an intricate
manner that they also are capable of yielding in all

directions. The European buildings are, of course, made

of brick and stone with mortar joints. Some of these, as
the buildings of the Ginza in Tokio, are not designed for
great strength. On the other hand, others have thick
and massive walls and are equal in strength to those we
find in Europe.

The third type of buildings are those which are built
in blocks; and these blocks being bound together with
iron rods traversing the walls in various directions are
especially designed to withstand earthquakes. <A system
somewhat similar to this has been patented in America,
and examples of these so-called earthquake-proof buildings
are to be found in San Francisco.

Speaking of Japanese buildings, Mr. R. H. Brunton,
who has devoted especial attention to them says that,! ‘to
imagine that slight buildings, such as are seen here (i.e.
in Japan), are the best calculated to withstand an earth-
quake shock is an error of the most palpable kind.’ After
describing the construction of a Japanese house in pretty
much the same terms as we have used, he says ‘ that with
its unnecessarily heavy roof and weak framework it is a
structure of all others the worst adapted to withstand a
heavy shock.’ He tells us, further, that these views are
sustained by the truest principles of mechanics. In order
to render buildings to some extent proof against earth-
quakes, some of the heavy roofs in Tokio have been so
constructed that they are capable of sliding on the walls.
Mr. Brunton mentions a design for a house, the upper

1 See ‘ Constructive Art in Japan,’ by R. H. Brunton, C.E., F.R.G.S.,
F.G.8S., Transactions of Asiatic Socicty of Japan, December 22, 1873,
and January 13, 1875.

124 , EARTHQUAKES.

part of which is to rest on balls, which roll on inverted
cups fixed on the lower part of the building, which isto be
firmly embedded in the earth. A similar design was,
at the suggestion of Mallet, used to support the tables
carrying the apparatus of some of the lighthouses erected
in Japan by Mr. Brunton. The very existence of these
designs seems to indicate that the ordinary European
house, however solidly and strongly it may be built, is
not sufficient to meet the conditions imposed upon it.
What is required, is something that will give way—an
approximation to the timber frame of a Japanese house,
so strongly condemned by Mr. Brunton and others. The -
crucial test of the value of the Japanese structure, as com-
pared with the modern buildings of brick and stone, is
undoubtedly to be found by an appeal to the buildings
themselves. So far as my own experience has gone, I must
say that I have never seen any signs in the Japanese
timber buildings which could be attributed to the effects
of earthquakes, and His Excellency Yamao Yozo, Vice
Minister of Public Works, who has made the study of the
buildings of Japan a speciality, told me that none of the
temples and palaces, although many of them are several
centuries old, and although they have been shaken by
small earthquakes and also by many severe ones, show
any signs of having suffered. The greatest damage wrought
by large earthquakes appears to have resulted from the
influx of large waves or from fires. In every case where
an earthquake has been accompanied by great de-
struction, by consulting the books describing the same,
it can be seen, from the illustrations in these books
portraying conflagrations, that this destruction was chiefly
due to fire. When we remember that nearly all Japanese
houses are constructed of materials that are readily
inflammable, it is not hard to imagine how destruction of

EFFECTS PRODUCED UPON BUILDINGS. 125

this kind has come about. To a Japanese, living as he
does in a house which has been compared to a tinder-box,
fire is one of his greatest enemies, and in a city like Tokio
it is not at all uncommon to see during the winter months
many fires which sweep away from 100 to 500 houses.
In one winter I was a spectator of three fires, each of
which was said to have destroyed upwards of 10,000
houses.

_ Although it would appear that the smaller earthquakes
of Japan produce no visible effect upon the native
buildings, it is nevertheless probable that small effects
may have been produced, the observation of which is
rendered difficult by the nature of the structure. If we
look at buildings of foreign construction, by which are
meant buildings of brick and stone, the picture before us
is quite different, and everywhere the effects of earthquakes
are palpable even to the most casual observer. Of these
effects numerous examples have already been given. Not
only are these buildings damaged by the cracking of walls
and the overturning of chimneys, but they also appear to
be affected internally. For instance, in the timbers of
the roof of the museum attached to the Imperial College
of Engineering in Tokio, there are a number of diagonal
pieces acting as struts or ties intended to prevent more
or less horizontal movements taking place. Those which
are rigidly joined together with bolts and angle irons
have apparently suffered from their rigidity, being twisted
and bent into various forms. The buildings in Tokio, |
which are strongly put together, being especially designed
to withstand earthquakes, appear to have suffered but
little. I know only one example which at the time of
the severe shock of 1880 had several of its chimneys
damaged. | :

The ordinary houses in Italy, though built of stone and

126 EARTHQUAKES.

mortar, are but poorly put together, and, as Mallet has
remarked, are in no way adapted to withstand the frightful
shakings to which they are subjected from time to time.

In the large towns, like Naples, Rome, and Florence,
where happily earthquakes are of rare occurrence, although
the building may be better than that found in the country,
the height of the houses and the narrowness of the streets
are sufficient to create a shudder, when we think of the
possibility of the ogcurrence of a moderately severe earth-
quake.

In South America, although many buildings are built
with brick and stone, the ordinary houses, and even the
larger edifices, are specially built to withstand earth-
quakes. In Mr. James Douglas’s account of a ‘ Journey
Along the West Coast of South America,’ we read the
following!: ‘ The characteristic building material of Guaya-
quil is bamboo, which grows to many inches in thickness,
and which, when cut partially through longitudinally at
distances of an inch or so, and once quite through, can
be opened out into fine elastic boards of serviceable width.
Houses, and even churches, of a certain primitive beauty
are built of such reeds, so bound together with cords that
few nails enter into the construction, and which, therefore,
yield so readily to the contortions of the earth during an
earthquake as to be comparatively safe.’ 3

Here we have a house, which, so far as earthquakes are
concerned, is an exaggerated example of the principles
which are followed in the construction of an ordinary
Japanese dwelling.

Another plan adopted in South America can be
gathered from the same author’s writings upon Lima,
about which he says, ‘To build high houses would be to
erect structures for the first earthquake to make sport of,

! Journal of the American Geographical Society, vol. x.

EFFECTS PRODUCED UPON BUILDINGS. We

and, therefore, in order to obtain space, safety, and comfort,
the houses of the wealthy surround court after court, filled
with flowers, and cooled with fountains, connected one
with another with wide passages which give a vista from
garden to garden.’

History would indicate that ids of this type have
been arrived at as the results of experience, for it is said
_ that when the inhabitants of South America first saw the
Spaniards building tall houses, they told them they were
building their own sepulchres.!

In Jamaica, we find that even as early as 1692 ex-
perience had taught the Spaniards to construct low houses,
which withstood shakings better than the tall ones.”

In Caraccas, which has been called the city of earth-
quakes, it is said that the earthquakes cause an average
yearly damage amounting to the equivalent of a per capita
tax of four dollars. To reduce this impost to a minimum

much attention is paid to construction. ‘ Projecting

basement corners (giving the house a slightly pyramidal
appearance) have been found better than absolutely per-
pendicular walls; mortised corner-stones and roof beams
have saved many lives when the central walls have split
from top to bottom; vaults and key-stone arches, no
matter how massive, are more perilous than common
wooden lintels, and there are not many isolated buildings
in the city. In many streets broad iron girders, riveted
to the wall, about a foot above the house door, run from
house to house along the front of an entire square. Turret-
like brick chimneys, with iron top ornaments, would ex-
pose the architect to the vengeance of an excited mob;
the roofs are flat, or flat terraced; the chimney flues
terminate near the eaves in a perforated lid.’§ |
1 Phil. Trans., li. 1760. 2 Thid., xviii.

*¢The City of Earthquakes, H. D. Warner, Atlantic Monthly,
March 1883.

128 EARTHQUAKES,

Typical houses for earthquake countries.— From what
has now been said about the different buildings found in
earthquake countries, it will be seen that if we wish to put
up a building able to withstand a severe shaking, we have
before us structures of two types. One of these types may
be compared with a steel box, which, even were it rolled
down a high mountain, would suffer but little damage;
and the other, with a wicker basket, which would equally
withstand so severe a test. Both of these types may be,
to some extent, protected by placing them upon a loose
foundation, so that but little momentum enters them at
their base. One suggestion is to place a building upon
iron balls. Another method would be to place them upon
two sets of rollers, one set resting upon the other set at
right angles. The Japanese, we have seen, place their
houses on round stones. The solid type of building is
expensive, and can only be approached partially, whilst
the latter is cheap, and can be approached closely. In
the case of a solid building it would be a more difficult
matter to support it upon a movable foundation than in
the case of a light framework. Such a building is
usually firmly fixed on the ground, and consequently at
the time of an earthquake, as has already been shown by
experiment, must be subjected to stresses which are very
great. In consequence also of the greater weight of the
solid structure, more momentum will enter it at its base
than in the case of the light structure. Also, we must
remember that the rigidity favours the transmission of
momentum, and with rigid walls we are likely to have
ornaments, coping-stones, and the comparatively freer
portions forming the upper part of a building displaced ;
whilst, with flexible walls absorbing momentum in
the friction of their various parts, such disturbances
would not be so likely. Mr. T. Ronaldson, referring to

EFFECTS PRODUCED UPON BUILDIINGS 129

this, says, that in 1868, at San Francisco, the ornamental
stone-work in stone and cement buildings was thrown

from its position, whilst similar ornaments in neighbour-

ing brick buildings stood.

To reduce the top weight of a building, hollow bricks
might be employed. To render a building more homo-
geneous and elastic, the thickness of bricks might be
reduced. Inasmuch as the elasticity of brick and timber
are so different, the two ought to be employed separately.
For internal decorations plaster mouldings might be re-
placed by papier maché and carton-pierre, the elastic
yielding of which is comparatively great.! Houses,

q _ whether of brick and stone, or of timber, ought to be

broad and low, and the streets three or four times as wide
as the houses. The flatter the roofs the better.

One of the safest houses for an earthquake country
would probably be a one-storied strongly framed timber
house, with a light flattish roof made of shingles or sheet-
iron,the whole resting on a quantity of small cast-iron balls
earried on flat plates bedded in the foundations. The
chimneys might be made of sheet-iron carried through
holes free of the roof. The ornamentation ought to be
of light materials.

At the time of severe earthquakes many persons seek
refuge from their houses by leaving them. In this case
accidents frequently happen from the falling of bricks
and tiles. Others rush to the doorways and stand beneath
_thelintels. Persons with whom the author has conversed
have suggested that strongly constructed tables and bed-
steads in their rooms would give protection. To see
persons darting beneath tables and bedsteads would un-
doubtedly give rise to humiliating and ludicrous exhibi-
tions. This latter idea is not without a value, and most

' T. Ronaldson, A Treatise on Earthquake Dangers Sc.

130 EARTHQUAKES.

certainly, if applied in houses of the type described, would
be valuable.

The great danger of fire may partially be obviated by
the use of ‘earthquake lamps,’ which are so constructed
that before they overturn they are extinguished. It is
said that in South America some of the inhabitants are
ready at any moment to seek refuge in the streets, and
they have coats prepared, stocked with provisions and
other necessaries, which, if occasion demands, will enable
them to spend the night in the open air. These coats,
called ‘earthquake coats,’ might also, with properly con-
structed houses, be rendered unnecessary.

Destruction due to the nature of the inaarfee
rocks.—That the nature of the ground on which a
building stands is intimately related with the severity of
the blow it receives is a fact which has often been de-
monstrated.

One cause of destruction is due to placing a building
on foundations which are capable of receiving the full
effects of a shock, and transmitting it to the buildings
standing on them.

For instance, the reason why a soft bed mnieht possibly
make a good foundation, is, as has been pointed out by
Messrs. Perry and Ayrton, because the time of trans-
mission of momentum is increased ; in fact, the soft bed
is very like a piece of wood interposed between a nail and
the blows of a hammer—it lengthens the duration of
impact. For this reason we are told that a quaking bog
will make a good foundation. When a shock enters loose
materials its waves will be more crowded, and it is possible
that a line of buildings may rest on more than one wave
during a shock. There are many examples on record of
the stability of buildings which rested on beds of particu-
lar material at the time of destructive earthquakes. As

EFFECTS PRODUCED UPON BUILDINGS. 131

the observations which have been made by various writers
on this subject appear to point in a contrary direction, I
give the following examples :—

In the great Jamaica earthquake of 1692, the portions
of Port Royal which remained standing were situated on
a compact limestone foundation; whilst those on sand
and gravel were destroyed (‘ Geological Observer,’ p. 426).
Again, on p. 148 of the same work, we read, ‘ According _
_ to the observations made at Lisbon, in 1737, by Mr. Sharpe,
the destroying effects of this earthquake were confined to
the tertiary strata, and were most violent on the blue
clay, on which the lower part of the city is constructed.
Not a building on the secondary limestone or on the basalt
was injured.’

In the great earthquakes of Messina, those portions of
the town situated on alluvium, near the sea, were destroyed,
whilst the high parts of the town, on granite, did not suffer
somuch. Similar observations were made in Calabria, when
districts consisting of gravel, sand, and clay became, by the
shaking, almost unrecognisable, whilst the surrounding
hills of slate and granite were but little altered. At San
Francisco, in 1868, the chief destruction was in the allu-
vium and made ground.

At Talacahuano, in 1835, the only houses which
escaped were the buildings standing on rocky ground:
all those resting on sandy soil were destroyed.

From the results of observations like these, it would
seem the harder rocks form better foundations than the
softer ones. The explanation of this, in many cases, |
appears to lie in the fact that the soft strata were in a
state of unstable equilibrium, and by shaking, they were
caused to settle. Observations like the following, however,
point out another reason why soft strata may sometimes
afford a bad foundation.

132 - EARTHQUAKES.

‘Humboldt observed that the Cordilleras, composed of
gneiss and mica-slate, and the country immediately at
their foot, were more shaken than the plains.”

‘Some writers have asserted that the wave-like move-
ments (of the Calabrian earthquake in 1783) which were
propagated through recent strata from west to east, became
very violent when they reached the point of junction with
the granite, as if a reaction was produced when the undula-
tory movement of the soft strata was suddenly arrested by
the more solid rocks.’

Dolomieu when speaking of this earthquake says, the
usual effect ‘was to disconnect from the sides of the
Apennines all those masses (of sand and clay) which
either had not sufficient bases for their bulk, or which
were supported only by lateral adherence.’

These intensified actions taking place at and near to
lines of junction between dissimilar strata is probably due
to the phenomena of reflection and refraction.

When referring to the question as to whether build-
ings situated on loose materials suffered more or less than
those on solid rocks, Mallet, in his description of the
Neapolitan earthquake of 1857, remarks: ‘ We have in
this earthquake, towns such as Saponara and Viggiano,
situated upon solid limestone, totally prostrated ; and we
have others such as Montemarro, to a great extent based
upon loose clays, totally levelled. We have examples of
almost complete immunity in places on plains of deep
clay as that of Viscolione, and in places on solid lime-
stone, like Castelluccio, or perched on mountain tops like
Petina.’?

After reading the above, we see that the probable reason
why, in several cases, beds of soft materials have not made

1 Principles of Geology, Lyell, vol. ii. p. 106.
2 The Neapolitan Earthquake of 1857, R. Mallet, vol. ii. p. 359.

et a ae

=.

EFFECTS PRODUCED UPON BUILDINGS. | 133

good foundations, consists in the fact that they have either
been of small extent or else have been observed only in
the neighbourhood of lines which divided them from other
formations, which lines are always those of great disturb-
ances. :

At the end of his description of the Neapolitan earth-
quake of 1857, Mallet says that more buiidings were

destroyed on the rock than on the looseclay. This, how-

ever, he remarks, is hardly a fact from which we can draw
any valuable deductions, because it so happened that more
buildings were constructed on the hills than on the loose
ground.}

Professor D. S. Martin, writing on the earthquake of
New England in 1874, remarks that in Long Island the
shock was felt where there was gneiss between the drift.
Around portions to the east the observations were few and
far between. He also remarks that generally the shocks
were felt more strongly and frequently on rocky than on
soft ground.! |

From these examples, it would appear that the hard
ground, which usually means the hills, forms a better
foundation than the softer ground, which is usually to be
found in the valleys and plains. Other examples, how-
ever, point to a different conclusion. For instance,a civil
engineer, writing about the New Zealand earthquake of
1855, when all the brick buildings in Wellington were over-
thrown, says that ‘it was most violent on the sides of the
hills at those places, and least so in the centre of the
alluvial plains.’ ?

In this example it must be noticed that the soft
alluvium here referred to was of large extent, and not loose
material resting on the flanks of rocks, from which it was

|
DAME. 06t.1X- 191.
2 Reports of British Association, 1858, p. 106.

134 EARTHQUAKES,

likely to be shaken down, as in most of the previous ex-
amples. |

The results of my own observations on this subject
point as much in one direction as inthe other. In Tokio,
from instrumental observations upon the slopes and tops
of hills, the disturbance appears to be very much less
than it isin the plains. Thus, at my house, situated on
the slope of a hill about 100 feet in height, for the earth-
quake of March 11, 1882, I obtained a maximum ampli-
tude of motion of from three to four millimétres only, whilst
Professor Ewing, with a similar instrument, situated on the
level ground at about a mile distant, found a motion of fully
seven millimétres. This calculation has been confirmed
by observations on other earthquakes. Thus, for instance,
in the destructive earthquake of 1855, when a large por-
tion of Tokio was devastated, it was a fact, remarked by
many, that the disturbance was most severe on the low
ground and in the valleys, whilst on the hills the shock
had been comparatively weak. As another illustration, I
may mention that within three-quarters of a mile from
my house in Tokio there is a prince’s residence which
has so great a reputation for the severity of the shakings
it receives that its marketable value has been consider-
ably depreciated, and it is now untenanted.

In Hakodadi, which is a town situated very similarly
to Gibraltar, partly built on the slope of a high rocky
mountain and partly on a level plain, from which the
mountain rises, the rule is similar to that for Tokio,
namely, that the low, flat ground is shaken more severely
than the high ground. At Yokohama, sixteen miles south-
west from Tokio, the rule is reversed, as was very clearly
demonstrated by the earthquake of February 1880, when
almost every house upon the high ground lost its chimney,
whilst on the low ground there was scarcely any damage

EFFECTS PRODUCED UPON BUILDINGS. 135

done; the only places on the low ground which suffered
were those near to the base of the hills. The evidence as
to the relative value of hard ground as compared with
soft ground, for the foundation of a building, is very con-
flicting. Sometimes the hard ground has proved the
better foundation and sometimes the softer, and the
superiority of one over the other depends, no doubt, bps
a variety of local circumstances.

These latter observations open up the inquiry as
to the extent to which the intensity of an earthquake
may be modified by the topography of the disturbed
area.

Lhe swing of mowntarns.—If an earthquake wave
is passing through ground the surface of which is level,
so long as this ground is homogeneous, as the wave travels
- further and further we should expect. its energy to become
less and less, until, finally, it would insensibly die out.
If, however, we have standing upon this plain a mountain,
judging from Mallet’s remarks, this mountain would be
set in a state of vibration much in the same way as a
house is set in vibration, and it would tend to oscillate
backward and forward with a period of vibration dependent
upon the nature of its materials, size,andform. The upper
portion of this mountain would, in consequence, swing
through a greater are than the lower portion, and build-
ings situated on the top of it would swing to and fro
through a greater arc than those which were situated
near its foot. This explanation why buildings situated
on the top of a mountain should suffer more than those
situated on a plain, is one which was offered by Mallet
when writing of the Neapolitan earthquake. He tells us
that towns on hills are ‘rocked as on the top of masts,’
and if we accept this explanation it would, in fact,
be one reason why the houses situated on the Bluff at

136 EARTHQUAKES.

Yokohama suffered more than those situated in the settle-
ment. This explanation is given on account of the great
authority it claims as a consequence of its source. It is
not clear how the statement can be supported, as different
portions of the mountain receive momentum in opposite
directions at the same time.

Want of support on the faces of hills—When a
wave of elastic compression is propagated through a
medium, we see that the energy of motion is being con-
tinually transmitted from particle to particle of that
medium. A particle, in moving forwards, meets with an
elastic resistance of the particles towards which it moves,
but, overcoming these resistances, it causes these latter
particles to move, and in turn to transmit the energy to
others further on. So long as the medium in which this
transfer of energy is continuous, each particle has a limit
to its extent of motion, dependent on the nature of the
medium. When, however, the medium, which we will
suppose to be the earth, is not continuous, but suddenly
terminates with a cliff or scarp, the particles adjacent to
this cliff or scarp, having no resistance offered to their
forward motion, are shot forward, and, consequently, the
ground here is subjected to more extensive vibrations
than at those places where it was continuous. This may
be illustrated by a row of marbles lying in a horizontal
groove; a single marble rolled against one end of this
row will give a concussion which will run through the
chain, like the bumping of an engine against a row of
railway cars, and as a result, the marble at the opposite
end of the row, being without support, will fly off.
Tyndall illustrates the same thing with his well known
row of boys, each one standing with his arms stretched
out and his hands resting upon the shoulders of the boy
before him. A push being given to the boy at the back,

EFFECTS PRODUCED UPON BUILDINGS. 137

the effect 1s to transmit a push to the first boy, who,
being unsupported, flies forward.

In the case of some earthquakes, most disastrous
results have occurred which seem only to admit of an
explanation such as this. A remarkable instance of this
kind occurred when the great earthquake of 1857 ‘swept
along the Alps from Geneva to the east-north-east, and
its crest reached the edge of the deep glen between
Zermatt and Visp. Then the upper part of the wave-
movement, a thcusand or two thousand feet in depth
from the surface, came to an end; the forward pulsation
acted like the breaker of the sea, and heavy falls of rock
encumbered the western side of the valley.’

Earthquake shadows.—lIf a mcuntain stands upon a
plain through which an elastic wave is passing, which is
almost horizontal, the mountain is, so to speak, in the
shadow of such a wave. If we only consider the normal
motion of this wave, we see that the only motion which
the mountain can obtain will be a wave of elastic distor-
tion produced by a shearing force along the plain of the
base. Should, however, the wave approach the mountain
from below, and emerge into it at a certain angle, only
the portion of the mountain on the side from which the
wave advanced could remain in shadow, whilst the portion
on the opposite side would be thrown into a state of com-
pression and extension. Portions in shadow, however,
would be subject to waves of elastic distortion. In a
manner similar to this we may imagine that certain
portions of the bluff, so far as the advancing wave was
concerned, were in shadow, and thus saved from the
immediate influence of the direct shock. <A hypothetical
case of such a shadow is shown in the accompanying
section, illustrating the contour of the ground at Yoko-
hama. The situation which might be in the shadow of

138 EARTHQUAKES.

one shock, however, it is quite possible might not be in ~
that of another. We must also remember that a place in
shadow for a direct
shock might be af-
fected by reflected
waves, and also by
the transverse vibra-
_ tions of the direct
shock. These effects
are over and above
the effects produced
by the waves of
elastic distortion just
referred to. It might
~ be asked whether
whole countries, like
England, which are
but seldom shaken,
are in shadow.
Destruction due
to the interference of
waves.—Referring to
the section of the
ground at Yokohama
(Fig. 27), it will be
seen that both the
settlement and the
bluff stand upon beds
of gravel capping
horizontal beds of
grey tuff. The gravel
of that portion of the
settlement on the
seaboard _ originally

Settlement

Bluff

Fic, 27.—Hypothetical section at Yokohama,

gerere acnne-—-~ = ~~ ~~~ = --- == -- --

EFFECTS PRODUCED UPON BUILDINGS. 139

formed the line of a shingle beach. That portion of the
settlement back from the sea stands upon ground which
was originally marshy. In the central portions of the
settlement this bed of gravel is very thick, perhaps 100
feet or so, but as you near the edge of the bluff it pro-
bably becomes thinner, until it finally dies out upon the
flanks of the scarps.

On the top of the bluff, the beds of gravel will, in every
probability, be generally thinner than they are upon the
lower level. The beds of tuff, which is a soft grey-
coloured clay-like rock, produced by the solidification of
voleanic mud, appear, when walking on the seaboard, to
be horizontally stratified. If there is a dip inland, it is
in all probability very slight. Here and there the beds
are slightly faulted. Taken as a whole we may consider
these beds as being tolerably homogeneous, and an earth-
quake in passing through them would meet with but
little reflection or refraction. At the junction of these
beds with the overlying gravels, both reflection and refrac-

% _ tion would comparatively be very great.

On entering the gravel, as the wave would be passing
into a less elastic medium, the direction of the wave
would be bent towards the perpendicular to the line of
junction, and the angle of emergence at the surface would
consequently be augmented. At the surface certain
reflection would also take place, but the chief reflections
would be those at the junction of the tuff and the allu-
vium.

Under the settlement it is probable that all the reflec-
tions which took place would be single. Thus wave
fronts like a, advancing in a direction parallel to the line
a, would be reflected in a direction a, and give rise toa
series of reflected waves A, These are shown by thicker
lines. Similarly all the neighbouring waves to the right

140 EARTHQUAKES.

and left of a, would give rise to a series of reflected waves.
If the lines drawn representing wave fronts are districts
of compression, then, where two of the lines cross each
other, there would be double energy in producing com-
pression. Similarly, districts of rarefaction might accord,
and, again, compression of one wave might meet with the
rarefaction of another and a neutralisation of effect take
place. A diagram illustrating concurrence and interfer-
ence of this description is given in Le Conte’s ‘ Elements
of Geology,’ p. 115. The interference which has been
spoken of, however, is not the greatest which would occur.
The greatest would probably be beneath the bluff and the
scarps which run down to join the level ground below.
This would be the case because it is a probability that
there might not only be cases of interference of single
reflected waves, but also of waves which had been not only
twice but perhaps thrice reflected. For example, a wave
like B, (which is parallel to A, of the first supposition),
advancing in a direction parallel to 6,, might be reflected
along the line 6, giving rise to waves like B,, which in
turn might be reflected along 6, giving rise to waves like
B,. The number of districts where there would be con-
currence and interference would, in consequence of the
number of times waves might be reflected, be augmented.
Here the violence of the shock would, at certain points, be
considerably increased, but as a general result energy
must be lost, so that even if some of the reflected waves
found their way into the portion we have regarded as
being in shadow, their intensity would not be so great as
if they had entered it directly.

The shaking down of loose materials from the sides of
hills may be partially explained on the assumption of an
increased disturbance due to interference.

Earthquake bridges.—In certain parts of South

EFFECTS PRODUCED UPON BUILDINGS. . 141

America there appear to exist tracts of ground which are
practically exempt from earthquake shocks, whilst the
whole country around is sometimes violently shaken. It
would seem as if the shock passes beneath such a district
as water passes beneath a bridge, and for this reason
_ these districts have been christened ‘ bridges.’

This phenomenon appears to depend upon the nature
of the underlying soil. When an elastic wave passes
from one bed of rock to another of a different character, a
certain portion of the wave is reflected, while the
remainder of it is transmitted and refracted, and
‘bridges’ we may conceive of as occurring where the
phenomenon of total reflection occurs.

In the instances given of soft materials having proved
good foundations, it was assumed that they had chiefly
acted as absorbers of momentum. They have also acted
as reflecting surfaces, and where no effects have been felt
by those residing on them, this may have been the result
of total reflection, and the soft beds thus have played the
part of bridges.

Fuchs gives an example taken from the records of
the Syrian earthquake of 1837, where not only neigh-
bouring villages suffered differently, but even neighbour-
ing houses. In one case a house was entirely destroyed,
whilst in the next house nothing was felt.

In Japan, at a place called Choshi, about 55 miles
east of the capital, earthquakes are but seldom felt,
although the surrounding districts may be severely
shaken.

From descriptions of this place it would appear that
there is a large basaltic boss rising in the midst of
alluvial strata. The immunity from earthquakes in
this district has probably given rise to the myth of the
Kanam rock, which is a stone supposed to rest upon the

1A2e EARTHQUAKES.

head of a monstrous catfish (Namadzu), which by its writh-
ings causes the shakings so often felt in this part of the
world.!

Prof. D. S. Martin, writing on the earthquake of New
England in 1874, says that it was felt at four points; it
was felt in the heart of Brooklyn all within a circle of
half a mile across; ‘and this fact would suggest that a
ridge of rock perhaps approaches the surface at that
point, though none is known to appear.’ ?

The subject of special districts, which are more or less
protected from severe shakings, will be again referred to,
and it will be seen that after a seismic survey has been
made even of a country like Japan, where there are on
the average at least two earthquakes per day, itis possible
to choose a place to build in as free from otha as
Great Britain.

General exampies of earthquake oe —The fol-
lowing examples of earthquake effects are drawn from
Mailet’s account of the Neapolitan earthquake of 1857.

At a town called Polla there was great destruction.
Judging from the fissures in the parts that remained
standing it seemed that the emergence of the shock had
been more vertical in the upper part of the town than in
the lower, proving that whatever had been the angle
below, the hill had itself vibrated, which, being horizontal,
had modified the angle of the fissures.

Diano suffered but little, partly because it was well —
built, and partly on account of its situation, which was
such that before the shock reached it the disturbance
had to pass from beds of clay into nearly vertically placed.
beds of limestone. Also a great portion of the shock was
eut off by the Vallone del Raccio to the north and north-

1 See chapter ‘ Causes of Earthquakes’ for details of this myth.
2 Am. Jou. Sci. vol. x. p. 191.

EFFECTS PRODUCED UPON BUILDINGS. 143

west of the town. Here the effects of the partial extinc-
tion of the wave on the ‘free outlaying stratum’ were
visible in the masses of projected rock.

Castellucio did not suffer because its well buttressed
knoll was end on to the direction of shock, and on account
of a barrier of vertical breccia beds protecting it upon the
east.

Pertosa stands on a mound. The destruction was
least in the southern part of the town. From the relation
of the beds of breccia on which the town stands, and the
direction of the wave path, it is evident that the southern
part of the town received the force of the shock through
a greater thickness of the breccia beds than the other
parts did.

Petina, standing on a level limestone spur jutting out
from a mountain slope, suffered nothing, whilst Anletta
five miles to the south-west, and Pertosa six miles distant,
were in great part prostrated. (1) The terrace did not
vibrate, and (2) between Petina and Anletta there is almost
6,000 feet of piled up limestone, so that any shock emer-
gent at a steep angle had to pass up transversely through
these beds.

Protection of busldings.—In addition to giving
proper construction to our buildings, choosing proper
foundations and positions for them, something might
possibly be done to ward off the destructive effects of an
earthquake. We read that the Temple of Diana at
Ephesus was built on the edge of a marsh, in order to
ward off the effect of earthquakes. Pliny tells us that
the Capitol of Rome was saved by the Catacombs, and
Elisée Reclus! says that the Romans and Hellenes found
out that caverns, wells, and quarries retarded the disturb-
ance of the earth, and protected edifices in their neigh-

1 The Earth, p. 599.

144 EARTHQUAKES.

bourhood. The tower of Capua was saved by its numerous
wells. Vivenzis asserts that in building the Capitol the
Romans sunk wells to weaken the effects of terrestrial
oscillations. Humboldt relates the same of the inhabi-
tants of San Domingo.

Quito is said to receive protection from the numerous
cafions in the neighbourhood, whilst Lactacunga, fifteen
miles distant, has often been destroyed.

Similarly, it is extremely probable that many portions
of Tokio have from time to time been protected more or
less from the severe shocks of earthquakes by the numer-
ous moats and deep canals which intersect it.

Although we are not prepared to say how far artificial
openings of this description are effectual in warding off
the shocks of earthquakes, from theoretical considerations,
and from the fact that their use has been discovered by
persons who, in all probability, were without the means
of making theoretical deductions, the suggestions which
they offer are worthy of attention.

General conclusions.—The following are a few of the
more important results which may be drawn from the
preceding chapter :—

1. In choosing a site for a house find out by the
experience of others or experimental investigation the
localities which are least disturbed. In some cases this
will be upon the hills, in others in the valleys and on the
plains.

2. A wide open plain is less likely to be disturbed than
a position on a hill.

3. Avoid loose materials resting on harder strata.

4. If the shakings are definite in direction, place the
blank walls parallel to such directions, and the walls with
many openings in them at right angles to such direc-
tions.

; P below.

EFFECTS PRODUCED UPON BUILDINGS. 145

5. Avoid the edges of scarps or bluffs, both above and

6. So arrange the openings in a wall, that for horizontal
stresses the wall shall be of equal strength for all sections
at right angles.

7. Place lintels over flat arches of brick or stone.

8. To withstand destructive shocks either rigidly
follow one or other of the two systems of constructing an
earthquake-proof building. The light building on loose
foundations is the cheaper and probably the better.

9. Let all portions of a building have their natural
periods of vibration nearly equal.

10. If it is a necessity that one portion of a building
should have a very different period of vibration to the
remainder, as for instance a brick chimney in a wooden
house, it would seem advisable either to let these two
portions be sufficiently free to have an independent
motion, or else they must be bound together with great
strength.

11. Avoid heavy topped roofs and chimneys. If the
foundations were free the roof might be heavy.

12. In brick or stone work use good cement.

13.. Let archways curve into their abutments.

14. Let roofs have a low pitch, and the tiles, especially
those upon the ridges, be well secured.

146 EARTHQUAKES,

CHAPTER VIIL.
EFFECTS OF EARTHQUAKES ON LAND.

1. Cracks and fissures—Materials discharged from fissures—Explanation
of fissure phenomena. 2. Disturbances in lakes, rivers, springs,

wells, fumaroles, &c.—Explanation of these latter phenomena. —

3. Permanent displacement of ground—On coast lines—Level tracts
—Among mountains—Explanation of these movements.

Cracks and fissures formed in the ground.—Almost
all large earthquakes have produced cracks in the ground.
The cracks which were found in the ground at Yokohama
(February 22, 1880) were about two or three inches wide,
and from twenty to forty yards in length. They could
be best seen as lines along a road running near the upper
edge of some cliffs which overlook the sea at that place.
The reason that cracks should have occurred in such a
position rather than in others was probably owing to the
greater motion at such a place, due to the face of the cliff
being unsupported, and there Jeing no resistance opposed
to its forward motion. It often happens that earthquake
cracks are many feet in width. At the Calabrian earth-
quake of 1783, one or two of the crevasses which were
formed were more than 100 feet in width and 200 feet in
depth. Their lengths varied from half a mile to a mile.!
Besides these large cracks, many smaller ones of one or
two feet in breadth and of great length were formed. In

1 Lyell, Principles of Geology, vol. ii. chap. xxix,
Lp TY

EFFECTS OF EARTHQUAKES ON LAND. 147

the large fissures many houses were engulfed. Subse-
quent excavations showed that by the closing of the
fissures these had been jammed together to form one
compact mass. These cracks are usually more or less ©
parallel, and at the same time parallel to some topo-
graphical feature, like arange of mountains. For example,
the: cracks which were formed by the Mississippi earth-
quake of 1812 ran from north-east to south-west parallel
to the Alleghanies. By succeeding shocks these crevasses
are sometimes closed and sometimes opened still wider.
Their permanency will also depend upon the nature of
the materials in which they are made.

During an earthquake large cracks may suddenly open
and shut. .

During the convulsions of 1692 which destroyed Port
Royal, it is said that many of the fissures which were formed,
opened and shut. In some of these, people were entirely
swallowed up and buried. In others they were trapped
_ by the middle, and even by the neck, where if not killed
instantaneously they perished slowly. Subsequently their
‘projecting parts formed food for dogs.}

The earthquake which, July 18, 1880, shook the
Philippines caused many fissures to be found, which in
some places were so numerous that the ground was broken
up into steps. Near to the village of San Antonio the
soil was so disturbed that the surface of a field of sugar-
canes was so altered that in some cases the top of one row
of full grown plants was on a level with the roots of the
next. Into one such fissure. a boat disappeared, and into
another, a child.

Subsequently the child was excavated, and its body,
which was found a short distance below the surface, was
completely crushed.?

1 Gent. Mag. vol. xx. p. 212. *% Trans. Seis. Soc. vol. v. p. 67-68.

148 EARTHQUAKES,

At the time of the Riobamba earthquake, not only
were men engulfed, but animals, like mules, also sank into
the fissures which were formed.

The fissures which were formed at the time of the
Owen’s Valley earthquake in 1872 extended for miles nearly
parallel to the neighbouring Sierras. In some places the
ground between the fissures sank twenty or thirty feet,
and at one place about three miles east of Independence,
a portion of the road was carried eighteen feet to the south
by a fissure.!

Speaking generally, it may be said that all large
earthquakes are accompanied by the formation of fissures.
The Japanese have a saying that at the time of a large
earthquake persons must run to a bamboo grove.

The object of this is to escape the danger of being
engulfed in fissures, the ground beneath a bamboo grove
being so netted together with fine roots that it is almost
impossible for it to be rent open.

Materials discharged from fisswres.—Together with
the opening of cracks in the earth it often has happened
that water, mud, vapours, gases, and other materials, have
been ejected.

At the time of the Mississippi asriha ee water, mixed
with sand and mud, was thrown out with such violent
that it spurted above the tops of the highest trees. In
Italy such phenomena have often been repeated.

From the fissures which were formed in 1692 at the
time of the earthquakes in Sicily, water issued which in
some instances was salt.?

By the Cachar earthquake (January 10, 1869) numer-

ous fissures were formed parallel to the banks of a

river, from this water and mud were ejected. Dr.
Oldham, who describes this earthquake, says that the

1 Am. Jour. Sci. vol. iv. 2 Phil. Trans. vol. xviil.

|

EFFECTS OF EARTHQUAKES ON LAND. 149

first shot of dry mud or sand was mistaken for smoke or
steam. The water was foul, and hotter than surface
_ water at the time, but only slightly so; and the sulphur-
ous smell was nothing more than you would perceive in
stirring up the mud at the bottom of any stagnant pool
which had lain undisturbed for some time.!

In 1755, when Tauris was destroyed, boiling water
issued from the cracks which were formed. Similar
phenomena were witnessed at a place eight miles from
La Banca in Mexico, in the year 1820. Part of this hot
water was pure and part was muddy.

Sometimes the water which has been ejected has been
so muddy that the mud has been collected to form small
hills. This was the case at the time of the Riobamba
earthquake. The mud in this case consisted partly of —
coal, fragments of augite, and shells of infusoria.

At the time of the Jamaica earthquake men who had
fallen into crevices were in some cases thrown out again
by issuing water.

Sometimes, as has already been mentioned, vapour,
gases, and even flames issue from fissures. Vapour of
sulphur appears to be exceedingly common. Kluge says
that many fish were killed in consequence of the sulphur-
ous vapours which rose in the sea near to the coast of
New Zealand in 1855.

On December 14, 1797, an insupportable smell of
sulphur was observed to have accompanied the earth-
quake which at that time shook Cumana, which was
greatest when the disturbance was greatest.

Sulphurous fumes which were combustible were
belehed out of the earth at the time of the Jamaica
earthquake in 1692. The smell which accompanied this

1 Oldham and Mallet, ‘Cachar Earthquake,’ Proc. Gevlog. Soe.
1872.

150 EARTHQUAKES.

was so powerful that it caused a general sickness which
swept away about 3,000 persons.!

From the fissures formed at Concepcion in 1835, water,
which was black and fcetid, issued.?

The earthquakes of New England in 1727 were
accompanied by the formation of fissures, from which
sand and water boiled out in sufficient quantity to form
a quagmire. In some places ash and sulphur are said to
have been ejected.

At one house the stink of sulphur accompanying the
earthquake was so great that the family could not bear to
remain in doors.’

Emanations of gas sometimes appear to have burst
out from submarine sources.

Thus the earthquake at Lima, in March, 1865, was
accompanied with great agitation of the water and an
odour of sulphuretted and carburetted hydrogen. This
former gas was developed to such an extent that the
white paint of the U.S. ship ‘ Lancaster’ was blackened.4
With the smell, flames have sometimes been observed,
as, for instance, at the time of the Lisbon earthquake.

At the time of the earthquakes of 1811 and 1813, in
the Mississippi valley, steam and smoke issued from some
of the fissures which were formed.

Instances are recorded where stones have been shot
up from fissures unaccompanied by water, as, for instance,
at the earthquake of Pasto (January, 1834). It is imagined
that the propelling power must have been the sudden
expansion of escaping gases.

It has been suggested that flames seen above fissures

1 Phil. Trans. vols. li. and xviii.; Gent. Mag. vol. xx. 212,
2 Trans. Royal Geog. Soc. vol. vi.

3 Phil. Trans. vols. Xxxvi. and Xxxix.

4 Am. Jour. of Sct. 1865, vol. xl. p. 365.

EFFECTS OF EARTHQUAKES ON LAND. 15]

might perhaps be due to the burning ‘of materials like
sulphur. Mr. D. Forbes, who examined the effects of the
earthquakes of Mendoza, which were felt for a distance of
1,200 miles, says thut where the hard rock came to the
surface there were no traces of fissures, these being
entirely confined to the alluvium. The rumours of fire
and smoke having appeared at some of the fissures were
withcut foundation, the presumed smoke being nothing
but dust.! .
In addition to flames lights appear often to have been
observed, the origin of which cannot be easily explained.
The earthquake of November 22, 1751, at Genoa
is said to have been accompanied by a light like that
of a prodigious fire which seemed to arise out of the
ground.? — |
Explanation of fissure phenomena.—The manner in
which fissures are formed has already been explained
when referring to the want of support in the face of hills
(page 136).
Similar remarks may be applied to the banks of rivers
and all depressions, whether natural or artificial, which
have a steep slope. At such places the wave of shock
emerges on a free surface, which, being unsupported in
the direction of its motion, tends to tear itself away
from the material behind, and form a fissure parallel to
the face of the free surface. The distance of the fissure
from the face of the free surface will, theoretically, be
equal to half the amplitude of the wave of motion, one
half tending to move forwards, and the other half back-
wards. The reason that water and other materials rush
forth from fissures has been explained by Schiller as being
due to cracks having been opened through impervious
1 Proce. Geolog. Soc. Ap. 1875, p. 270.
2 Gent. Mag. vol. xxi. p. 569...
8

152 EARTHQUAKES,

strata, which, before the earthquake, by their continuity
prevented the rising of subterranean water under hydro-
static pressure.!

Kluge explains the coming up of the water as being
due to the same causes his he considers may be the
origin of disturbances in the sea.

The most reasonable explanations of the eruption of
water, mud, sand, and gas through fissures are those given
by Oldham and Mallet in their account of the Cachar
earthquake.

In the case of a horizontal shock passing through a
bed of ooze or water-bearing strata, the elastic wave will
tend to pack up the water during the forward motion to
such an extent that it will flow or spout up through any
aperture communicating with the surface. By the re-
petition of these movements causing ejections, sand or
mud cones, like those produced by a volcanic eruption,
may be formed, and by a similar action water may be shot
violently up out of wells, as was the case in Jamaica in
1692.

If an emergent wave acts through a water-bearing
bed upon a superincumbent layer of impervious material,
this upper layer is, during the upward motion, by its inertia
suddenly pressed down upon the latter.

This pressure is equal to that which would raise the
upper layer to a height equal to the amplitude of the
motion of an earth particle, and with a velocity at least
equal to the mean velocity of the earth particle resolved
in the vertical direction.

For a moment the water bearing strata receive an
enormous squeeze, and the water or mud starts up
through any crevice which may be formed leading to the
surface,

1 Jahrb. f. Min. 1840, p. 173... -

EFFECTS OF EARTHQUAKES ON LAND. 153

From this we see that liquids may rise far beyond the
level due to hydrostatic pressure.!

Volger has attributed the origin of lights or flames
appearing above fissures to the friction which must take
place between various rocky materials at the time when
the fissures are opened. As confirmatory of this he refers
___ to instances where similar phenomena have been observed
at the time of landslips. At the time of these landslips
the heat developed by friction has been sufficiently in-
tense to convert water into steam, the tension of which
threw mud and earth into the air like the explosion of a
mine.’

The gas eruptions which occasionally take place with
earthquakes are probably due to the opening of fissures
- communicating with reservoirs or strata charged with
| 4 products of natural distillation, or chemical action, which
| _ previously had accumulated beneath impervious strata.
Of the existence of such gases we have abundant evidence.
In coal mines we have fire-damp which escapes in increased
quantities with a lowering of the barometrical pressure.
| In volcanic regions we have many examples of natural
| __ springs of carbon dioxide.

These various gases sometimes escape in quantity, or
erupt without the occurrence of earthquakes. Rossi men-
q tions an instance where a few years ago quantities of fish
| _were killed by the eruption of gas in the Tiber, near Rome.
_ Another instance is one which occurred at. Follonica on
_ April 6, 1874. On the morning of that day many of the
streets and roads were covered with the dead bodies of
rats and mice. It seemed as if it had rained rats. From
the facts that the bodies of the creatures seemed healthy,

Oldham and Mallet, ‘ Cachar Earthquake,’ Trans. Geolog. Soc. Ap.
1872.
2 O. Volger, Unters. ib. d. Phin. d. Erdb, vol. iii. p. 414.

154 7 EARTHQUAKES.

that the destruction had happened suddenly, and not
come on gradually like an epidemic, it was supposed that
they had been destroyed by an emanation of carbon di-
oxide. The fact that many of them lay in long lines
suggested the idea that they had been endeavouring to
escape at the time of the eruption.’ If we can suppose
sudden developments of gas like this to have occasionally
accompanied earthquakes, we may sometimes have the
means of accounting for the sickness which has been felt.

Disturbances in lakes.—It has often been observed
that, at the time of large earthquakes, lakes have been
thrown into violent agitation, and their waters have been
raised or lowered. At the time of the great Lisbon earth-
quake, not only were the waters of European lakes thrown
into a state of oscillation, but similar effects were pro-
duced in the great lakes of North America. In some
instances, as in the case of small ponds, these movements
may be produced by the horizontal backward and forward
motion of the ground. At other times they are probably
due to an actual tipping of a portion of their basins.
Movements like these latter will be again referred to in
the chapter on Earth Pulsations. On January 27, 1856,
there was a shock of earthquake at Bailyborough, Ireland,
which occasioned an adjacent lough to overflow its banks
and rush into the town with great impetuosity. In return-
ing it swept away two men, leaving behind a great quantity
of pike and eels of a prodigious growth.’

Disturbances in rivers.—Just as lakes have been
disturbed, so also have there been sudden disturbances in
rivers. Sometimes these have overflowed their banks,
whilst at other times they have been suddenly dried up.
a certain cases the reason that a portion of a river should

2 ieee olan Endogen1, vol. i. p. 166.
2 Gent. Mag. vol. xxvi. p. 91.

EFFECTS OF EARTHQUAKES ON LAND. 155

have become dry has been very apparent, as, for instance, at
the time of the Zenkoji earthquake in Japan in 1847, when
__ the Shikuma-gawa became partly dry in consequence of the
large masses of earth which had been shaken down from
overhanging cliffs damming a portion of its course, and
| _ thus forming, first, lakes, and subsequently, new water-
| courses. As another example, out of the many which
| might be quoted, may be mentioned the sudden drying
up of the river Aboat, a tributary of the Magat, in the
Philippine Islands, on July 27,1881, shortly after a severe
shock of earthquake. The water of this river ceased to
flow for two hours, after which it reappeared with con-
siderable increase of volume and of a reddish colour.
Signor E. A. Casariego, who describes this, remarks that
the phenomenon could easily be explained through the
slipping down of the steep banks in narrow parts of its
upper valley, by which means its flow had been obstructed
until the water had time to accumulate and pass over or
demolish the obstruction. |
After the earthquake of Belluno (June 29, 1873), the
torrent Tesa, which is ordinarily limpid, became very
muddy.! Similar phenomena have been observed even in
Britain, as, for instance, in 1787, when, at the time of a
shock which was felt in Glasgow, there was a temporary
stoppage in the waters of the Clyde. Again, in 1110,
there was a dreadful earthquake at Shrewsbury and
Nottingham, and the Trent became so low at Nottingham
that people walked over it.

The earthquake of 1158, which was felt in many parts
of England, was accompanied by the drying up of the
Thames, which was so low that it could be crossed on foot
even at London.?

1 Compte Rendu, 1873, p. 66.
2 An Historical Account of Earthquakes, p. 46.

156 - EARTHQUAKES.

Facts analogous to these are mentioned in the accounts
of many large earthquakes. Sometimes rivers only be-
come muddy or change their colour. In an account of
the Lisbon earthquake we read that some of the’rivers
near Neufchatel suddenly became muddy.

At other times large waves are formed. Thus the
earthquake of Kansas (April 24, 1867) apparently created.
a disturbance in the rivers at Manhattan, which rolled in
a heavy wave from the north to the south bank.?

Sometimes curious phenomena have happened with
regard to rivers without the occurrence of earthquakes.
Thus, for instance, on November 27, 1838, there was
a simultaneous stoppage of the Teviot, Clyde, and
Nith.

In these rivers similar phenomena have been observed
in previous years.

Again, on January 1, 1755, there was a sudden sinking
of the river Frooyd, near Pontypool. This appears to
have been due to the water sinking into chasms which
were suddenly opened.’

Effects produced in springs, wells, fumaroles, ee
Springs also are often affected by earthquakes. Some-
times the character of their waters change; those which
were pure become muddy, whilst those which were hot
have their temperature altered.

Sometimes springs have been dried up, whilst at other
times new springs have been formed.

This latter was the case in New England (October 27,
1727). In some places springs were formed, whilst at
other places they were either entirely or partly dried
up."

At and near Lisbon, in 1755, some fountains became

1 Phil. Trans. vol. xlix. p. 436. 2 Am. Jour. Sci. vol. xlv. p. 129,
8 Phil. Trans. vol. xlix. p. 547. * Tbid. vols. xlii, and xxxix.

EFFECTS OF EARTHQUAKES ON LAND. 157

muddy, others decreased, others increased, and others
dried up. At Montreux, Aigle, and other places, springs

4 became turbid.

The baths at Toplitz, in Bohemia, which were dis-
covered in A.D. 762, were seriously affected by the same
earthquake. Previous to the earthquake it is said that
they had always given a constant supply of hot water.
At this time, however, the chief spring sent up vast
quantities of water and ran over. One hour before this —
it had grown turbid and flowed muddy. After this it
stopped for about one minute, but recommenced to flow
with prodigious violence, driving before it considerable
quantities of reddish ochre. Finally, it settled back to its
original clear state and flowed as before.’

In 1855, at the earthquake of Wallis, many new springs
burst forth, and some of these in Nicolai Thale were so
rich in iron that they quickly formed a deposit of ochre.

At the time of the Belluno earthquake (June 29,
1873),a hot spring, La Vena d’Oro, suddenly became red.?

The following examples of like epee ke are taken
from the writings of Fuchs.?

In 1738 the hot springs of St. Euphema rose ounuide®
ably in their temperature.

During the earthquake of October, 1848, the hot
springs of Ardebil, which usually had a temperature of
from 44° to 46° C., rose so high that their temperature
was sufficient to cause scalding. .

At the time of the earthquake of Wallis, i in 1855, the
temperature of hot springs rose 7°, and the quantity of
water increased three times.

During the earthquake of 1835 in Chili, the springs
1 Phil. Trans. vol. xlix. part i.

2 Compte Rendu, 1873, part ii. p. 66.
8 Die Vulcan. Ers. d. Erde, C. W. C. Fuchs,

158 . EARTHQUAKES.

of Cauquenes fell from 118° to 92° F. Subsequently,
however, they again rose.

Fumaroles are similarly disturbed. Thus, at the time
of the earthquakes of Martinique (September, 1875), the
fumaroles there showed an abnormal activity.}

Wells often appear to be acted upon in the same
manner as springs.

At the time of the California earthquake (April, 1855),
the level of the water in certain wells was raised ten to
twelve feet.

A consequence of the earthquake at Neufehatel, in
1749, was to fill some of the wells with mud.? At
Constantinople, on September 2, 1754, wells became
dry.’ |

Explanation of the above phenomena.—That the
water in springs and wells should be caused to rise at
the time of an earthquake, admits of explanation on the
supposition of compressions taking place similar to those
which cause the rise of water in fissures. That the water
in wells and springs should be rendered turbid, is partly
explained on the supposition of more or less dislocation
taking place in the earthy or rocky cavities in which they
are contained or through which they flow. |

At the time of a large earthquake it is extremely
probable that there is a general disturbance in the lines of
circulation of subterranean waters and gases throughout
the shaken area. By these disturbances, new waters may
be brought to the surface, two or more lines of circulation
may be united, and the flow of a spring or supply of
a well be augmented. Fissures, through which waters
reached the surface, may be closed, wells may become dry,
or springs may cease to flow, hot springs may have their

1 Compte Rendu, 1875, p. 693. 2 Gent. Mag. vol. xix. p. 190.
8 Phil. Trans, vol. xlix. p. 115.

=

- ” Pe

a
_
Ca
oe

a
1c
ye

» =<
aA oe is was 2 pss, es

EFFECTS OF EARTHQUAKES ON LAND. 159

temperature lowered by the additions of cold water from
another source, and, in a similar manner, waters may be
altered in their mineralisation. An important point to
be remembered in this consideration is the mutual de-
pendence of various underground water supplies, and the
area over which any given supply may circulate. A well
in the higher part of Lincoln Heath is said to be governed
by the river Trent, which is ten miles distant ; when the
river rises the well rises in proportion, and when the river
falls the water in the well falls.

The change which is usually observed in hot springs
is, that before or with earthquakes they increase in tem-
perature, but afterwards sink back to their normal state.

_ This increase in temperature may possibly be due to com-

munication being opened with new or deeper centres of
voleanic activity, or a temporarily increased rate of flow.

That the water issuing from newly formed fissures or
springsshould be hot, might be explained on the supposition
of its arising from a considerable depth, or from some
volcanic centre. It might also be attributed to the heat
developed by friction at the opening of the fissures.
These changes which earthquakes produce upon the
underground circulation of waters are phenomena deserv-
ing especial attention. Although we know much about
the circulation of surface water, it is but little that we
yet know about the movement of the streams hidden from
view, from which these surface waters have their sources.
Earthquakes may be regarded as gigantic experiments on
the circulatory system of the earth, which, if properly in-
terpreted, may yield information of scientific and utilitarian
value.

The sudden elevations, depressions, or lateral shifting
of large tracts. of country at the time of destructive earth-

1 Gent. Mag. vol. xxi. 1751,

160 EARTHQUAKES.

quakes are phenomena with which all students of geology
are familiar. In most cases these displacements have
been permanent; and evidences of many of the move-
ments which occurred within the memory of man, remain
as witnesses of the terrible convulsions with which they
were accompanied.

Movements on coast lines and level tracts.—At the
time of the great earthquake of Concepcion, on February
20, 1835, much of the neighbouring coast line was sud-
denly elevated four or five feet above sea level. This, how-
ever, subsequently sank until it was only two feet. A rocky
flat, off the island of Santa Maria, was lifted above high-
water mark, and left covered with ‘ gaping and putrefying
mussel-shells, still attached to the bed on which they had
lived.’ The northern end of the island itself was raised
ten feet and the southern extremity eight feet. 7

By the earthquake of 1839, the island of Lemus, in the
Chonos Archipelago, was suddenly elevated eight feet.?

Of movements like these, especially along the western
shores of South America, Darwin, who paid so much atten-
tion to this subject, has given many examples. In 1822,
the shore near Valparaiso was suddenly lifted up, and
Darwin tells us that he heard it confidently asserted ¢ that
a sentinel on duty, immediately after the shock, saw a part
of a fort which previously was not within the line of his
vision, and this would indicate that the uplifting was
not vertical.’ That the large areas of land should be
shifted permanently in horizontal directions, as well as
vertically, we should anticipate from the observations

-which we are able to make upon large fissures which are

caused by earthquakes.
- Another remarkable example of sudden movement in

' Jour. Royal Geo. Soc. vol. vi. p. 319.
2 Darwin, Geolog. Observations, p. 232. 8 Thid. p. 245.

EE A RA SF OLS ade On eae eee Dk OT TR RE Ae ie Reh ree et Re Te PE Pree PR
Ried Boia eer i ee ee a ae em Te a Oe ee eee, ee ee a 7 a4 >

EFFECTS OF EARTHQUAKES ON LAND. 161

the rocky crust is that which took place during the earth-
quakes of 1811-12 in the valley of the Mississippi, near to

the mouth of the Ohio, which was. convulsed to such a

degree, that lakes, twenty miles in extent, were formed in
the course of an hour. This country, which is called the
‘sunk country,’ extends some seventy to eighty miles
north and south, and thirty miles east and west.!

In the ‘ Gentleman’s Magazine’ we read of the little
territory of Causa Nova, in Calabria, being sunk twenty-
nine feet into the earth by an earthquake, without throwing
down a house. The inhabitants, being warned by a noise,
escaped into the fields, and only five were killed.?

Other examples of these permanent dislocations of
strata are to be found in almost every téxt-book on
geology.

Geological changes produced.— Passing over the
accounts of earth movements which are more or less ficti-
tious, and confining our attention to the well authenticated
facts, we see at once the important part which earthquakes
have played as agents working geological changes. Even
in the nineteenth century long tracts of coast, as in Chili
and New Zealand, have been raised, whilst other areas, like
the Delta of the Indus, have been sunk. Sir H. Bartle
Frere, speaking about the disturbance which took place in
this latter region in 1819, remarks that all the canais
drawn from the Fullalee River ceased to run for about
three days, probably indicating a general upheaval of the
lower part of the canal. In conseyuence of the earth-
quakes in former times it is not unlikely that water-courses
have ceased to flow, water has decreased in wells, and
districts have been depopulated.’

1 Lyell, Principles of Geology, vol. ii. pp. 107-8.
2 Gent. Mag. 1733, vol. iii. p. 217.
$ «Farthquakes of Cutch,’ Jour. Royal Geo. Suc. vol. x1.

162 | EARTHQUAKES.

Sometimes these changes have taken place gradually,
and sometimes with violence. Mountains have been
toppled over, valleys have been filled, cities have been
submerged or buried.

With the records of these convulsions before us, we

see that seismic energy yet exhibits a terrible activity in
changing the features of the globe.

Reason of these movements.—To formulate a single
reason for these catastrophes would be difficult. Where
they are of the nature of landslips, or materials have been
dislodged from mountain sides, the cause is evidently the
sudden movement of this ground acting upon strata not
held together in a sufficiently stable condition. A similar
explanation*may be given for the sudden elevations or
depressions of strata in a district removed from the centre
where the disturbance had its origin. The seismic effort
exhibits itself in a certain area round its origin as a sudden
push, and by this push, strata are fractured and caused to
move relatively to each other.

At or near to the origin of an earthquake it might
be argued that it was the sudden falling of rocky strata
towards a position of stable equilibrium that caused the
shaking, and in such a case the movements referred to
may be regarded as the cause rather than the effect of an,
earthquake.

A subject closely connected with the sudden dislocation
of strata, is the production of secondary or consequent
earthquakes, due to the disturbance of ground in a critical
state (see p. 248),

CHAPTER IX.
DISTURBANCES IN THE OCEAN.

Sea vibrations—Cause of vibratory blows—Sea waves: Preceding
earthquakes; Succeeding earthquakes — Magnitude of waves—
Waves as recorded in countries distant from the origin—Records
on tide gauges—Waves without earthquakes—Cause of waves—
Phenomena difficult of explanation—Velocity of propagation—
Depth of the ocean—Examples of calculations—Comparison of
velocities of earthquake waves with velocities which ought to exist
from the known depth of the ocean.

Sea vibrations.—Whilst residing in Japan I have had
many opportunities of conversing with persons who had
experienced earthquakes when on board ships, and it has
often happened that these same earthyuakes have been
recorded on the shore. For example, at the time of every
moderately severe earthquake which has shaken Yoko-
hama, the same disturbance has been felt on board the
ships lying in the adjoining harbour. In some cases the
effect had been as if the ship was grounding ; in others, as
if a number of sharp jerks were being given to the cable.
The effect produced upon a. man-of-war lying in the
Yokohama harbour on the evening of March 11, 1881,
was described to me as a ‘violent irresistible shaking.’
Vessels eighty miles at sea have recorded and timed shocks
which were felt like sudden blows. These were accom-
_ panied by a noise described as a ‘dull rattle like
thunder.’

164 EARTHQUAKES.

In none of the cases here quoted was any disturbance
of the water observed.

The great earthquake of Lisbon was felt by vessels on
the Atlantic, fifty miles away from shore.

On February 10, 1716, the vessels in the harbour of New
Pisco were so violently shaken that both ropes and masts
were broken, and yet no motion in the water was observed.
Some have described these shocks like those which would
be produced by the sudden dropping of large masses of
ballast in the hold of the vessel. Other cases are known
where rigging was damaged, and even cannon have been
jerked up and down from the decks on which they rested.

Cause of vibratory blows.—From the rattling sound
which has accompanied some of these submarine shocks,
many of which, it may be remarked, have never been re-
corded as earthquakes upon neighbouring shores, it does
not seem improbable that they may have been the result
of the sudden condensation of volumes of steam. produced
by submarine volcanic eruptions.

As confirmatory of this supposition we have the fact,
that many of the marine disturbances which might be
called ‘sea-quakes,’ have been observed in places which
are close to, or in the line of, volcanic vents. Thus, M.
Daussy, who has paid special attention to this subject, has
collected evidence to show that a large number of shocks
have been felt by vessels in that portion of the Atlantic
between Cape Palamas, on the west coast of Africa, and
Cape St. Roque, on the east coast of South America.!

Some of the vessels only felt shocks and tremblings,
but others saw smoke, and some even collected floating
ashes. In considering the submarine shocks of this par-

1M. Daussy, ‘ Sur l’existence probable d’un volcan sousmarin situé
ar environ 0° 20/ de lat. S., et 22° 0’ de ee ouest,’ Comptes pee
vol. vi. p. 512.

DISTURBANCES IN THE OCEAN. 165

ticular area, we must bear in mind that it lies in the line
of Iceland, the west coast of Scotland, the Azores, Canaries,
Cape de Verd Islands, St. Helena, and other places, all of
which, if not at present in volcanic activity, shew evidence
of having been so within recent times. The connection
between volcanic action and earthquakes will be again
referred to.

Sea waves.—Although in the above-mentioned in-

stances sea waves have not been noticed, it is by no means

uncommon to find that destructive earthquakes have been
accompanied by waves of an enormous size, which, if the
earthquake has originated beneath the sea, have, subse-
quently to the shaking, rolled in upon the land, to create
more devastation than the actual earthquake. It may,
however, be mentioned that a few exceptional cases exist
when it is said that the sea wave has preceded the earth-
quake, as, for example, at Smyrna, on September 8, 1852.

Again, at the earthquake in St. Thomas, in 1868, it is
said that the water receded shortly befove the first shock.
When it returned, after the second shock, it was sufficient
to throw the U.S. ship ‘ Monagahela’ high and dry.!

Another American ship, the ‘ Wateree,’ was also lost in
1868 by being swept a quarter of a mile inland by the sea
wave which inundated Arequippa.

Much of the great destruction which occurred at the
time of the great Lisbon earthquake was due to a series cf
great sea waves, thirty to sixty feet higher than the highest
tide, which swamped the town. These came in about an
hour after the town had been shattered by the motion of
the ground.

The first motion in the waters was their withdrawal,
which was sufficient to completely uncover the bar at the
mouth of the Tagus. At Cadiz, the first wave, which was

1 Am. Jour. Sci. vol. xlv. p. 133.

166 EARTHQUAKES.

the greatest, is said to have been sixty feet in height.
Fortunately the devastating effect which this would have
produced was partially warded off by cliffs.

At the time of the Jamaica earthquake (1692) the sea
drew back for a distance of a mile.

In South America sea waves are common accompani-
ments of large earthquakes, and they are regarded with
more fear than the actual earthquakes.

On October 28, 1724, Lima was destroyed, and on
the evening of that day the sea rose in a wave eighty feet
over Callao. Out of twenty-three ships in the harbour,
nineteen were sunk, and four others were carried far
inland. The first movement which is usually observed is
a drawing back of the waters, and this is so well known
to precede the inrush of large waves, that many of the
inhabitants in South America have used it as a timely
warning to escape towards the hills, and save themselves
from the terrible reaction which, on more than one eee
has so quickly followed.

At Caldera, near to Copiapo, on May 9, 1877, which was
the time when Iquique was devastated, the first motion
which was observed in the sea was that it silently drew
back for over 200 feet, after which it rose as a wave over
five feet high. At some places the water came in as
waves from twenty to eighty feet in height.

At Talcahuano, on the coast of Chili, in 1835, there was
a repetition of the phenomena which accompanied the
destruction of Penco in 1730 and 1751. About forty
minutes after the first shock, the sea suddenly retired.
Soon efterwards, however, it returned in a wave twenty
feet high, the reflex of which swept everything towards
the sea. These phenomena were repeated three times.!

When Callao and Lima were destroyed, in 1746, the

! Am. Jour. Sci. vol. xiv. p. 209.

DISTURBANCES IN THE OCEAN. 167

sea first drew back, then came in as waves, four or five
minutes after the earthquake. Altogether, between October
28 and February 24, 451 shocks were counted. At one
time the sea came in eighty feet above its usual level.
One account says that the large waves came in forty-one
and a half hours after the first shock, and seventeen and
a half hours after comparative tranquillity had pre-
vailed.!

At the eruption of Monte Nuovo, near Naples, in
September 27, 1538, the water drew back forty feet, so
that the whole gulf of Baja became dry.

In 1696, at the time of the Catanian earthquake, the
sea is said to have gone back 2,000 fathoms. Instances
are recorded where the sea has receded several miles.

The time taken for the flowing back of the sea is
usually very different. Sometimes it has only been five
or six minutes, whilst at other times over half an hour,
and there are records where the time is said to have been
still longer.

Thus, at the earthquake of Santa(June 17, 1678), the
sea is stated to have gone as far back as the eye could reach,
and did not rise again for twenty-four hours, when it
flooded everything.

In 1690 at Pisco the sea went back aie sible and did
not return for three hours. When it returns it does
so with violence, and examples of the heights to which
it may reach have been given. The greatest sea wave
yet recorded, according to Fuchs, is one which, on
October 6, 1737, broke on the coast of Lupatka, 210 feet
in height.

There are, however, cases known where the sea has
returned as gradually asit went out. Thus, on December

1 D.C. F. Winslow, ‘ Tides at Tahiti,’ Am. Jour. Sci. 1865, p. 45 ; also
Mailet’s Catalogue of Earthquakes.

168 EARTHQUAKES.

4, 1854, when Acapulco was destroyed, the sea is said to
have returned as gently as it went out.

When sea waves have travelled long distances from
their origin, as, for instance, whenever a South American
wave crosses the Pacific to Japan, the phenomena which
are observed are like those which were observed at
Acapulco; the sea falls and rises, at intervals of from ten
minutes to half an hour, to heights of from six to ten feet,
without the slightest appearance of a wave. Its phe-—
nomenon is like that of an unusually high tide, which
repeats itself several times per horu. Even if we watch
distant rocks with a telescope, although the surface of
the ocean may be as smooth as the surface of a mirror,
there is not the slightest visible evidence of what is
popularly called a wave. The sea being once set in
motion it continues to move as waves of oscillation for a
considerable time. In 1877, as observed in Japan, the
motion continued for nearly a whole day. The period
and amplitude of the rise and fall were variable, usually -
it quickly reached a maximum, and tnen died out gradually.
As observed in a self-recording tide gauge at San Francisco,
the disturbance lasted for about four days. A diagram of
this is here given. In its general appearance it is very
similar to the records of other earthquake waves. The
large waves represent the usual six hours rise and fall of
the tides; usually these are fairly smooth curves. Super-
imposed on the large waves are the smaller zigzag curves
of the earthquake disturbance, lasting with greater or less
intensity for several days. As these curves are drawn to
scale—horizontally for hours, and vertically one fifth
inch to the foot, to show the extent of the rise and fall—
they will be easily understood.

Sometimes, as in the present example, the first move-
ment in the waters is that of an incoming wave. In many

DISTURBANCES IN THE OCEAN. 169

instances, however, this observation may be due to the
slow and more gentle phenomena of the previous drawing
out of the water, which in a steep waste, or when the water
is rough, would be difficult to observe, not having been
remarked.

The distance to which these sea waves have extended
has usually been ae great.

a: eM

an eel rela, alah
aS eh
ac anaueaa She

aa ese FU
peer LLNS

EEE COCC ECC CISSe

Fic. 28.—Record of Tide Gauge at Port Point, San Francisco. Showing
; Earthquake Waves of May 1877.

The sea wave of the Iquique earthquake of May 9,
1877, like many of its predecessors, was felt across the
basin of the whole Pacific, from New Zealand in the south,
to Japan and Kamschatka in the north. And but for the
intervention of the Eurasian and American continents

170 EARTHQUAKES.

would have made itself appreciable over the surface of the
whole of our globe. At places on the South American
coast, it has been stated that the height of the waves varied
from twenty to eighty feet. At the Samoa Islands the
heights varied from six to twelve feet. In New Zealand
the sea rose and fell from three to twenty feet. In Australia
the heights to which the water oscillated were similar to
those observed in New Zealand. In Japan it rose and fell
from five to ten feet. In this latter country, the phenomena
of sea waves which follow a destructive earthquake on the
South American coast are so well known that old residents
have written to the local papers announcing the probability
of such occurrences having taken place some twenty-five
hours previously in South America. In this way news of
great calamities has been anticipated, details of which only
arrived some weeks subsequently. Just as the destructive
earthquakes of South America have announced themselves
in Japan, in a like manner the destructive earthquakes of
Japan have announced themselves upon the tide gauges
of California. Similarly, but not so frequently, disturbances
shake the other oceans of the world. :

For example, the great earthquake of Lisbon propagated
waves to the coasts of America, taking on their journey
nine and a half hours.

Sea waves without earthquakes.—Sometimes we get
great sea waves like abnormal tides occurring without
any account of contemporaneous earthquakes. Although
earthquakes have not been recorded, these ill understood
phenomena are usually attributed to such movements.

Several examples of these are given by Mallet. Thus,
at 10 A.M. on March 2, 1856, the sea rose and fell fora
considerable distance at many places on the coast of York-
shire. At Whitby, the tide was described ebbing and
flowing six times per hour, and this to such a distance

DISTURBANCES IN THE OCEAN. 171

that a vessel entering the harbour was alternately afloat
and aground.

In 1761, 0n July 17, a similar phenomena was observed
at the same place.

A like occurrence took place at Kilmore, in the county
of Wexford, on September 16, 1864, when the water ebbed
_ and flowed seven times in the course of two hours and a
half. These tides, which appear to have taken about five
minutes to rise and five minutes to fall, were seen by an
observer approaching from the west as six distinct ridges
of water. The general character of the phenomena appears
to have been very similar to that which was produced at
the same place by the Lisbon earthquake of 1755; and
the opinion of those who saw and wrote about their
occurrence was that it was due to an earthquake disturb-
ance. Such phenomena are not uncommon on the Wexford
coast, where they are popularly known as ‘death waves,’
probably in consequence of the lives which have been lost
by these sudden inundations.

They have also been observed in other parts of Ireland,
the north-east coast of England, and in many parts of the
globe. They will be again referred to under the head of
earth pulsations. . ;

Cause of sea waves.—Mallet, who in his report to the
British Association in 1858, writes upon this last-mentioned
occurrence at considerable length, whilst admitting that
many may have originated from earthquakes, he thinks it
scarcely probable that an earthquake blow, sufficiently
powerful to have produced waves like those observed at
Kilmore, should not have been felt generally throughout
the south of Ireland. He, therefore, suggests that some-
times waves like the above might be produced by an
underwater slippage of the material forming the face of a
submarine bank, the slope of which by degradation and

2 | EARTHQUAKES.

deposition, produced by currents, had reached an angle
beyond the limits of repose of the material of which it
was formed. Mallet does not insist upon the existence
of these submarine landslips, but only suggests their
existence as a means of explaining certain abnormal sea
waves which do not appear to have been mee by
earthquakes.

In the generality of cases sea waves are accompanied
by earthquakes, but it may often happen that the connec-
tion between the two is difficult to clearly establish. One
simple explanation for the origin of waves occurring with
earthquakes, is, that in consequence of the earthquake a
large volume of water suddenly finds its way into cavities
which have been opened, the disturbance produced by the
inrush giving rise to waves.

A second explanation is, that the land along a shore is
caused by an earthquake to oscillate upwards, the water
running off to regain its level. A supposition like this is
negatived by the fact that these disturbances are felt far
away from the chief disturbance, on small islands. Also, it
may be added, that the whole disturbance appears to
approach the land from the sea, and not in the opposite
direction. Thus,in the earthquake of Oahu (February 18,
1871), it was remarked that the shock was first felt by
the ships farthest from the land.!

Another suggestion is that the waves are due toa
sudden heaving up of the bottom of the ocean. If this
lifting took place slowly, then the first result would be
that the water situated over the centres of disturbance
would flow away radially in all directions from above the
area of disturbance.

If, however, the submarine upheaval took place with
great rapidity, say by the sudden evolution of a large

1 Am. Jour. Sct. vol. i. p. 469.

=

DISTURBANCES IN THE OCEAN, 73

volume of steam developed by the entry of water into a
volcanic vent, as the water was heaped above the disturbed
area, water might run in radially towards this spot.

Supposing a primary wave to be formed in the ocean
by any such causes, then the falling of this will cause a
second wave to be formed, existing as a ring round the
first one. The combined action of the first and second
wave will form a third one, and so the disturbance, start-
ing from a point, will radiate in broadening circles.
During the up and down motion of these waves, the
energy which is imparted to any particle of water will,
on account of the work which it has to do in displacing its
neighbours, by frictional resistance, gradually grow less
and less, until it finally dies away. The waves which are
the result of this motion will also grow less and less.

If a series of sea waves were produced by a single dis-
turbance, we see that these will be of unequal magnitude.
Now, for small waves, the velocity with which they travel
depends upon the square root of their lengths; but with
large waves, like earthquake waves, the velocity depends
upon the square root of the depth of water, and these
latter travel more quickly than the former.

If, therefore, we have a series of disturbances of un-
equal magnitude producing sea waves, which, from the
‘series of shocks which have been felt upon shores subse-
quently invaded by waves, seems in all probability often
to have been the case, it is not unlikely that the waves of
an early disturbance may be overtaken and interfered with
by a series which followed.

These considerations help us to understand the appear-
ance of the records on our tide gauges, and also the
phenomena observed by those who have recorded tidal
waves as they swept inwards upon the land. For instance,
we understand the reason why sea waves, as observed at

174 EARTHQUAKES.

places at different distances from the origin of a disturb-
ance, should be of different heights. We also see an
explanation for the fact that small waves should some:
times appear to be interpolated between large ones, and
that these should occur at varying intervals. !

The fact that whenever a wave is produced, a certain
quantity of water must be drawn from the level which
surrounds it, in order that it should be formed, explains
the phenomena that the sea is often observed first to
draw back. Out in the open ocean it is drawn from the
hollow between two waves. As has been pointed out by
Darwin, it is like the drawing of the water from the shore
of a river by a passing steamer.

The difference in the height of waves, as obseaued at
places lying close to each other, is probably due to the con-
figuration of the coast, the interference of outlying islands,
reefs, &c.—causes which would produce similar effects in
the height of tide.

As a wave approaches shallow water it gradually in-
creases in height, its front slope becomes steep, and its
rear slope gentle, until finally it topples over and breaks.
This increasing in height of waves is no doubt connected
with the destruction of Talcahuano and Callao, which are
situated at the head of shallow bays. Valparaiso, which is
on the edge of deep water, has never been overwhelmed.'
Another case tending to produce anomalies in the cha-
racter of waves would be their reflection and mutual in-
terference, the reflections due to the configuration of the
ocean bed and coast lines.

The complete phenomena which may accompany a
violent submarine disturbance are as follows :—

By the initial impulse of explosion or lifting of the
ground, a ‘great sea wave’ is generated, which travels

1 Darwin, Researches in Geology, S¢., p. 378.

DISTURBANCES IN THE OCEAN. 175

shorewards with a velocity dependent upon its size and
the depth of the ocean. At the same instant, a ‘ sound
wave’ may be produced in the air, which travels at a
quicker rate than the ‘great sea wave.’ A third wave
which is produced, is an ‘earth wave,’ which will reach
the shore with a velocity dependent on the intensity of the
impulse and the elasticity of the rocks through which it is
propagated. This latter, which travels the fastest, may
carry on its back a small ‘ forced sea wave.’ On reaching
the shore and passing inland, this ‘earth wave’ will cause
a slight recession of the water as the ‘forced sea wave’
slips from its back.

As these ‘forced sea waves’ travel they will give
blows to ships beneath which they may pass, being trans-
mitted from the bottom of the ocean to the bottom of the
ships like sound waves in water. At the time of small
earthquakes, produced, for example, by the explosion of
small quantities of water entering volcanic fissures, or by
the sudden condensation of steam from such a fissure
entering the ocean, aqueous sound waves are produced,
which cause the rattling and vibrating jars so often
noticed on board ships.

Phenomena difficult of explanation.—Although we
ean in this way explain the origin and phenomena of sea.
waves, we must remember, as Kluge has pointed out, that
it is not the simple backward and forward movement of
the ground which produces sea waves, and that the majority
of earthquakes which have occurred in volcanic coasts
have been unaccompanied by such phenomena. Out of
15,000 earthquakes observed on coast lines, only 124

were accompanied by sea waves.) Out of 1,098 earth-

quakes catalogued by Perrey for the west coast of South

_ America, only nineteen are said to have been accompanied
1 Kluge, Jahrb. f. Min. 1861, p. 977.

9

176 EARTHQUAKES.

by movements in the waters. According to the ‘ Geogra-
phical Magazine’ (August 1877, p. 207), it would seem
that out of seventy-one severe earthquakes which have
occurred since the year 1500 upon the South American
coast many have been accompanied by sea waves. Darwin
also remarks, when speaking of South America, that almost
every large earthquake has been accompanied by consider-
able agitation in the neighbouring sea.}

On April 2, 1851, when many towns in Chili were
destroyed, the sea was not disturbed. At the time of the
great earthquake of New Zealand (June 23, 1855), al-
though all the shocks came from the sea, yet there was |
no flood. The small shock of February 14, however, was
accompanied by a motion in the sea.

To these examples, which have been chiefly drawn
from the writings of Fuchs, must be added the fact that
the greater number of disturbances which are felt in the
north-eastern part of Japan, although they emanate from
beneath the sea, do not produce any visible sea waves.
They are, however, sufficient to cause a vibratory motion
on board ships situated near their origin.

Another point referred to by Fuchs, as difficult of
explanation, is, that the water, when it draws back, often
does so with extreme slowness, and farther, in some in-
stances, it has not returned to its original level. That
the sea might be drawn back for a period of fifteen or
thirty minutes is intelligible, when we consider the great
length of the waves which are formed. Cases where it
has retired for several hours or days, and when its
original level is altered, appear only to be explicable on
the assumption of more or less permanent changes in the
levels of the ground. For example, in the earthquake of
1855 which shook New Zealand, the whole southern por-
tion of the northern island was raised several feet.

' Darwin, Voyage of a Naturalist, p. 309

DISTURBANCES IN THE OCEAN, 177

These sudden alterations in the levels of coast lines
have already been referred to.

Other points which are difficult to understand are the
occurrence of disturbances in the sea at the time of feeble
earthquakes, and with earthquakes occurring in distant
places. As examples of such occurrences, Fuchs quotes
the following: ‘On May 16, 1850, at 4.28 a.M., an earth-
quake took place in Pesth, and at 7.30 a motion was
observed in the sea at Livorno. Again, at the time of the
earthquake of December 19, 1850, which shook Heliopolis,
a flood suddenly came in upon Cherbourg.’ May not these
phenomena be the result of an earth pulsation, which
produced an earthquake at one point, and a sea wave at

another ?
Equally difficult to understand are the observations

when the disturbance in the sea has occurred several
hours after an earthquake; as, for instance, at Batavia, in
1852, when there was an interval of two hours; and to
this must be added the observations where the motion of
the sea has preceded that of the earthquake—as, for in-
stance, in 1852, at Smyrna. Whilst recognising the fact
that it is possible to suggest explanations for many of
these anomalies, we must also bear in mind that they are,
generally speaking, exceptional, and, in some instances,
may possibly be due to errors in observations.

Velocity of propagation of sea waves, and depth
of the ocean.—It has long been known to physical science
that the velocity with which a given wave is propagated
along a trough of uniform depth, holds a relation to the
depth of the trough.

If v is the velocity of the wave, and h the depth of
the trough, this relation may be expressed as follows :-—

178 EARTHQUAKES.

Where g = 32°19 and k& = 5°671.

It will be observed that these two formule (the first of
which is known as Russell’s formula, and the second as
Airy’s) are practically identical.

The apparent difference is in the average value as-
signed to the constant. |

For large waves such as we have to deal with, it would
be necessary, if we were desirous of great accuracy, to
increase the value of h by some small fraction of itself.
We might also make allowance for the different values of
g, according to our position on the earth’s surface. With
these formule at our disposal it is an easy matter, after
having determined the velocity with which a wave was
propagated, to determine the average depth of the area
over which it was transmitted.

In making certain earthquake tnvestigations the re-
verse problem is sometimes useful—namely, determining
the velocity with which a sea wave has advanced upon a
shown line, from a knowledge of the depth of the water
in which it has been propagated.

Calculations of the average depths of the Pacific, de-
pendent on the velocity with which earthquake waves
have been propagated, have been made by many investi-
gators.

In most cases, however, in consequence of having
assumed the wave to have originated on a coast line,
when the evidence clearly showed it to have originated
some distance out at sea, the calculations which have
been made are open to criticism. The average depths
which I obtained for various lines across the Pacific
appear to be somewhat less than the average depth as
given by actual soundings. We must, however, remember
that the common error in actual soundings is that they
are usually too great, it being difficult in deep-sea sound-

DISTURBANCES IN THE OCEAN. 179

a ing to determine when the lead actually reaches the
_ bottom. Until oceans have been more thoroughly sur-

_ veyed with the improved forms of sounding apparatus,

we shall not be able to verify the truth of the results
_ which have been given to us by earthquake waves.

EXAMPLES OF CALCULATIONS ON SEA WAVES.

1. The wave of 1854.—This wave originated near
Japan, and it was recorded on tide gauges at San Francisco,
San Diego, and Astoria.

On December 23, at 9.15. A.M., a strong shock was felt
at Simoda in Japan, which, at 10 o’clock, was followed by a
large wave thirty feet in height. The rising and falling
of the water continued until noon. Half an hour after,
the movement became more violent than before. At
2.15 p.M. this agitation decreased, and at 3 P.M. it was
comparatively slow. Altogether there were five large
waves.

On December 23 and 25, unusual waves were recorded
upon the self-registering tide gauges at San Francisco,
San Diego, and Astoria.

At San Francisco three sets of waves were observed.
The average time of oscillation of one of the first set was
thirty-five minutes, whilst one of the second and third sets
was almost thirty-one minutes.

At San Diego three series of waves were also shown, but
with average times of oscillation of from four to two minutes
shorter than the waves at San Francisco.

The San Francisco waves appear to indicate a re-
currence of the same phenomena.

The record at San Diego shows what was probably the
effect of a series of impulses, the heights increasing to the

:
:

180 EARTHQUAKES,

third wave, then diminishing, then once more renewed,
after which it died away.
The result of calculations based on these data were :—

Distance Time Velocity Depth of
geographi-| of trans- in feet ocean in
cal miles | mission per sec. fathoms

———_—_—— |

Simoda to San Diego Ar ame 8 Oy a fet a 545 2100
Simoda to San Francisco 4527 12 39 528 2500 or 2230

{

The difference for the depths in the San Francisco
path depends whether the length of the waves is reckoned
at 210 or 217 miles. The length of the waves on the
San Diego path were 186 or 192 miles,!

The wave of 1868.—On August 11, 1868, a sea wave
ruined many cities on the South American coast, and
25,000 lives were lost. This wave, like all the others,

_ travelled the length and breadth of the Pacific.

In Japan, at Hakodate, it was observed by Captain T.
Blakiston, R.A., who very kindly gave me the following
account :

On August 15, at 10.30 A.M., a series of bores or tidal
waves commenced, and lasted until 3 P.M. In ten minutes
there was a difference in the sea level of ten feet, the water
rising above high water and falling below low water mark
with great rapidity. The ordinary tide is only two and a
half to three feet. The disturbance producing these waves
originated between Iquique and Arica, in about lat. 18.28
S. at about 5 p.m. on August 13. In Greenwich time this
would be about 13h. 9m. 40s. August 13. The arrival of
the wave at Hakodate in Greenwich time would be about
14h, 7m. 6s. August 14: that is to say, the wave took
about 24h. 57m. to travel about 8,700 miles, which

1 Prof. A. D. Bache, United States Coast Survey Report, 1855, p. 342,

DISTURBANCES IN THE OCEAN. 181

gives us an average rate of about 511 feet per second,
These waves were felt all over the Pacific. At the
Chatham Islands they rushed in with such violence that
whole settlements were destroyed. At the Sandwich
Islands the sea oscillated at intervals of ten minutes for
three days.

Comparing this wave with the one of 1877 we see that
one reached Hakodate with a velocity of 511 feet per second,
whilst the other travelled the same distance at 512 feet
per second.

An account of this earthquake wave: has been given
by F. von Hochstetter (‘ Uber das Erdbeben in Peru am 13.
August 1868 und die dadurch veranlassten Fluthwellen
im Pacifischen Ocean,’ Sitzungsberichte der Kaiserl. —
Akademie der Wissenschaften, Wien 58. Bd., 2. Abth.
1868). From an epitome of this paper given in ‘ Peter-
mann’s Geograph. Mittheil.’ 1869, p. 222, I have drawn
up the following table of the more important results
obtained by F. von Hochstetter.

The wave is assumed to have originated near Arica.

Distance Time Velocity Depth of
sea mniies taken by in feet per ocean in
from Arica wave second feet
ham:

Valdivia . : “ 1,420 5 60 479 7,140
Chatham Islands . 5,520 15° 19 608 11,472
Lyttleton . = - 6,120 £92 7S 533 8,838
Newcastle : : 7,380 22 28 538 9,006 .
Apia (Samoa) . - 5,760 16 ° 2 604 11,346
Rapa : ; - 4,057 Ti aL 611 11,598
Hilo . : , 5,400 14 25 555 9,568
Honolulu . : : 5,580 12 OT 746 17,292

Calculations on the same disturbance are also given by
J. E. Hilgard.!

Assuming the origin of the wave to have been at Arica,
his results are as follows:

1 United States Coast Survey Report, or Am. Jour. Sci. vi. p. 77.

182 EARTHQUAKES.
: Time Nautical
mission hour

é miles ho same
San Diego . - 5 4,030 10255 369
Fort Point - - 4,480 12 56 348
Astoria . - : 5,000 dices) 265
Kodiak . 3 . 6,200 22 00 282
Rapa . : s 4,057 10 54 372
Chatham Islands 4 5,520 ae OM: 368
Hawaii - 5,460 14 10 385
Honolulu . - - 5,580 12 18 454
Samoa 4 - 4 5,760 15 338 368
Lyttelton . - 5 6,120 bo OE 322
Newcastle . 4 2 9,380 22 10 332
. Sydney . - yee EL eG) 23 41 314

|

The. wave of 1877.—Two sets of calculations have
been made upon the wave of 1877 by Dr. E. Geinitz of
Rostock.!

The following table is taken from Dr. Geinitz’s second
paper, in which there are several modifications of his first
results. The origin of the disturbance is assumed to have
been near Iquique.

Ba Z

30 C4 (=H oe |
ee £2 | Bek | Boz
Observation stations é ee ea Se | Sao) ome

£ bo < a a | So

| |
|
| hoa nea.

Taiohac (Marquesa Islands) | 4,086| 8 40 A.M.j 12 15 | 563°8| 1,647
Apia(Samoa) . he eo 740112 0 » | 15 30 | 610-4] 1,930
Hilo (Sandwich Islands) ; 5,526 | 10 24 -,, | 14 0 | G67 O50
Kahuliu 6 . | 5,6281}10 30 ,, | 14 5 | G75-o)eeee
Honolulu 5,712 10 50 ,, | 14 25 | 669-7) 2,319
Wellington (New Zealand) . 5,657| 2 40 P.M.| 18 15 j; 524-2) 1,430
Lyttelton . | 5,641} 248 ,, | 18 23 | 519-8} 1,400
Newcastle (Australia). . | 6,800] 232 ,, | 18 7 | 6sa0) 2a
-| Sydney , - | 6,782} 235 ,, | 18 10 | 631:4] 2,065
Kamieshi (Japan) : - | 8,790} 7 20 ,, | 22 55 | 649-0} 2,182
Hakodate _,, : . | 8,760! 9 25 ,, | 25° 0 | S925 ieee
Kadsusa is ; ies 939) 9 50 ,, | 25 15 | 604:9} 1,895

1 Petermann’s Mittheilungen, 1877, Heft xii. 8. 454, and Wova Acta
der Kst. Leop. Carol. Deutschen Acad. d. Naturforscher, Band xl. No. 9.

DISTURBANCES IN THE OCEAN. 183

The mean depths represent a mean of two sets of
_ calculations, one made with the aid of Airy’s formula, and
_ the other by Scott-Russell’s formula. The result of my
_ own investigation about this disturbance, the origin of
_ which, by several methods of calculation, is shown to have
been beneath the ocean, near 71° 5’ west long., and 21° 22’
south lat., are given on next page.

Dr. Geinitz considers that his calculated depths of
the ocean and those obtained by actual soundings are in
accordance, a result which is diametrically opposed to
that which I have obtained.

This difference between my calculations and those of
Dr. Geinitz, Hochstetter, and others, chiefly rests on the
origin we have assigned for the sea waves. Dr. Geinitz,
for instance, although he says that the origin of the 1877
earthquake was not on the continent but to the west in
the ocean, bases all his calculations on the assumption
that the centrwm was at or near to Iquique, and the
time at which that city was disturbed was the time at
which the waves commenced to spread across the ocean.
This time is 8.25 p.m. At this time, however, it appears
that the waves must have been more than double the
distance between the true origin and Iquique, from
Iquique on their way towards the opposite side of the
Pacific. Introducing this element into the various cal-
culations which have been made respecting the depth of
the Pacific Ocean as derived from observations on earth-
quake waves—which element, insomuch as the waves
appear to have come in to inundate the land some time
after the shock, needs to be introduced—we reduce the |
velocity of transit of the earthquake wave and, conse-
quently, the resultant depths of the ocean.

In Dr. Geinitz’s paper there are also some slight
differences in the times at which the earthquake phe-

02 eh | 26918 GIG BES Re 8S el ah OL OS OFT | ° ° ayepoxey
ST 9 | BEG 679 FP8'8 Ba Es ILE ST OL OS OFT] ° ‘ —- 1YsTeouey
¢¢c0'9 IPP Bgg'g 0 981 S66" 2, “Ol SF ogee ce ° w0yeq4A'T
TS0°9 OVP GPg'g 66. SL |.8e= Le OF CS GL pe f * BOIVyY
OT * IT | 8919 Gh PLg'g Gr 81 1 6e. ke OL O8— Pah |e * 07SUT|T2 AA
169°¢ LGV G19 oF 6S 8 Ol Sa Se oui ae SroneIniey,
OT "43 ZI | GLEO6 99g GLL‘G BOP etal Wel, Gh Ol es AN Utena ie " * eoureg
LEV‘OT | 62g T19‘¢ Spe VAL ell. 1S Ot Cre OS ee 4 nijynyey
i nae of “8 100€| LIZOL | 99 909° 9. EL eo Ge -OF ee IST Bef? o; oo OT
ra GG | ‘IF 790948] L08'6 194 469°9 SO GAL AS tS. (Ol Soe 291 | Ae smnimouory
Se GT 94 OI 7358'S Ogs 826 €g § | 39 OL 6 QS Sl ae : wordeou09
S 000° OL G69 LL |\S9L 9 6 pire bell * osrered[e A
o 0g €96'S 838 809 9. @ | 91 9 6 1 TL |* °* oquimbop
| OT 608° ELS Gop LG 9Ge oe 6 Te. 1h 1G = =S1exeEULG)
3 Gp 10 GT “Ss | 289° 6¢ 801 Sa On lege cies gg OL |° ° seuoqtfop
< * os | 2198'S 69g 08 06 0 | 6I &L 6 ce Oe ees * eltqog
| GS "13 06 | OLL‘E StS 18 CaO) \SlGe el 6 fol OL |? <1) % ~ * onbmby
199‘T 1&3 899 Ol F 16 21 6 Gl- Lb le Oe oene®
UI 6 | I3L°L 86P 8LSF 6G SI |86 @ OT G& Sol |° ‘“ooslouVI A Ug
69 SE 6 |‘MY IL |* 92A8A Jo ULSLIO
"Ul "7 "UL "Ul fep , [o}
(seaport
soqnurut puodes qvor13 Ul pore] cy oul} UvoU
aE j aadets eT uva00 944 -nojeo) seytuL | Aq uoyey Tete ee opnjyisuoT
[eAroquy Usps yet) OME oun JO [VATIIW

184

DISTURBANCES IN THE OCEAN. 185

nomena were observed at various localities. These,
however, are but of minor importance. At the end of
the paper by Dr. Geinitz two interesting tide gauge
records are introduced, one from Sydney and the other
from Newcastle. These appear to show a marked dif-
ference in the periods of the sea waves at these two
places.!

Comparison of velocities of wave transit which
have been actually observed, with velocities which ought
to exist from what we know of the depth of the Pacific
by actual soundings.—From a chart given in ‘ Peter-
mann’s Geograph. Mittheilungen,’ Band xxiii. p. 164,
1877, it is possible to draw approximate sections on lines
in various directions across the bed of the Pacific.

From the origin of the shock to Japan (Kameishi)
the line would be as follows :—

about 7,441 miles . ° - ° 15,000 feet deep

POO Ue? - - “ « 18,000 %
i - - - - 27.000 9
BOM Wika lo va th; wi 9a at). sco, WO 00ma mame
GO a eS a Bh GAO ORR Ee

On account of the Tuscarora and Belkap Deeps this
would be the most irregular line over which the wave
had to travel.
From the origin to New Zealand (Wellington) the
line would be

about 5,274 miles . ‘ e ‘ » 15,000 feet deep.

MO ee a wn ee LOO ee

From the origin to Samoa the line would be

about 5,773 miles . . : . 15,000 feet deep.

From the origin to the Sandwich Islands (Honolulu)
the line would be

1 J, Milne: ‘Peruvian Harthquake of May 9, 1877.’ See Trans. Seis.
Soc. of Japan, vol. ii.

186 EARTHQUAKES.

almost 5,634 miles yj ° ° - 15,000 feet deep -

and 60 ,, . . . - 12,000 rt

By Scott-Russell’s rule, or, what is almost identically
the same, by Airy’s general formula, we can calculate
how long it would take such waves as we have been
speaking about to travel over the different portions of
each of these lines, and by adding these times together
we obtain the time taken to travel across any one line.
I have made these calculations, but as I get in every
case answers which are too small, I think it unnecessary
to give them.

The actual times taken to travel the distances just
referred to were,

To Japan (Kameishi) : . ° . 23 hr. 38 min.
» New Zealand (Wellington). - « D8, 2S ee
» Samoa F 14\5 ) BSiaaes

»» Sandwich Islands (Honolulu) . - df ,,. bda

From San Francisco to Simoda the line is almost
3,567 miles, 3,000 fathoms deep, 840 miles, 2,500 fa-
thoms deep, and 120 miles 1,000 fathoms deep. This
gives an average depth of about 2,854 fathoms. Bache
calculated the depth at 2,500 fathoms. )

If we are to consider that, because the sea wave at
Simoda came in some time after the land shock had
been felt, the origin of this earthquake, instead of being
at Simoda, was some distance out at sea, this calculated
depth would be reduced.

ras
“
2
3
aM
3
iy
% :

CHAPTER X.

' DETERMINATION OF EARTHQUAKE ORIGINS.

Approximate determination of an Origin—Earthquake-hunting in
Japan—Determinations by direction of motion—Direction indicated
by destruction of buildings—Direction determined by rotation—
Cause of rotation—-The use of time observations—Errors in such
observations—Origin determined by the method of straight lines—
The method of circles, the method of hyperbolas, the method of
co-ordinates—Haughton’s method—Difference in time between
sound, earth, and water waves— Method of Seebach.

OnE of the most practical problems which can be sug-
gested to the seismologist is the determination of the
district or districts in any given country from which
earthquake disturbances originate. With a map of a
country before us, shaded with tints of different intensity
to indicate the relative frequency of seismic disturbance
in various districts, we at once see the localities where we
might dwell with the least disturbance, and those we
shou'd seek if we wish to make observational seismology
astudy. Before erecting observatories for the systematic
investigation of earthquakes in a country, it would be
necessary for us, in some way or other, to examine the
proposed country to find out the most suitable district.
The special problem of determining approximately the
origin or origins of a set of earthquakes would be given
tous. Having made this preliminary investigation, the
next point is, by means of observatories so arranged that

188 EARTHQUAKES.

they could always work in conjunction with each other, to
determine the origins more accurately. By knowing the
origin from which a set of shocks spring we know the

general direction in which we may expect the most violent —

disturbances, and we can arrange our seismometers accord-
ingly.

Approximate determination of origins.—In 1880 I
obtained a tolerably fair idea of the distribution of seismic
energy throughout Japan, by compiling the facts obtained
from some hundreds of communications received from
various parts of the country respecting the number of
earthquakes that had been felt.

The communications were replies to letters sent to
various residents in the country and to a large number of
public officers. By taking these records, in conjunction
with the records made by instruments, it was ascertained
that in Japan alone there were certainly 1,200 shocks
felt during the year, that is to say, three or four shocks
per day. ‘The greater number of these shocks were felt
along the eastern coast, commencing at Tokio, in the
south, and going northwards to the end of the main island.
These shocks were seldom felt on the west coast. It
appeared as if the central range of mountains formed a
barrier to their progress. Similarly, ranges of mountains
to the south-west of Tokio prevented the shocks from
travelling southwards. Proceeding in this way the con-
clusion was arrived at that the west coast, the southern
part of Japan, and the islands of Shikoku and Kiushiu,
had*their own local earthquakes.

Earthquake-hunting.—These preliminary enquiries
having shown that the northern part of Japan was a better
district for seismological observations than the southern
half, the next step was to subject the northern half toa
closer analysis. This analysis was commenced by sending

‘a

re eS oe ae

DETERMINATION OF EARTHQUAKE ORIGINS. 189

to all the important towns, from thirty to one hundred
miles distant from Tokio, bundles of postcards. These
were entrusted to the local government offices with a
request that each week one of these cards would be re-
turned to Tokio stating the number of shocks felt. In
this way it was quickly discovered that the majority of
shakings emanated from the north and east, and seldom,
if ever, passed a heavy range of mountains to the south.
The barricade of postcards was then extended farther
northwards, with the result of surrounding the origin of
certain shocks amongst the mountains, whilst «thers were
traced to the sea shore. By systematically pursuing
earthquakes it was seen that many shocks had their origin
beneath the sea—they shook all the places on the north-
east coast, but it was seldom that they crossed through
the mountains, forming the backbone of the island, to
disturb the places on the west coast.

The actual results obtained in three months by this
method of working are shown in the accompanying map,
which embraces the northern half of the main island of
Nipon and part of Yezo. . The shaded portion of the map
indicates the mountainous districts, which are traversed
by ranges varying in height from about 2,000 and 7,000
feet. The dotted lines show the boundaries of the more
important groups of earthquakes which were recorded.

I. is the western boundary of earthquakes, which at
places to the eastward are usually felt somewhat severely.
Some of these have been felt the most severely at or near
Hakodadi, whilst farther south their effects have been
weak. Occasionally the greatest effect has been near to
Kameishi. Sometimes these earthquakes terminate along
the western boundaries of III. or IV., not being able to
pass the high range of mountains which separate the plain
of Musashi from Kofu.

190 EARTHQUAKES.
138 140 Saporhy 144
SK

SS
N \
\ a \\

Fic. 29.—Northern Japan. Mountainous districts shaded
with oblique lines,

DETERMINATION OF EARTHQUAKE ORIGINS, 191

II. is the boundary of a shock confined to the plain

__which surrounds Kofu. These earthquakes are evidently

quite local. Many of the disturbances have evidently
originated beneath the ocean, having come in upon the
land in the direction of the arrows a or B.

III. This line indicates the boundary of a group of
shocks which are often experienced in Tokio. These may
come in the directions p, E, or F. It is probable that
some of them originate to the eastward of Yokohama, on
or near to the opposite peninsula.

IV. V. and VI. The earthquakes bounded by these
lines probably originate in the directions C or D.

VII. The earthquakes bounded by this line probably
come from the direction E.

VIII. This line gives us the boundary of earthquakes
which may come from the direction B.

The above boundaries sometimes do not extend so far
to the westward as they are shown. At other times,
groups like V. and VI. extend farther to the south-west.
These earthquake boundaries, which so clearly show the
effects of high mountains in preventing the extension of
motion, have been drawn up, not from single earthquakes,
but from a large series of earthquakes which have been
plotted upon blank maps, and are now bound together to
form an atlas. To give an idea of the material upon
which I have been working, I may state that between
March 1 and March 10, 1882, I received records of no less
than thirty-four distinct shocks felt in districts between
Hakodate and Tokio, and for each of these it is quite
possible to draw a map. In addition to the boundaries of
disturbances given in the accompanying map, other bound
aries might be drawn for shocks which were more local in
their character. The groups which contained the greatest
number of shocks are III., IV., V., VI., and VII. By

192 EARTHQUAKES.

work of this description it was found that a very im-
portant group of earthquakes might be studied by a line
of stations commencing at Saporo in the north, passing
through Hakodate, down the east coast of the main island,
to Tokio or Yokohama in the south. A further aid to
the study of this group, together with the study of an
important local group, might be effected with the help of
a few additional stations properly distributed on the plain
of Musashi, which surrounds Tokio. With this example
before us it will be recognised that the choice of sites for
a connected set of seismological observatories will often
be more or lessa special problem. If earthquake stations
were to be placed in different directions around Tokio
without preliminary investigation, it is quite possible that
some of them might be so situated that they would seldom
if ever work in conjunction with the remaining observa-
tories, and therefore be of but little value. And this
remark must equally apply to districts in other portions
of the globe. The method is crude, and, so far as actual
earthquake origins are concerned, it only yields results
which are approximate. The crudeness and the want of
absoluteness in the results is, however, more than coun-
terbalanced by the certainty with which we are enabled to
express ourselves with regard to such results as are ob-
tained. Even when working with the best instruments
we have at our command, unless we are employing some
elaborate system, this method of working gives a most
valuable check upon our instrumental records, and enables
us to interpret them with greater confidence.
Determination of earthquake origins from the direc-
tion of motion.—If we assume that an earthquake is pro-
pagated from a centre as a series of waves, in which
normal vibrations are conspicuous, and obtain at two
localities, not in the same straight line with the origin,

Oe ee ees

DETERMINATION OF EARTHQUAKE ORIGINS. 193

and sufficiently far separated from each other, the direc-
tion of movement of these normal motions, by drawing
lines parallel to.these directions through our two stations,
the lines would intersect at a point above the required
origin. If instead of two points we had three, or, better
still, a large number, the results we should obtain ought
to be still more certain. Unfortunately, it seems that
earthquakes seldom originate from a given point, and,
further, normal motions are not always (sufficiently) pro-
minent. Sometimes, as has already been shown in the
chapters on earthquake motion, they may be non-existent.
It is probable, however, that difficulties of this sort are
more usually associated with non-destructive earthquakes.
Mallet regards the destructive effects of an earthquake as
almost solely due to normal motions. If this be true, for
destructive earthquakes, the problem is shorn of many
of its difficulties. In cases where normal vibrations are
not prominent, where we have only transverse vibrations,
motions due to the interference of normal or transverse
motions, or directions of motions due to the topographical
or geological nature through which the disturbance has
passed, the determination of the origin of an earthquake
by observations on the direction in which the ground has
been moving appears to be a problem which is practically
without a solution. We will, therefore, only consider the
determination of the origin of those earthquakes which
have predominating directions in their movements, which
directions we will consider as normal ones. The question
which is, then, before us, is the determination of the direc-
tion of these normal movements. First of all we may
take the evidence of our senses. In exceptional cases
these have given results which closely approximate to the
truth, but in the majority of cases such results are not to
be relied upon, as the inhabitants of a town will, for the

194 EARTHQUAKES.

same shock, give directions corresponding to all points of
the compass. Much, no doubt, depends upon the situa-
tion of the observer, and much, perhaps, upon his tem-
perament. If he is sitting in a room alone, and is accus-
tomed to making observations on an earthquake, on feeling
the earthquake, if he concentrates his attention on the
direction in which he is being moved, his observations
may be of value. If, however, he is not so situated, and
his attention is not thus concentrated, his opinions, unless
the motion has been very decided in its character, are
usually of but little worth.

Direction determined from destruction of buald-
ings.—When an observer first sees a town that has been
partially shattered by an earthquake, all appears to be
_ confusion, and it is difficult to imagine that in such ap-
parent chaos we are able to discover laws. If, however,
we take a general view of this destruction and compare
together similarly built buildings, it is possible to dis-
cover that similar and similarly situated structures have
suffered in a similar manner. By carefully analysing the
destruction we are enabled to infer the direction in which
the destroying forces have acted. It was chiefly by
observing the cracks in buildings, and the direction in
which bodies were overthrown or projected, that Mallet de-
termined the origin of the Neapolitan earthquake. From
the observations given in Chapter VII. it would appear
that, with destructive earthquakes, walls which are trans-
verse to the direction of motion are most likely to be
overturned, whilst, with small earthquakes, these walls are
the least liable to be fractured. j

From a critical examination of the general nature of
the damage done on the buildings of a town, earthquake
observers have shown that the direction of a shock may
often be approximately determined. The direction in

DETERMINATION OF EARTHQUAKE ORIGINS. 195

which a body having a regular form like a prismatic
gravestone or a cylindrical column is overturned some-
times gives the means by which we can determine the
direction from which a movement came.

The rotation of bodies.—It has often been observed
that almost all large earthquakes have caused objects like
tombstones, obelisks, chimneys, &c., to rotate.

One of the most natural and at the same time most
simple explanations is to suppose that during the shock
there had been a twisting, or backward and forward screw-
like motion in the ground. Amongst the Italians and the
Mexicans earthquakes producing an effect like this are
spoken of as ‘vorticosi.’ In the Calabrian earthquake,
not only were bodies like obelisks twisted on their bases,
but straight rows of trees seem to have been left in
interrupted zigzags. These latter phenomena have been
explained upon the assumption of the interference of
direct waves and reflected waves, the consequence of
which being that points in close proximity might be
caused to move in opposite directions. Reflections such
as these would be most likely to occur near to the junction
of strata of different elasticity, and it may be remarked
that it is often near such places that much twisting has
been observed.

Another way in which it is possible for twisting to
have taken place would be by the interference of the
normal and transverse waves which probably always exist
in an earthquake shock, or by the meeting of the parts
of the normal wave itself, one having travelled in a direct
line from the origin, whilst the other, travelling through
variable material, has had its direction changed.

Mallet, however, has shown that the rotation may
have been in many cases brought about without the
supposition of any actual twisting motion of the earth—

196 EARTHQUAKES.

a simple backward and forward motion being quite suffi-
cient. If one block of stone rests upon another, and the
two are shaken backwards and forwards in a straight line,
and if the vertical through the centre of gravity of the
upper block does not coincide with the point where there
is the greatest friction between the blocks, rotation must
take place. If the vertical through the centre of gravity
falls on one side of the centre of friction, the rotation
would be in one direction, whilst, if on the other side, the
rotation would be in the opposite direction. _ %

Although the above explanation is simple, and also in
many cases probably true, it hardly appears sufficient. to
account for all the phenomena which have been observed.

Thus, for instance, if the stones in the Yokohama
cemetery, at the time of the earthquake of 1880, had been
twisted in consequence of the cause suggested by Mallet,
we should most certainly have found that some stones
had turned in one direction whilst others had been twisted
in another. By a careful examination of the rotated
stones, I found that every stone—the stones being in
parallel lines—had revolved in the same direction, namely
in a direction opposite to that of the hands of a watch.

As it would seem highly improbable that the centre of
greatest friction in all these stones of different sizes and
shapes should have been at the same side of their centres
of gravity, an effect like this could only be explained by
the conjoint action of two successive shocks, the direction
of one being transverse to the other.

Although fully recognising the sufficiency of two trans-
verse shocks to produce the effects which have been
observed in Yokohama, I will offer what appears to me to
be the true explanation of this phenomenon: it was first
suggested by my colleague, Mr. Gray, and appears to be
simpler than any with which I am acquainted.

DETERMINATION OF EARTHQUAKE ORIGINS. 197

If any columnar-like object, for example a prism
of which the basal section is represented by a BCD (see
fig. 30), receives ashock atrightangles
to BC, there will be a tendency for
the inertia of the body to cause it
to overturn on the edge Bc. If the
shock were at right angles to DC, the
tendency would be to overturn on the
edge Dc. If the shock were in the
direction of the diagonal ca, the
tendency would be to overturn on the
pointc. Let us, however, now suppose Fig. 30.
the impulse to be in some direction like EG, where G is
the centre of gravity of the body. For simplicity we may
imagine the overturning effect to be an impulse given
through G in an opposite direction—that is, in the direction
GE. This force will tend to tip or make the body bear
heavily on c, and at the same time to whirl round C as
an axis, the direction of turn being in the direction of
the hands of a watch. If, however, the direction of im-
pulse had been E’G, then, although the turning would
still have been round Cc, the direction would have been
opposite to that of the hands of a watch.

To put these statements in another form, imagine
GE’ to be resolved into two components, one of them
along Gc and the other at right angles,ar. Here the
component of the direction Gc tends to make the body
tip on C, whilst the other component along GF causes
revolution. Similarly GE may be resolved into its two

components Gc and GF, the latter being the one tending
to cause revolution.

From this we see that if a body has a rectangular
section, so long as it is acted upon by a shock which is
parallel to its sides or to its diagonals, there ought not to

198 EARTHQUAKES.

be any revolution. If we divide our section A BCD up into
eight divisions by lines through these directions, we shall
see that any shock the direction of which passes through
any of the octants which are shaded will cause a positive
revolution in the body—that is to say, a revolution corre-
sponding in its direction to that of the movements of the
hands of a watch; whilst if its direction passes through
any of the remaining octants the revolution will be nega-
tive, or opposite to that of the hands of a watch. From
the direction in which any given stone has turned, we can
therefore give two sets of limits between one of which the
shock must have come.

Further, it will be observed that the tendency of the
turning is to bring a stone, like the one we are discussing,
broadside on to the shock; therefore, if a stone with a
rectangular cross section has turned sufficiently, the direc-
tion of a shock will be parallel to one of its faces, but if
it has not turned sufficiently it will be more nearly parallel
to its faces in their new position than it was to its faces
when in their original position.

If a stone receives a shock nearly parallel with its

diagonal, on account of its instability it may turn either —

positively or negatively according as the friction on its
base or some irregularity of surface bearing most influence.
Similarly, if a stone receives a shock parallel to one of
its faces, the twisting may be either positive or negative,
but the probability is that it would only turn slightly ;
whereas in the former case, where the shock was nearly
parallel to a diagonal, the turning would probably be great.

Determination of direction from winstruments.—
When speaking about earthquakes it was shown, as the
result of many observations, that the same earthquake in
the space of a few seconds, although it may sometimes
have only one direction of motion, very often has many

—

:

‘
et |
-
ibs
me
beceael
Ha
jr
ae
!
I

DETERMINATION OF EARTHQUAKE ORIGINS. 199

directions of motion. In certain cases, therefore, our

records, if we assume the most permanent motions to be

normal ones, give definite and valuable results. In other

cases it is necessary to carefully analyse the records, com- .
paring those taken at one station with those taken at
another.

One remarkable fact which has been pointed out in
reference to artificial earthquakes produced by exploding

:- charges of gunpowder or dynamite, and also with regard

to certain earthquakes, is that the greatest motion of the
ground is wwards, towards the point from which the
disturbance originated. Should this prove the rule, it
gives a means of determining, not only the direction of
an earthquake, but the side from which it came.
Determination of earthquake origins by time obser-
vations.—The times at which an earthquake was felt at
a number of stations are among the most important
observations which can be made for the determination
of an earthquake origin. The methods of making time
observations, and the difficulties which have to be over-
come, have already been described. When determining
the direction from which a shock has originated, or
determining the origin of the shock by means of time
observations, it has been usual to assume that the velocity
of propagation of the shock has been uniform from the
origin. The errors involved in this assumption appear to
be as follows :— |
1. We know from observations on artificial earth-
quakes that the velocity of propagation is greater between
stations near to the origin of the shock than it is between
more remote stations; and also the velocity of propaga-
tion varies with the initial force which produced the
disturbance. If our points of observation are sufficiently
close together as compared with their distance from the
10

200 EARTHQUAKES.

origin of the disturbance, it is probable that errors of this
description are small and will not make material differences
in the general results.

2. We have reasons for believing that the transit
velocity of an earthquake is dependent on the nature of
the rocks through which it is propagated. Errors which
arise from causes of this description will, however, be
practically eliminated if our observation points are
situated on an area sufficiently large, so that the dis-
tribution of the causes tending to alter the velocity of a
shock balance each other. It must be remarked, that
causes of this description may also produce an alteration
in the direction of our shock. :

Other errors which may sometimes enter into our
results, when determining the origin of shocks by means
of observations on velocities, are the assumptions that the
disturbance has travelled along the surface from the
epicentrum and not in a direct line from the centrum.
Again, it is assumed that the origin is a point, whereas
it may possibly be a cavity or a fissure. Lastly, if we
desire extreme accuracy, we must make due allowance for
the sphericity of the earth and the differences of elevation
of the observing stations.

I. The method of straight lines.—Given a number of
pairs of points Aj, A,, By, By) Cy) C,, &c., at each of which
the shock was felt simultaneously, to determine-the origin.

Theoretically if we bisect the line which oins A, and
A, by a line at right angles to A,, 4,, and similarly bisect
the lines B,, B,, Co, C,, all these bisecting lines a, a, bo, b,,
Co) C5 &e., ought to intersect in a point, which point will
be the epzcentrum or the point above the origin.

This method will fail, first, if A, A, Bo, B,, Cy, C, form a
continuous straight line, or if they form a series of parallel
lines.

DETERMINATION OF EARTHQUAKE ORIGINS. 201

Hopkins gives a method based on a principle similar
to the one which is here employed—namely, given that a
shock arrives simultaneously at three points to determine,
the centre. In this case, the relative positions of the
three points, where the time of arrival was simultaneous,
must be accurately known, and these three points must
not lie in a straight line, or the method will fail. For
practical application the problem must be restricted to the
ease of three points which do not lie nearly in the same
straight line. :

II. The method of circles.—Given the times ¢,, t,, t,
&e., at which a shock arrived at a number of places A), A,,
A,, &c., to determine the position from which.the shock
originated.

Suppose A, to be the place which the shock reached
first, and that it reached 4,, A,, Aj, &c., successively after-
wards.

Let ,—=a

t,—t, =)
i, == lg == Cy Ce

With Aj, A,, 43, &c. as centres, describe circles with
radii proportional to the known qualities a, b, c, &e., and
also a circle which passes through a, and touches these
circles. The centre of the last circle will be the epicen-
trum. The radii proportional to a, 6, c, &. may be
represented by the quantities ax, bx, cx, &c., where x is
the velocity of propagation of the shock.

It will be observed that the times at which the shock
arrived at three places might alone be sufficient. If,
instead of taking the times of arrival of a shock, the
arrival of a sea wave be taken, the result would be a
closer approximate to the absolute truth.

It will be observed that this method is not a direct
one, but is one of trial. If, however, an imaginary case

202 | EARTHQUAKES.

be taken, and three given points of observation, Aj, Aj) Ass
be plotted on a piece of paper, it will be found that it is
not a difficult matter to determine two numbers propor-
tional to a and 6 which will allow you to draw two circles
so that they may betouched by a third circle drawn through
A)» This pro lem has practically been applied in the case
of the arrival of a sea wave at a number of places on
the South American coast, at the time of the earthquake
of May 9, 1877. This is illustrated as follows. The
places which were chosen were MHuanillos, Tocopilla,
Cobija, Iquique, Mejillones.

In the following table the first column gives the times
at which the sea wave arrived at each of these places in
Iquique time; in the second column the difference
between these times and the time at which it reached
Huanillos is given; in the third column the distances
through which a sea wave, propagated at the rate of 350
feet per second, could travel during the intervals noted in
the second column is given.

Time after | Distance at !
arrival at | 350 feet per
Huanillos ; second

| Arrival of sea
wave

m. minutes mites

h.
Huanillos 8 3 0
Tocopilla 8 32 2 3
Cobija . 8 38 8 32
Iquique 8 40 10 40
Mejillones 8 46 16 64

The distances marked in the third column are used as —
radii of the circles drawn round the places to which —
they respectively refer.

The centre of the circle drawn to touch the circles of
the first column, and at the same time to pass through
Huanillos, is marked c. “a

DETERMINATION OF EARTHQUAKE ORIGINS. 203

The position from which the shock originated appears
_ therefore to have occurred very near to a place lying in
Long. 7° 15’ W. and Lat. 21° 22’ S.

73 72 77 70 69 68

Vy, Neanide

is

|Mejiliones

Fig. 31.

g The actual operations which were gone through in
making the accompanying map were as follows. First,
a -the places with which we had to deal were represented on
a map in orthographical projection, the centre of pro-

204 EARTHQUAKES.

jection being near to the centre of the map. This was
done so that the measurements which were made upon
the map might be more correct than those we should
obtain from an ordinary chart where this portion of the
world was not the centre of projection. Next, a number
was taken as equal to the velocity with which the sea wave
had travelled. The first velocity taken was about 400
feet per second—this being about the velocity with which,
theoretically, it must have travelled in an ocean having
a depth equal to that indicated upon the charts—also it
seemed to have travelled at this rate from the various
times of arrival as recorded at places along the coast.
Circles were then drawn round Tocopilla, Cobija, Iquique,
and Mejillones with radii equal to 2, 8,10, and 15, each
multiplied by (60 x 400). It was then seen by tral that
it was impossible to draw a single circle which should
touch four circles and also passthrough Huanillos. These
four circles were, in fact, toolarge. Four new but smaller
circles, which are shown in the map, were next drawn, their
radii being respectively equal to the numbers 2, 8, 10,
and 16, each multiplied by (60 x 350), and it was found
that a circle, with a centre Cc, could be drawn which would
practically touch the four circles, and at the same time
would pass through Huanillos.

Ill. The method of hyperbolas.—The method which I
call that of hyperbolas is only another form of the method
of circles. It is, however, useful in special cases, as, for
instance, where we have the times of arrival of earthquakes
at only two stations. Between Tokio and Yokohama, at
which places I frequently obtain tolerably accurate time
records, the method has been applied on several occasions
with advantage. Inthe preceding example let us suppose
that the only time records which we had were for Huan-
illos and Mejillones, and that the wave was felt at the

.

DETERMINATION OF EARTHQUAKE ORIGINS. 205

latter place sixteen minutes or 960 seconds after it was
experienced at the former. Calling these places H and

-M respectively, round m draw a circle equal to the 960

multiplied by the velocity with which the wave was pro-
pagated. It is then evident that the origin of this dis-
turbance must be the centre of a circle which passes
through H and touches the circle drawn round mM. Join
HM, cutting the circle round Miny. Bisect yHinv. It
is evident that v is one possible origin for the disturbance.
Next, from M, in the direction of H, draw any line MZ P;
join ZH; bisect 2H at right angles by the line OPN.
Because PH=PzZ, it is evident that P is a second possible
origin. Proceeding in this way a series of points lying to
the right and left of v on the curve RV Tmay be found,
and we may therefore say that the origin lies somewhere
in the curve RVT. By increasing or decreasing our
velocity we vary the position of the curve RVT, and, in-
stead of a line on which our origin may be, we obtain a
band. As the assumed velocity increases, the circle round
M becomes larger, and has its limit when it passes through
H, where the two arms of the curve RVT will close to-
gether and form a prolongation of the line MyYH as the
assumed velocity diminishes. The circle round M becomes
smaller unti] it coincides with the point mM. At such a
moment the curve RV T opens out to form a straight line
bisecting MH at right angles. The curve RVT isa hyper-
bola with a vertex v and foci H and mM. Inasmuch as
PM—PH=a constant quantity. If we have the time
given at which the shock or wave arrived at a third
station as at Iquique, itis evident that a second hyper-
bola R’ v’ 1’ might be drawn with Iquique and Huanillos
as foci, and that the mutual intersection of these two
hyperbolas with a third hyperbola, having for its foci
Iquique and Mejillones, would give the origin of the wave.

206 EARTHQUAKES,

The obtaining of a mutual intersection would depend on
the assumed velocity, and the accuracy of the result, like
that of the method of circles, would depend upon the
trials we made. The method here enunciated may he
carried farther by describing hyperboloids instead of
hyperbolas, the mutual intersection of which surfaces
would, in the case of an earth wave, give the actual
origin or centrum rather than the point above the origin
or epicentrum.

IV. The method of co-ordinates.—Given the times at
which a shock arrived at five or more places, the position
of which we have marked upon a map, or chart, to deter-
mine the position on the map of the centre of the shock,
its depth, and the velocity of propagation.

Commencing with the place which was last reached by
the shock, call these places , 15 Po, Pz, and p,, and let ~
the times taken to reach these places from the origin be
respectively t, ¢,, t,, ¢,, and ¢,.

Through p draw rectangular co-ordinates, and with a
scale measure the co-ordinates of p,, p,, Pz, and p,, and
let these respectively be a,, b, 3 G55 by 3 G3, 633 G4, 6,. Then
if x, y, and z be the co-ordinates of the origin of the
shock, d, d,, d,, d,, and d,, the respective distances of
Ps Pi» Pos P39 and p, from this origin, and v the velocity
of the shock, we have
eP+yPrt Pa P= ve
(a, —-av7y? + (6, -y+ 2% =v HC
(a, — 2)? + ( — yt P= ote
(@q,—-a7)? + (,-yP+ v= vt
(q—-2'% + ,-—yP+ Pav

yo ae a Td

Because we know the actual times at which the waves
arrived at the places p, 11, Pos P35 P4, We know the values
t— t,,t— t,, t— t,, i— t,. Call these respectively m, p,
g, and 7. Suppose ¢ known, then

DETERMINATION OF EARTHQUAKE ORIGINS. 207

%Z=t—m
t, =t—p
tZ=t—-—g
%=t—-7.7.

Subtracting equation No. 1 from each of the equations
; 2, 3, 4, and 5, we obtain,

a a2 + 02? — 2a, 2 — Qh, y = v? (2 — &) = v7 (m? — 2m)

a az + BD} — 2a,x% — 2b,y = v* (ty — t?) = v? (p? — 2 p)

a3 + b2 — 2a,x% — 2b,y= v3 -—-YV =v (g — 2¢q)

a, + bf — 2a,e — 2byy = VG — V) = ve? — 2t7r)

iemler 7 — a, and 207 t = w.

Then

2a,2 + 2b,y¥ + um?— wm = a? + 0?
2a,@ + 2b,y + up? —wp = a2 + 6?
¢ 2a,7 + 2b,y +ug? —wq = a2 + 82
a 4. 24,2 + 2b,y + ur? —wr = + bi

goateniae

1
8
pe

= We have here four simple equations containing the
: four unknown quantities x, y, wu, and w. |

x and y determine the origin of the shock. The absolute
velocity v equals / wu. From v and w we obtain ¢t. Sub-
stituting x, y, v, and ¢ in the first equation we obtain z.

We have here assumed that the points of observation
. have all about the same elevation above sea level.

_ ___ If it is thought necessary to take these elevations into
account, a sixth equation may be introduced.

If the propagation of the wave is considered as a hori-
zontal one, as would be done when calculating the position
of the epicentrum or point above the origin, by means of
the times of arrival of a sea wave, the ordinate z of the
first five equations would be omitted. Working in this .
way the resulting four equations, viz.

2a, © + 2b, y + un? — wm? = a? + 02
&e. &e. &e.
remained unchanged.
Applying this method to the same example as that

208 EARTHQUAKES.

used as illustration for the two previous methods, we
obtain for the co-ordinates of Mejillones, Iquique, Cobija,
Tocapilla, and Huanillos, measured in geographical miles,
and the times in Iquique time at which the wave reached
each, as given in the following table; ow and oy being,
drawn through Mejillones.

Co-ordinates Time of arrival
ox OY h. :
Mejillones . 5 a or 0O b or O 8 46p.m
Iquique . é ‘ a, or 150 b, or 96 8 400
Cobija . : : &, or 3 6, or 14 838.23
Tocopilla . : a, or 66 b, or 31 3 FOZ
Huanillos. : a, or 102 b, or 58 8°30,

From this data we find the co-ordinates « and y of
this origin to be 85°8 and 56°7; whilst the velocity of
propagation = 45 feet per second.

Measuring these ordinates upon the map, we obtain a
centre lying very near Long. 71° 5’ W. and Lat. 21°22’
S., a position which is very near to that which has already
been obtained by other methods.

If instead of Huanillos we substitute the ordinates
and time of arrival of the sea wave for Pabalon de Pica,
another point for the origin will be obtained lying farther
out at sea. To obtain the best result, the method to be
taken will evidently be, first to reject those places at
which it seems likely that some mistake has been made
with the time observations, and then with the remaining
places to form as many equations as possible, and from
these to obtain a mean value. This is a long and tedious
process, and as the time observations of this particular
earthquake are probably one and all more or less inaccu-
rate, it is hardly worth while to follow the investigation
farther.

In this example, as in the preceding ones, it will be

Wi BESS

.
i
i

ccm

DETERMINATION OF EARTHQUAKE ORIGINS. 209

observed that it has been sea waves that have been dealt
with, rather than earth vibrations. It is evident, however,
that these latter vibrations may be dealt with in a similar
manner.

In these determinations it will also have been observed
that it is assumed that the disturbance has radiated from
a centre, and, therefore, approached the various stations in
different directions. If we assume that we have three
stations very near to each other as compared with their
distances from the origin, so that we can assume that the
wave fronts at the various stations were parallel, the
determination of the direction in which the wave ad-
vanced appears to be much simplified. The determina-
tion of the direction in which a wave has passed across
three stations was first given by Professor Haughton.

Haughton’s method.—Given, the time of an earth-
quake shock at three places, to determine its horizontal
velocity and coseismal line.

The solution of this is contained in the formula

a(t, —t,) sin p
c(t, —t,) + a(t, —t,) cos 8

When A, B, and C are three stations at which a shock is
observed at the times ¢,, t,, and ¢,; a, 6, and care the
distances between A, B, and C, and @ is the angle made
by the coseismal lines « aw, yB y, and the line a B, which
are assumed to be parallel.

This I applied in the case of the Iquique earthquake,
but owing to the smallness of the angles between the
three stations A, B, and ©, the result was unsatisfactory.
The problem ought to be restricted, first, to places which
are a long distance away from a centre, and, secondly, to
places which are not nearly in a straight line. This pro-
blem may be solved more readily by geometrical methods.

tan o=

210 EARTHQUAKES.

Plot the three stations a, B, and C on a map, join the two
stations between which there was the greatest difference
in the time observation. Let these, for example, be A
andc. Divide the line ac at point D, so that aD : DC as
the interval between the shock felt at a and B is to the
interval between the shock felt at Band c. The line BD
will be parallel to the direction in which the wave advanced.

‘The difference in time of the arrival of two disturb-
ances.—In the various calculations which have been made

to determine an origin based on the assumption of a

known or of a constant velocity, we have only dealt with
a single wave, which may have been a disturbance in the
earth or in the water. A factor which has not yet been
employed in this investigation is the difference in time
between the arrival of two disturbances; one propagated,
for instance, through the earth, and the other, for
example, through the ocean. The difference in the times
‘of the arrival-of two waves of this description is a
quantity which is so often recorded that it is well not to
pass it by unnoticed. ‘To the waves mentioned we might
also add sound waves, which so frequently accompany
destructive earthquakes, and, in some localities, as, for
instance, in Kameishi, in North Japan, are also commonly
associated with earthquakes of but small intensity. It
was by observing the difference in time between the
shaking and the sound in different localities that Signor
Abella was enabled to come to definite conclusions regard-
ing the origin of the disturbances which affected the
province of Neuva Viscoya in the Philippines, in 1881 ;
the places where the interval of time was short, or the
places where the two phenomena were almost simul-
taneous, being, in all probability, nearer to the origin
than when the intervals were comparatively large. I
myself applied the method with considerable success

ef ee he ear SO ye Oe ey eo, ee, Oe ae 5 ee eet ee a ns

i a ee ll Ai i a 2 a

ae

DETERMINATION OF EARTHQUAKE ORIGINS. 211

when seeking for the origin of the Iquique earthquake of

1877. The assumptions made in that particular instance
were, first, that the velocity of the disturbance through
the earth was known, and, secondly, that the velocity
with which a sea wave was propagated was also known.

A method similar to the above was first suggested by
Hopkins. It depended on the differences of velocity with
which normal and transversal waves are propagated.!

Seebach’s method. —To determine the true velocity of
an earthquake, the time of the first shock, and the depth
of the centre.

Let the straight line
M, ™,, M,, Mz represent
the surface of the earth
shaken by an earthquake.
For small earthquakes, to
consider the surface of
the earth as a plane will
not lead to serious errors.
If an earthquake origi-
nates at Cc, then to reach
the surface at M it tra-
verses a distance fA in
the time ¢. To reach the surface at M,, it traverses a
distance h + w, inatimet,. If v equals the velocity of
propagation,

Seebach now says that if we have given the position
of M or epicentrum of the shock, and draw through it
rectangular axes like Mm, and MT,, and lay down on

' Report of British Association, 1847, p. 84.

212 EARTHQUAKES.

M ™, in miles the distances from M of the various stations
which have been shaken, and in equal divisions for minutes
lay down on MT, the differences of time at which M, ™,,
m,, &c. were shaken, then M,T,, M,T,, &c. are the
co-ordinates of points on an hyperbola. The degree of
exactness with which this hyperbola is in any given case
.constructed is a check upon the accuracy of the time
observations and the position of the epicentrwm. The
apex of the hyperbola is the epicentrum.

The intersection of the asymptote with the ordinate
axis is the time point of the first shock, which, because
the scale for time and for space were taken as equal, gives
the absolute position of the centrum. This intersection
is shown by dotted lines. Knowing the position of the
centrum, we can directly read from our diagram how far
the disturbance has been propagated in a given time.

CHAPTER XI.
THE DEPTH OF AN EARTHQUAKE CENTRUM.

The depth of an earthquake centrum—Greatest possible depth of an
earthquake—Form of the focal cavity.

Depth of centrwm.—The first calculations of the depth at
which an earthquake originated were those made by Mallet
for the Neapolitan earthquake of 1857.° These were made
ou the assumption that the earth wave radiated in straight
lines from the origin, and, therefore, at points at different
distances from the epicentrum it had different angles of
emergence. These angles of emergence were chiefly calcu-
lated from the inclination of fissures produced in certain
buildings, which were assumed to be at right angles to the
direction of the normal motion. If we have determined
the epicentrum of an earthquake and the muzoseismal
circle, and make either the assumption that the angle of
emergence in this circle has been 45° or 54° 44’ 9” (see
page 54), it is evidently an easy matter by geometrical
construction to determine the depth of the centrum.
Hofer followed this method when investigating the earth-
quake of Belluno.

Other methods of calculation which have sane employed
are based on time observations, as, for instance, the method ~
of Seebach, the method of co-ordinates, the method of hyper-
boloids or spheres (see pages 200-212).

By means of a number of lines parallel to twenty-six

214 EARTHQUAKES.

angles of emergence, drawn in towards the seismic vertical,
Mallet found that twenty-three of these intersected at a
depth of 73 geographical miles. The maximum depth was
84 geographical miles, and the minimum depth 22 geo-
graphical miles.

The mean depth was taken at a depth of 52 geo-
graphical miles where, within a range of 12,000 feet,
eighteen of the wave paths intersected the seismic ver-
tical.

The point where these wave paths start thickest is at
a depth not greater than three geographical miles, and
this is considered to be the vertical depth of the focal |
cavity itself.

For the Yokohama earthquake of 1880, from ae in~
dications of seismometers, and by other means, certain
angles of emergence were obtained, leading to the conclu-
sion that the depth of origin of that earthquake might be
between 14 and 5 miles.

Possibly, perhaps, the earthquake may have originated
from a fissure the vertical dimensions of which was com-
prised between these depths.

A source of error in a calculation of this description is
that the vertical motions may have been a component of
transverse motions or perhaps due to the slope of surface
waves.

The following table of the depths at which certain
earthquakes have originated has been compiled from the
writings of several observers.

In feet

| Minimum Mean Maximum
Rhineland 1846 (Schmidst) 127,309

Sillien . 1858 (Schmidst) | 86,173
Middle Germany . 1872 (Seebach) 47,225 58,912 | 70,841 —
Herzogenrath .| 1873 (Lasaulx) 16,553 36,516 | 56,477
Neapolitan . . | 1857 (Mallet) 16,705 34,930 | 49,359
Yokohama . .' 1880 (Milne)

7,920 17,260 | 26,400

THE DEPTH OF AN EARTHQUAKE CENTRUM. 215

A table similar to this has heen compiled by Lasaulx.!

With the exception of the determination for the two
last disturbances these calculations have been made with
the assistance of the method of Seebach, which depends,
amongst other things, on the assumptions of exact time
determinations, direct transmission of waves from the
centrum, and a constant velocity of propagation. _

Admitting that our observations of time are practically
accurate, it appears that the other assumptions may often
lead to errors of such magnitude that our results may be
of but little value.

From what has been said respecting the velocity with
which earth disturbances are propagated, it seems that
these velocities may vary between large limits, being
greatest nearest to the origin.

If we refer to Seebach’s method, we shall see that a
condition of this kind would tend to make the differences
in time between various places, as we recede from the
epicentrum, greater than that required for the construc-
tion of the hyperbola. The curve which is obtained
would, in consequence, have branches steeper than that of
the hyperbola, and the resultant depth, obtained by the
intersection of the asymptotes of this curve with the
seismic vertical, indicates an origin which may be much
too great.

Another point worthy of attention, which is common
to the method of Mallet as well as to that of Seebach, is
the question whether the shock radiates directly from
the origin, or is propagated from the origin more or less
vertically to the surface, and then spreads horizontally.
We know that earthquakes, both natural and artificial,
may be propagated as undulations on the surface of the
ground, and that the vertical motion of the latter, as

1 Das Evrdbeben von Herzogenrath, §c., p. 134.

oe.

FEIT OE OEE ae PO ET Cs TN Te OES aye TE EPS RN ee METS ee ieee Oe

>

oe

216 EARTHQUAKES.

testified by the records of well-constructed instruments,
has no practical connection with the depth from which
the disturbance originated.

In cases like these, the direction of cracks in buildings,
and other phenomena usually accredited to a normal
radiation, may in reality be due to changes in inclination
of the surface on which the disturbed objects rested.
When our points of observation are at a distance from the
epicentrum of the disturbance which, as compared with
the depth of the same, is not great, calculations or ob-
servations based on the assumption of a direct radiation
of the disturbance may possibly lead to results which
are tolerably correct. The calculations of Mallet for the
Neapolitan earthquake appear to have been made under
such conditions.

For smaller earthquakes, and for places at a distance
from the seismic vertical of a destructive earthquake, the re-
sults which are deduced from the observations on shattered
buildings, and all observations based upon the assumption
of direct radiation, we must accept with caution.

Another error which may enter into calculations of
this description is one which has been discussed by Mallet
at some length. This is the effect which the form and
the position of the focal cavity may have upon the trans-
mission of waves. |

Should the impulse originate from a point or spherical
cavity, then we might, in a homogeneous medium perhaps,
regard the isoseismals as concentric circles, and expect to
find that equal effects had been produced at equal distances
from the epicentrum. Should, however, this cavity be a
fissure, it is evident that even in a homogeneous medium
the inclination of the plane of such a cavity will have
considerable effect upon the form of the waves which
would radiate from its two walls.

.
"
a
|
;

CS RS eT WL See Te ee

THE DEPTH OF AN EARTHQUAKE CENTRUM. 217

For example, let it be assumed that the first impulse
of an earthquake is due to the sudden formation of a
fissure, rent open from its centre, and that the waves leave
the walls at all points normal to its surface. Then, as
Mallet points out, it is evident that the disturbance will
spread out in ellipsoidal waves, the greatest axis of which
will be perpendicular to the plane of the fissure.

By taking a number of cases of fissures lying in various
directions and drawing the ellipsoidal waves which would
result from an elastic pressure, like that of steam suddenly
admitted into such cavities, the differences in effect
which would be simultaneously produced by these waves
on reaching the surface can be readily understood. The
following example of an investigation on this subject will
serve as an example to illustrate the general nature of the
many other cases which might be taken.

Let a disturbance simultaneously originate from all
points of the fissure f/f. This will spread outwards in
ellipsoidal shells to
the surface of the
earth @e. The
major axis of these
ellipsoidal _ shells
will be the direc-
tion of greatest
effect. In the di-
rection cd_ the
waves will plunge
into the earth, and
places to the right
side of the fissure
will, to use an expression due to Stokes, when speak-
ing of analogous phenomena connected with sound, be
in earthquake shadow. The same expression has been

Pile. oo:

218 EARTHQUAKES.

employed, somewhat differently, when speaking of the
effects produced on buildings.

For places, like s and p, situated at equal distances
from the seismic vertical, it is evident that the intensity
of the shock will be different, and also its time of arrival.
It will also be observed that the isoseismals will take the
form of ovals or distorted ellipses, the larger or fuller end
of which being to the left of the fissure.

Other cases, like those just given, which are dis-
cussed by Mallet in his account of the Neapolitan earth-
quake, are where the fissure forms the division be-
tween materials of different elasticities. In the hard and
more elastic material the waves will be more crowded, the
velocity of a wave particle will be greater, and the transit
will be quicker than in the less elastic medium.

The result is that the distance of equal effect from the
seismic vertical will be greatest in _ the direction of the
more compressible material.

Unless these considerations are kept carefully before
the mind when investigating the depth and, we may add,
the position and form of the centrum of an earthquake,
serious errors may arise.

Greatest depth of an earthquake origin.—A curious
but instructive calculation which Mallet made was a
determination of the greatest possible depth at which an
earthquake may occur. This calculation is based upon
the idea that the impulsive effect of an earthquake has
an intimate relationship with the height of neighbouring
voleanoes, the column of lava supported on a volcanic
cone being a measure of the internal pressure tending to
rupture the adjacent crust of the earth.

Michell, in 1700, virtually propounded this idea, when
he suggested that the velocity of propagation of an earth-
quake was related to the height of such a column.!

: 1 Phil. Trans. vol. li.

THE DEPTH OF AN EARTHQUAKE CENTRUM. 219

Mallet showed that there was probably considerable
truth in such a supposition by appealing to the results of
actual observation. The pressure gauge of the Neapolitan
district would be Vesuvius, the height of which has in
round numbers varied between 3,500 to 4,000 feet. One
of the most destructive earthquakes in this district
namely, the one of 1857—projected bodies with an initial
velocity of about fifteen feet per second. The Riobamba
earthquake, which projected bodies with an initial velocity
of eighty feet per second, appears to have been the most
violent earthquake, so far as its impulsive effort. is con-
cerned, of which we have any record. It occurred
amongst the Andes, where there are volcanoes from 16,000
to 21,000 feet in height.

Comparing these two earthquakes together, we see
that the Riobamba shock had a destructive power 5:33
times that of the Neapolitan shock, and we also see that
the Riobamba volcanoes were about 5:33 times higher
than Vesuvius. The accordance in these quantities is
certainly interesting, and tends to substantiate the idea
that volcanoes are barometrical-like pressure gauges of a
district.

Carrying the argument still further, Mallet says that
if the depth of origin of earthquakes were the same, then
the area of disturbance would, for like formations and
configuration of surface, be a measure of the earthquake
effort, and also some function of the velocity of the wave.
From this we may generally infer ‘that earthquakes, like
that of Lisbon, which have a very great area of sensible
disturbance, have also a very deep seismal focus, and also
the greatest depth of seismal focus within our planet
is probably not greater than that ascertained for this
Neapolitan earthquake, multiplied by the ratio that the
velocity of the Riobamba wave bears to that of its wave,

220 EARTHQUAKES.

or, what is the same thing, by the ratio of the altitudes
of the volcanoes of the Andes to that of Vesuvius.’

Now, as the depth of the Neapolitan shock may be
taken at 34,930 feet, the greatest probable depth of origin
of any earthquake impulse occurring in our planet is
limited to 5°333 x 4,930 feet, or 30°64 geographical miles.

Ingenious as this argument is, we can hardly admit it
without certain qualifications.

First, we are called upon to admit the identity of the
originating cause of the voleano and the earthquake—as
to what may be the originating cause of earthquakes we.
have yet to refer, but certainly in the case of particular
earthquakes, as, for instance, those which occur in countries
like Scotland, Scandinavia, and portions of Siberia, the
direct connection between these phenomena are not at first
sight very apparent.

Secondly, even if we admit the identity of the origin
of these phenomena, it is not difficult to imagine that
the fluid pressure brought to bear upon certain portions
of the crust of the earth may possibly in many instances
be infinitely greater than that indicated by the height
of the column of liquid lava in the throat of a volcano,
the true height of which we are unable to obtain.
Further, in certain instances such a column only appears
to be a measure of the pressure upon the crust of the
earth in the immediate vicinity of the cone. 3

Thus, in the Sandwich Islands, we have lava standing
in the throat of the volcano of Mouna Loa 10,000 feet
higher than it stands in the crater Kilauea, only twenty
miles distant. That these columns should be measures
of the same pressure, originating in a general subterranean
liquid layer with which they are connected, is a supposition
difficult to satisfactorily substantiate.

Another measure of the impulsive efforts which sub-

THE DEPTH OF AN EARTHQUAKE CENTRUM. 221

terranean forces may exert upon the crust above them is
evidently the height to which volcanoes eject materials.
Cotopaxi is said to have hurled a 200-ton block of stone
nine miles. Sir W. Hamilton tells us that in 1779 Vesu-
vius shot up a column of ashes 10,000 feet in height ;
and Judd tells us that this same mountain in 1872 threw
up vapours and rock fragments to the enormous height
of 20,000 feet. This would indicate an initial velocity of
1,131 feet per second.

Notwithstanding Mallet’s calculation that thirty miles
is the limiting depth for the origin of an earthquake, the
origin of the Owen’s Valley earthquake of March 1872
was estimated as being at least fifty miles.!

Form of the focal cavity.— Among the various
problems which are put before those who study the
physies of the interior of our earth it would at first sight
appear that there was none more difficult than the attempt
to determine the form of the cavity, if it be a cavity, from
which an earthquake originates. Almost all investigators
of seismology have recognised that the birthplace of an
earthquake is not a point, and have made suggestions
about its general nature. The ordinary supposition is
that the earthquake originates from a fissure, and if the
focus of a disturbance could be laid bare to us it would
have the appearance of a fault such as we so often see
exposed on the faces of cliffs.

A strong argument, tending to demonstrate that some
of the shakings which are felt in Japan are due to the
production of such fissures, is the fact that the vibrations
which are recorded are transverse to a line joining the
point of observation and the district from which, by time
observations, we know the shock to have originated. The
most probable explanation of this phenomena appears to

1 See Am. Jour. Sci. 1872.

222 EARTHQUAKES,

be that one mass of rock has been sliding across another
mass, giving rise to shearing strains, and producing waves
of distortion.

The first seismologist who attacked the problem of
finding out the dimensions and position of such a fissure
was Mallet, when working on the Neapolitan earthquake
of 1857. The reasons that the origin should, in the first
place, have been a fissure, rather than any other form of
cavity, was that such a supposition seemed to be a priora
the most probable, and, further, that it afforded a better
explanation of the various phenomena which were observed,
than that obtained from any other assumption.

The method on which Mallet worked to determine
the form and position of the assumed fissure, which
method was subsequently more or less closely followed
by other investigators, was as follows :—

From an observation of the various phenomena pro-
duced upon the surface of the disturbed area, a map of
isoseismals was constructed. These were seen, as has
been the case with many earthquakes, not to distribute
themselves in circles round the epicentrum, but as distorted
oval or elliptical figures, the major axes of which roughly
coincided with each other. Further, the epicentrum, did
not lie in the centre of these ovals, but was near to the
narrow end where they converged.

This at once showed, if the reasoning respecting the
manner in which waves are propagated from an inclined
fissure be correct, that the fissure was at right angles to
the major axis of the curves, dipping from their narrow
end downwards, in the direction of their larger wide-
spread ends.

The next weapon which Mallet employed to attack
this problem was the sound which was heard at different
points round about the focus. These sounds appear to have

THE DEPTH OF AN EARTHQUAKE CENTRUM. 223

been of the nature of sudden explosive reports accompanied
by rushing, rolling sounds. The form of the area in which
these sounds were heard was closely similar to that of
the first two isoseismals. Except in the central area of
great disturbance, no sound was heard to accompany the ~
shock.

Those at the northern and southern extremity of the
sound area all described what they heard as a ‘low,
grating, heavy, sighing rush, of twenty to sixty seconds’
duration.’ Those in the middle and towards the east and
west boundaries of this area described a sound of the same
tone, but shorter and more abrupt, and accompanied with
more rumbling.

The nature of the arguments which were followed in
discussing the sound observations will be found in the
chapter relating to these phenomena.

A portion of the argument which it is difficult to
follow relates to the maximum rate at which it can be
supposed possible for a fissure to be rent in rocks, which
rate depends on the density and elasticity of these rocks
and other constant factors.

Next it was observed that the paths of the waves
drawn on the surface, although generally intersecting in
a point, did not do so absolutely, but along a line
passing through the main focus some 7} miles in length.
This, coupled with the observations of sounds, led to the
supposition that the centre of disturbance, considered
horizontally, originated along a curved line passing through ~
the chief focus and the various intersections of the wave
paths.

The last phenomena brought forward to assist in the
solution of this interesting problem were a study of the
tremulous movements that preceded and followed the
shock, and their relation to the sound phenomena.

11

224 EARTHQUAKES.

If the earthquake originated by the formation of a
fissure, after the rending has gone on for a certain time
the focal cavity is enlarged to a certain extent, and the
great shock takes place. This would be followed by con-
cluding tremulous waves. A succession of phenomena
like those accompanied the shock about which Mallet
writes. | :

By observations such as these, coupled with what has
been said about the maximum and mean depths of the
focal cavity, Mallet came to the conclusion that the focal
cavity was a fissure, the rending open of which had
produced the earthquake. The vertical dimensions of
this cavity were not more than 5:3 miles, but were
probably limited to three miles.

From the intersection of the wave paths upon the
surface and the observed emergences, this fissure fol-
lowed horizontally a curve of double flexure, about nine
geographical miles in length. The area of this fissure was
twenty-seven geographical miles. The time of rending it
open in Apennine limestone would be about 74 seconds,
which should be the same as the period during which
tremors were felt. The time actually recorded was six
or eight seconds.

Briefly, this is, then, the line of reasoning which was
followed by Mallet in an investigation the results of
which are as interesting as they are startling. Since the
line of investigation has been opened, and the existence
of new problems has been indicated, other investigators,
although not exactly following Mallet’s method in all
their details, have, when endeavouring to attain the same
ends, employed similar weapons.

Thus, for example, Seebach, when determining the
depth and nature of the origin of the earthquake of
Middle Germany, reasoned somewhat as follows :—

THE DEPTH OF AN EARTHQUAKE CENTRUM. 225

Had the origin been more or less of a spherical
cavity, then the region of most violent disturbance upon
the surface would, according to a theorem we have
already mentioned, have been upon or near a circle of
about 8°8 miles in radius round the epicentrwm. This
region, however, was found by observation to lie along a
eurved band about forty miles in length, altogether on one

side of the epicentrum.

To explain this anomaly Seebach followed Mallet, and
assumed that the origin was not a spherical cavity, but a
fissure.

The depth and strike of this fissure was determined

s by the observation that the area of greatest disturbance

was along a curved line lying radial to the epicentrum.
Such a condition it was assumed indicated that the
fissure of origin must be inclined towards this area of
greatest disturbance. A line was then drawn from this
area to the centrum. A second line at right angles to
this one gave the dip of the fissure.

Hofer, when working on the earthquake of Belluno,
eame to the conclusion that the disturbance originated
from two faults meeting each other at an angle of 60°.
In this determination he was chiefly influenced by the
form of a certain homoseist which was of the form of an
elongated ellipse met on one side by a second ellipse, the
principal.axes of the two ellipses giving the strike of the
two faults.

iS)
i)
=P)

EARTHQUAKES,

CHAPTER XII.
DISTRIBUTION OF EARTHQUAKES. IN SPACE AND TIME.

General distribution of earthquakes—Occurrence along lines—Ex-
amples of distribution—Italian earthquake of 1873—In Tokio—
Extension of earthquake boundaries—Seismic energy in relation to
geological time; to historical time—Relative frequency of earth-
quakes—Synchronism of earthquakes—Secondary earthquakes.

General distribution of earthquakes.—The records of
earthquakes collected by various seismologists lead us —
to the conclusion that at some time or other every
country and every ocean in the world has experienced
seismic disturbances. In some countries earthquakes are
felt. daily, and from what will be said in the chapter on
earth pulsations it is not unlikely that every large earth-
quake might with proper instrumental appliances be
recorded at any point on the land surfaces of our globe.
The area over which any given earthquake extends is
indeterminate. The area over which an earthquake is
sensible is sometimes very great. The Lisbon shock of
1755 is estimated as having been sensible over an area of
3,300 miles long and 2,700 miles wide, but in the form
of tremors and pulsations it may have shaken the whole
globe.

The regions in which earthquakes are frequent are
indicated in the accompanying map, which, to a great
extent, is a reproduction of a map drawn by Mallet. The
regions coloured with the darkest tint are those where

DISTRIBUTION IN SPACE AND TIME. 224

great earthquakes are the most frequent. The actual
number of earthquakes which have been felt in the
differently coloured areas are given, when speaking of the
relation of seismic energy to season.

When looking at this chart it must be remembered
that if we were to make a detailed map of any one of
the different countries where earthquakes are frequent,
we should find in it all the differences that we observe in
the general chart. For instance, one portion of Japan,
where perhaps sixty shocks are felt per year, would be
coloured with a dark tint, whilst other portions of the
same country, where there is only one slight shaking felt
every few years, would be left almost uncoloured. The
black dots indicating the position of volcanic vents are
even more general in their signification than the tinted
areas. Professor Haughton gives for the world a list of
407 volcanoes, 225 of which are active. These numbers
are the same as those given by A. von Humboldt. Of the
active volcanoes 172 are on the margin of the Pacific,
and of the total number eight arein Japan. From my own
observations in Japan independently of the Kurile Islands,
I have enumerated fifty-three volcanoes which are either
active or have been active within a recent period. In a
few years’ time this list will probably be increased. I
mention this fact to show how very imperfect our
knowledge is respecting the number of volcanic vents
existing on our globe. If we were in a position to
indicate the volcanoes which had been in eruption during
the last 4,000 years, the probability is that they would
number several thousands rather than four or five
hundred.

An inspection of the map shows that earthquakes
chiefly occur in volcanic and mountainous regions. The
most earthquake-shaken regions of the world form the

228 EARTHQUAKES.

boundaries of the Pacific ocean. It may be remarked

that these boundaries slope beneath the neighbouring.

ocean at a much steeper angle than the boundaries of
countries where earthquakes occur but seldom. The
coasts of South America, Kamschatka, the Kuriles, Japan,
and the Sandwich Islands, for example, have slopes beneath
the Pacific from one in twenty to one in thirty. The
coasts of Australia, Scandinavia, and the eastern parts of
South America, where earthquakes are practically un-
known, have slopes from one in fifty to one in two
hundred and fifty. Many earthquakes have taken place
in mid-ocean. In the Atlantic Ocean M. Perrey has
given about 140 instances of such occurrences.

The majority of the earthquakes which shake tae
appear to have their origin in the neighbouring ocean.
If we could draw a map of earthquake origins, it is prob-
able that the greater number of the marks indicating
these origins would be found to be suboceanie and along
lines parallel to the shores of continents and islands
which rise steeply from the bed of deep oceans. In
countries like Switzerland and India, our marks would
hold a relationship to the mountains of these countries.!
Looking at the broad features of the globe, we see on its
surface many vast depressions. Some of these saucer-like
hollows form land surfaces, as in central Asia. The
majority of these, however, are occupied by the oceans.
Active volcanoes chiefly occur near the rim of the hollows
which have the steepest slopes. The majority of earth-
quakes probably have their origin on or near the bottom
of these slopes. To these, however, there are exceptions,
as for instance the earthquakes in the Alps, in the hills of

1 David Milne says that ‘out of 110 shocks recorded in England,
thirty-one originated in Wales, thirty-one along the south coast of
England, fourteen on the borders of Yorkshire and Derbyshire, and five
or six in Cumberland.’

DISTRIBUTION IN SPACE AND TIME. 229

Scotland, and the shakings which are occasionally felt in
countries like Egypt. The earthquakes which shake the
borders of the Pacific have their origins in, and their effects
are almost exclusively felt on, the sides of the bounding
ridge facing this ocean. In Japan it is the eastern sides
of the islands which suffer, the western side being almost
as free from these convulsions as England.

Similar remarks may be made about the eastern side
of South America, especially the southern portion of the
continent. At Buenos Ayres, for example, there has been
no disturbance since Mendoza was destroyed, some twenty
years ago. In British Guiana slight shocks are occasion-
ally felt in the low delta which forms the settled portion
of the colony, but they are extremely rare.

Disturbances in lines or zones.—It has often been
observed that disturbances are propagated along the length
of mountains or valleys, and it is but seldom that earth-
quakes cross them transversely. Thus the valleys of the
Rhone, the Rhine, and the Danube are lines along which
disturbances travel.

The major axes of the elliptical areas of disturbances
which have shaken India have a general direction parallel
to the valley of the Ganges along the flanks of the
Himalayas.

The disturbances which have shaken London appear
to have been chiefly east and west, or along the valley of

the Thames. In South America the line of disturbance is

along the western sides of the Andes. Another line is
along the northern coast of the continent through Anda-
lusia and Caraccas towards the Antilles and Trinidad. The
shocks of the Pyrenees are chiefly felt along the southern
side of these mountains. In the middle and on the
northern side they are but seldom felt. This propagation
in lines or zones may in certain cases be apparent rather

230 EARTHQUAKES.

than real. Thus the north and south ranges of mountains
in Japan are mountains almost simultaneously shaken
along their eastern flanks, giving the impression that an
earthquake had originated simultaneously from a fissure
parallel to this line, or else, starting at one end, had run
down their lengths. Time observations have, however,
- shown that such disturbances had their origin at some
distance in the ocean, and, travelling inwards, had reached
all points on the flanks of these mountains almost simul-
taneously. The same explanation will probably hold for the
so-called linear disturbances of western South America.

\l earthquake disturbances have probably a tendency
to radiate from their source, and are only prevented from
doing so by meeting with heavy mountainous districts,
which by their mass and structure absorb the energy com-
municated to them. Much energy is also lost by emerg-
ence on the open flanks of a range of mountains. Rather
than say that high mountains often bound the exten-
sion of an earthquake, or that earthquakes appear to run
along the flanks of such mountains, we might say that
earthquakes have boundaries parallel to the strike of the
rocks in a given district, that such a direction is the one
in which the propagation is the easier.

Rossi is of opinion that volcanic fractures play an
important part in governing the distribution of seismic
disturbances. When a volcano is formed, a series of
starlike fractures are formed round the central crater.
Secondary craters may indicate the line of these fissures.
The mountains about Rome are regarded as typical of this
radial structure. The more distant the secondary craters
are from the centre of the system, the smaller will they
he, and also the younger. If two fissures intersect we
get a larger crater at the junction. Earthquakes are
propagated along the direction of these fissures, whilst the

Ee on er: es:

DISTRIBUTION IN SPACE AND TIME. 231

rising and falling of these lips throw off transverse waves.
Rossi adduces observations which appear to meet with
; explanation on such suppositions.
4 Suess, who has written upon the earthquakes of lower
Austria, shows how the majority of the disturbances have
; had their origin along certain lines which form a break in
7 the continuity of the Alps. One line runs north-east from
Bruck towards Vienna. Near Wiener Neustadt, where the
greatest number and heaviest shocks have occurred, this
line is met by a north-north-west line crossing the Danube
and following the valley of the river Kamp.! Hoeffer has
drawn similar lines from the head of the Adriatic, one set
running north-north-east to intersect near Litschau, and
the other north-north-west to intersect near Frankfort in
the valley of the Rhine.?
Eaanvples of distribution.—A curious example of the
distribution of seismic movement is that of the earthquake

This earthquake appears to have been simultaneously felt
on the Dalmatian coast and in central Italy, in a region
lying north-east from Rome and south-east from Florence.
In both of these areas the motion was from south-east to
north-west. The shock then radiated from the central
oa Italian regions, so that at places on the western shore
_ __ of the Adriatic it was felt after it had been felt on the
Dalmatian coast.

Many explanations might be offered for this peculiar
distribution of seismic activity. Possibly the shock
originated at a great depth beneath the bed of the
southern part of the Adriatic, and by following existing
lines of weakness simultaneously reached the surface of the
earth in central Italy and Dalmatia.

1 BE. Suess, Die Erdbeben Nicderosterrciches.
2 H. Hoeffer, Die Erdbehen Karnten’s.

of March 12, 1873, worked out by Professor P. A. Serpieri.

a ee OE ee te ee

232 : EARTHQUAKES. . _ |

In Tokio, which is built partly on a flat plain, partly
in valleys denuded from a low tableland, and partly on
| the spurs of the tableland itself, the distribution of
| earthquakes is a subject yet requiring attention. Some- —
times it has happened that persons in one house have
been sufficiently alarmed to escape into the open air,

ne figia e
Spoleto ov
Rome® L Ap
- XN
Naples \

a

Earthquake of March, 12th 1873.

(P.A.Serpieri)
Fig. 34.
: W
Areas almost simu'taneously struck from §.E, to N.W. ‘VN
A Me
Subsequent radial disturbance —_>

whilst others, not more than a mile distant, have not been
aware that the city had been shaken.

Extension of earthquake boundaries.—Natural ob-
: structions which may be sufficient to retard small earth-
i quakes may in certain instances not be found sufficient
to retard the larger disturbances. ‘Thus the shocks of

DISTRIBUTION IN SPACE AND TIME. 233

Calabria are usually only felt on the western side of the
Apennines, but instances have occurred when they have
crossed this barrier. In 1801 the earthquake of Cumana
crossed a branch of the coast range.

Sometimes earthquake boundaries give way, and
countries which they sheltered subsequently become ex-
posed to all disturbances. The true explanation of this
is probably in a shifting of the centre of seismic activity.
Thus up to December 14, 1797, although Cumana was
often devastated, the peninsula of Araya was not hurt.
On this date Araya commenced to suffer, and has con-
tinued to suffer ever since.

Fuchs gives an example of the movement of a seismic
centre in the case of the Calabrian earthquake. The first
shock commenced near Oppiedo, the second shock com-
menced four or five miles farther to the north, and the
third shock had its origin five or six miles still farther,
near to Girifalco.

234 EARTHQUAKES,

CHAPTER XIII.

DISTRIBUTION OF EARTHQUAKES IN TIME (continued).

Seismic energy in relation to geological tume.—lf
we admit that seismic energy is only a form of volcanic
energy, it must also be admitted that any cause tending
to produce a general decrease in the amount of the latter
will also produce an alteration in the amount of the
former.

The nebular hypothesis of Laplace tells us that the
solar system is the result of the whirling of a heated
gaseous mass, which as it cooled continually contracted
and consequently whirls the faster. With this hypothesis
before us, we understand why all the planets and their
satellites have a similarity in the directions of their move-
ments, why they revolve nearly in the same plane, in
orbits nearly circular, why some have a flattened figure

-and are surrounded by rings or belts, why the exterior

planets should have a greater velocity of rotation, a
greater number of satellites, and a less density as com-
pared with the interior planets, the similarity of the
elements in meteoric stones, the sun, the stars, and those
found upon our earth, and lastly why there should be an
increase in temperature as we descend into our earth.!
This increase in temperature as we descend into the earth

1 Sia Lectures on Physical Geography, by Rev. 8. Haughton, F.B.S.,
chap. 1.

: fg ta er
» ratat eR Bes. ; ee oe ee ee ne cones ets MA Soc eR ee ee ay Tagen Penis atta A PS met k
Lea ae EE At Be SPP eR Tole SPE. pr i ep apm yen Vola ge ta a: WS Ope Sp ee Was eae be eee eee ee ree ee os =

Se ee ee Ee

k:
:

DISTRIBUTION OF EARTHQUAKES IN TIME. 235

as deduced from many observations appears to be about
1° F. for every fifty or sixty feet of descent.

To explain this and other kindred phenomena it is
assumed that the earth was once very much hotter than
it is at present, and to reach its present stage it has been
gradually cooling. As the laws of cooling are perfectly
known, to calculate how many years it must have taken a
body like our earth to cool down to its present tempera-
ture is a definite problem. Sir William Thomson, start-
ing with the temperature of 7,000° F., when all the rocks
of the earth must have been molten and a skin or crust
upon the surface, such as is so quickly produced upon the
surface of molten lava, finds by calculation that the time
taken to reach the present temperature must have been
about one hundred million years. Into this period he
and other physicists desire to compress the history of all
the stratified deposits. Geologists find this period too
short. Others seeking to reconcile the views of physicists
and geologists endeavour to show that the various agencies
engaged in degrading rocks and accumulating sediments
in former ages are not to be judged of by the agencies
we now see around us; in former times they were more
active. At one period the elastic tides in the earth may
have been so great that they resulted in the fracturing
off from our planet its satellite the moon, and subse-
quently the moon, acting on the waters of the earth, may,
“even as late as 150,000 years ago, have produced every
three hours tides 150 feet in height.

Whatever may be the value of the figures here quoted,
reasonings like these bring us to the conclusions that the
various agencies which we now know to be acting upon
our earth were once far more potent than they are at
present, and if the moon, as a producer of elastic tides,
has any influence upon the occurrence of earthquakes,

236 EARTHQUAKES.

it must have had a much greater influence in bygone
times.

We might speak similarly with regard to the internal
heat of the earth.

From the present heat-gradient of our globe it is pos-
sible to calculate how much heat flows from the earth
every year.

This is equivalent to a quantity which would raise a
layer of water °67 centimetres thick, covering the whole
of our globe, from a temperature of 0° to 100° C.

Similarly, we might calculate the quantity of heat
which would be lost when the average heat gradient,
instead of being 1° F. for fifty feet of descent, was 1° F. for
twenty-five feet of descent.

We might also calculate how many years ago it was
since such a gradient existed.

The general result which we should arrive at would
be that in past ages the loss of heat was more rapid than
it is at present. Now the contraction of a body as it
cools is for low temperatures proportional to its loss of
heat, and this law is also probably true for contraction as
it takes place from high temperatures.

Contraction being more rapid, it is probable that
phenomena like elevations and depressions would be more
rapid than they are at present, and generally all changes
due to plutonic action, as has already been pointed out
by Sir William Thomson, must have been more active.

We have, therefore, every reason to imagine that
earthquakes which belong to the category of phenomena
here referred to were also numerous and occurred on a
grander scale during the earlier stages of the world’s
history than they do at present, and seismic and volcanic
energy, when considered in reference to long periods of
time, is probably a decreasing energy.

Ba eee aed 5 8 ee ee ES oy ee

Ee at ae Soe ae gi eT

DISTRIBUTION OF EARTHQUAKES IN TIME. 258

In making this statement we must not overlook the
fact that in geological time, as testified by the records of
our rocks, volcanic action, and with it probably seismic
action, has been continually shifting, first appearing in
one area and then in another, and even in the same area
we have evidence to show that these have periods of
activity and repose successively succeeding each other.
Thus in Britain, during the Paleozoic times, we have
many evidences of an intense volcanic activity. During
the Mesozoic or Secondary period volcanic energy appears
to have subsided, to wake up with renewed vigour in the

Cainozoic or Tertiary period.

During this latter period it is not at all improbable
that Scotland was in past times as remarkable for its
earthquakes as Japan is at the present day.

Later on it will also be shown that earthquakes are
concomitant phenomena, with those elevatory processes
which we have reason to believe are slowly going on in
certain portions of the earth’s crust. If, therefore, we
are able by the examination of the rocks which constitute
the accessible portions of our globe to determine which
periods were characterised by elevation, we may assume
that such periods were also periods of seismic activity.

Amongst these periods we have those in which various

-mountain ranges appeared. Thus the Grampians, and

the mountains of Scandinavia, were probably produced
before the deposition of the Old Red sandstone. The
Urals were upheaved prior to Permian times. The chief
upheaval in the Alps took place after Eocene times. The
Rigi and other sub-Alpine mountains were formed after
the deposition of the Miocene beds. About this same
time the Himalayas were upheaved.! |

The earthquakes which from time to time shake those

1 Ramsay, ‘ Geological History of Mountain Chains,’ Mining lourna.

RDS enn EE eR

238 EARTHQUAKES.

newer mountains apparently indicate that the process of
mountain-making is hardly ended.

Seismic energy in relation to historical time.—
The distribution of seismic energy with regard to his-
torical time is a subject which has been very carefully
examined by Mallet, who collected together a catalogue
of between six and seven thousand earthquakes, embraced
between the periods B.c. 1606 and a.D. 1850. The earth-
quake of B.c. 1606 was on the occasion of the delivery of
the law at Mount Sinai. Between B.c. 1604 and B.c. 1586
an earthquake probably occurred in Arabia, when Korah,
Dathan, and Abiram were swallowed up. Another biblical
record is that of B.c. 1566, when the walls of Jericho
were overthrown.

The earliest records from China is in B.c. 5953 in
Japan B.C. 285; in India a.p. 894.

By using the number of earthquakes which have been
recorded in each century as ordinates, Mallet constructed
a curve, which apparently shows a continual increase in
seismic energy, especially during recent times. This,
Mallet remarks, contradicts all the analogies of the
physics of the globe, and points out that the rapid increase
in the number of earthquakes in latter years is chiefly
due to the greater number of records which have been
made, and the increase of the area of observation. No
doubt many of the records made by the ancients have
been lost. .

If we compare Mallet’s records, as he invites us to do,
with the great outlines of human progress, we see that
the two increase simultaneously, and we come to the
conclusion that, taken as a whole, during the historical
period the seismic activity of the world has been tolerably
constant.

These conclusions, based on the evidence at our

ie i

DISTRIBUTION OF EARTHQUAKES IN TIME. 239

command, are not to be confuted. If, however, instead
of considering the seismic energy of the whole world, we
consider the seismic energy of particular areas, it seems
reasonable to expect that in certain instances sometimes
a decrease and sometimes an increase in this energy
might be discovered, especially, perhaps, in areas which
are highly volcanic.

In France we know that volcanic activity ceased at a
period closely bordering on historical times, and it is not
unlikely that seismic activity may have ceased at a corre-
sponding time.

In a country like Japan, it is possible that in one
district seismic energy may be on the increase, whilst in
another upon the decrease.

In a country like England, it is probable that the
seismic state is constant, and, whatever changes may be
now occurring, they are taking place at so slow a rate
that, even if our records of the historical period were
complete, we could hardly be expected to find these
changes sufficiently marked to be observable.

For purposes of reference, and also for examining the
present question, the table, page 240, has been compiled.
The earthquakes given are chiefly those which have been
recorded in histories as being more or less destructive.

In the second column of this table will be seen the
number of earthquakes which have occurred in Japan
during each century, the centuries being marked in the
first column. In columns 3 to 18 inclusive are given the
number of earthquakes which have occurred during dif-
ferent centuries in the various countries and districts
mentioned at the head of each column. These latter,
which are taken from the writings of Mallet, are given
for the sake of comparison with the Japanese earthquakes.
If we commence with the seventh century in the column

oO eee ee a sae ae Pe aD Oe EPS DB Or eee ee ee ee Oe ee ee ae ee

Gy 122) O21 091471 |e] 191° FEL -| 98 | O6E | GPL | ELI | 18 | 1is| $8 | OT] ett | 22 | XIX
g |zseior |s |¢s || ss! yer | of | ser} gs | IFT | TL |29c| ge leo | IIT | Te | ‘INLAX
ieee ep eor i) Lon ea S| teti te) Oet | 6c 116 | OT) FH Oe. | Tri
; iy le 1 11 |9 | —1> 2 f olge | Se | ee | Ore PD -\G0t. |S ae ge <
(Site teal Nl eo Uta eS Li | St Gogh le=— aE epaealet 834| 96 | °AX
ee | = a ae Tg | 02 [ileum Slee srs | eg: 61 | “AIX
Ce ee ee ee ee 9% | ST a 1 Be hge oT | STi
(Oe | ee a tie Zo | BI | | Sarita. (ance enn gp
Coie — 1 | of is Gall Ge ae OF ne g(a eae gaoe:| “xt
el || |e gle Nees 2 {—|—| — }zt| x
a Cte ieee = | 5) — 19 Gigi Woe 1G || eee Oral) OCI
S Piles leer ese | et | S| ol T Sj | Pe ee ee LEA
Ei Ce eee = || — | g — |T — |—}|—}|—}—| — }2t| Wa
5 — |—|—;/—|—|—|—| 2 | — {le | —|—]o |—]—|] — |r |r
o — | — | — | —| —|— | — | set — |¢ fae | et ae ee
Ee cen || a ge ee || ee Rd Pee Pm Bc)
= — ;—;/—}|—!—|—|—-| — —;}—]—]—}]—-}—};—-|]—-}] — It J cot
— {—/|—/—}—;-—-|-| —- — |—-} — | —}]—}—]/—!|—-]|] —'{|-| a.
& om ee oy he pre Cae Pas Pew ptt fee: peeee fos i = ae as ee T aE
ep] wl oe EL tel 4 oe = co) i ee bd a)
Bas | g| & H| Bl gee| SS/ BE] Y | we] w| B/E IZE| & e
Tom S| ale 2 S Cars Splat d aces eats | Me: E. =.
eeelrelwele| leelfa/ SPER [eee] e2| 2 | Fa] E/EE| eIEE| ER] =| =
see lealec| &| SIRS ES| EBA | Bee EE] & | wel] e Ee) else) Be |e] &
qo | S| es B@igo|Fs| s8ue|/ SbF) es | F | fa) 8 lee] Ble] as | ry
eAa| «| 2 eaee ees | Peele a 2 eRe Ge) Sele eel B :
Seu M ee Ble sel ee ae ee | care a 2 eel ela, oe
Giese eon | om srt | St | - or Tie) Or 6 Glo pe| sg: leg 3) lee alae 1

240

DISTRIBUTION OF EARTHQUAKES IN TIME. 24]

for Japan, we see that a great increase in the number
of earthquakes, as we come towards the present time, is
not so observable as it is in the other columns.

The explanation for this probably lies in the fact that
Japan has practised civilised arts for a longer period than
many of the European and other countries mentioned in
the table.

In Japan, no doubt, the records of later years have
been more perfect than they were in early times, but this,
although so potent an effacer of what was probably the
true state of natural phenomena in the case of Europe,
has not quite obliterated the truth in Japan; for instead
of an apparent increase of seismic energy since early times
it shows a slight decrease. 3

To draw up a table of earthquakes such as the one
which has just been given, and then, after the inspection
of it, draw conclusions as to whether there has been an
increase or decrease in seisrnic energy, is, however, hardiy
a just method of reasoning. The earthquakes, taken as
they are, for the whole of Japan, represent a collection
of places some of which are 1,000 miles apart. When we
consider that many earthquakes which occurred at one
end of this line were never felt at the other end, in order
to justly estimate the periodicity of seismic phenomena
it would seem that we ought either to take some par-
ticular seismic area or else the whole world.

The particular area which has been taken is that of

_ Kioto in Central Japan, and the earthquakes which have

been felt there are enumerated in the table.

In order to show the variation in seismic activity
of this district a curve has been plotted, fig. 35,
with ordinates equal to the values given for the Kioto
earthquakes during succeeding centuries. The upper
points of these ascending and descending lines are

242 _ EARTHQUAKES.

joined by a free curve. The lower points are similarly
joined. The points of bisection of ordinates drawn
between these two curves
are taken as points in a F
curve to show the true
secular change in seismic |
energy.

By looking at this wavy
> line it will be seen that the

intervals between maxima
= and minima are closer to-
eae cz “gether in early times than
they are later on.

Thus, between the
eighth century and the
ninth century, points of
maximum and minimum
seismic efforts occurred at
times a century apart,
whilst later on, from the
eleventh to the fifteenth
century, they were at in-
tervals of 300 years apart.

By inspecting either —
the wavy line or the re-
sultant curve, it will be
seen that since the ninth
x century down to the pre-

sent time there has been
a decided decrease in seis-
-mic energy. From the
ninth century down to the
fifteenth century this de-

Soh Caf aay ee ae ee sae it Ee Ha eae i es ea aaa rl aie
EN a eee pee Sn SP PaieS Se Pee A ee ee Oe res ve paces 7 AS

XH
Fria. 35.—Curve of Scismic Intensity for Kioto

Ss
\
aE
bes
[aa

Ee / |

Centuries

mae
plot

© B et eu D ih ACN) fv °
crease is represented by a
"fizysuaquy |

DISTRIBUTION OF EARTHQUAKES IN TIME. 243

3 regular curve. At this point, however, the decrease be-
comes slightly more rapid, and is represented by a second
curve. If, instead of calculating ordinates for my curve,
in which intensity has been considered, simply the number
; of earthquakes are counted, a similar result is obtained.
From this it appears that the rate at which seismic
energy decreased during the last 500 years was about
the same as that at which it decreased during the 500
years previous to this period.

If the lists for the Italian and Turco-Hellenie districts
could be similarly analysed, and the earthquakes of any
particular district picked out from the others, it is very
probable that a similar decrease or alteration in seismic
energy might be observed.

Provided that we have at our disposal records of the
various earthquakes which have occurred in any given
district during a sufficiently long period of time, one
conclusion that we may expect to arrive at is that we
shall be able to trace some variation in the seismic
activity of that district. For the Kioto area, it has been
shown that there is a diminution in seismic activity,
In other districts, however, there may possibly be an
increase.!

Relative frequency of earthquakes.—A question which
is of great interest to those who dwell in shaken districts
is as to how often disturbances may be expected to occur.

From a general examination of this question, consider-
ing the earthquakes of the whole world, Mallet arrived at
the following conclusions :—

ee eee ae ee ee ee ee

=

eet ye ee

Pe Og A Oe he eee ae ee, YOR
eg re 4 me 5

1 A notable example of a rapid diminution in the number of earth-
quakes felt at a place is that of Comrie in Scotland. In 1839-40, no
. less than sixty shocks were felt in eleven months. In 1842-43, about
thirty shocks were felt, and in the following year thirty-seven. Since
this time the number of shocks has decreased until they are almost of
as rare occurrence at Comrie as in other portions of the British Isles,

“Fa
oe

.
at!

244 EARTHQUAKES.

1. While the smallest or minimum paroxysmal inter-
vals may be a year or two, the average interval is from
five to ten years of comparative repose.

2. The shorter intervals are in connection with periods
of fewer earthquakes—not always with those of least in-
tensity, but usually so.

3.. The alternations of paroxysm and of repose appear
to follow no absolute law deducible from these curves.

4. Two marked periods of extreme paroxysm are ob-
servable in each century, one greater than the other—
that of greatest number and intensity occurring about
the middle of each century, the other towards the end of
each. |

The form of the curves which Mallet has drawn seem
to indicate that seismic energy came in sudden bursts,
and then subsided, gradually gathering strength for another
exhibition. This is continually seen in the shocks ex-
perienced in various seismic areas—a large shock, or the
maximum of the activity dying out by repeated small
shocks on succeeding days.

Mr. I. Hattori, writing on the large earthquakes of
Japan, remarks that on the average there has been one
large earthquake every ten years. They, however, occur
in groups, as shown in the following table.

No. of shocks Period Interval

A.D. 827-836 10 years
» 880-890 LOi es

» 1040-1043
» 1493-1407
1510-1513
» 1645-1650
», 1662-1664
», 1853-1856

Hoo OPO OD
Ewe oP

Dr. E. Naumann, who has also written on the earth-

5

a

2
|
Vea

DISTRIBUTION OF EARTHQUAKES IN TIME. 245

quakes in Japan, remarks that if periods of seismic
activity do not occur every 490 years, there is a repetition
of the cycle after 980 years, but there is much variability.
A period of 68 years is very marked. On the average,
large earthquakes have occurred every 5°9 years. Fuchs
gives some interesting examples of the repetition of
earthquakes at definite intervals, of which the following
are examples. Sometimes earthquakes appear to have
repeated themselves after 100 years. One remarkable
example of this is that of Lima, on June 17, 1578,
which was repeated on the same day in the year 1678.
In Copiapo it is believed that earthquakes occur every -
twenty-three years, and examples of such repetitions are
found in the years 1773, 1796, and 1819. In Canada,
near to Quebec, earthquakes lasting forty days are said
to occur every twenty-five years. The plateau of Ardebil
is said to be regularly shaken by earthquakes every two
years. |

A. Caldcleugh, writing on the earthquake of Chili, in
1835,' remarks that the Spaniards first had the idea that
a great earthquake occurs every century. Afterwards they
thought the period was every fifty years. As a matter of
fact, however, there were large earthquakes in 1812, at
Caraccas ; in 1818, at Copiapos; in 1822, at Santiago; in
1827, at Bogota ; in 1828, at Lima; in 1829, at Santiago;
and in 1832, at Huasco.

The average period of seismic disturbances in any
country probably depends upon the subterranean volcanic
activity of that country. When the activity is great the
large earthquakes may occur at short intervals; but when
the activity is small, as in England, shocks of moderate
intensity may not be felt more than once or twice per
century. A general idea of the relative frequency of the

* Phil. Trans. vol. i. 1836.

246 EARTHQUAKES.

large earthquakes in various parts of the world may be

easily obtained by an inspection of the table on page 240.

Between the years 1850 and 1857 Kluge found that
in the world there had been 4,620 earthquakes, which is,
upon the average, nearly two per day. This estimate of
the frequency of earthquakes of sufficient intensity to
be recorded without the aid of instruments is, however,
much below the truth. In Japan alone there probably
occurs, as a daily average, a number at least equal to that
which has been just given for the whole world. Boussin-
gault considered that, in the Andes, earthquakes were
occurring every instant of time.!

To state definitely how many earthquakes are felt in
the world on the average every day is, from the data
which we have at our command, an impossibility. Per-
haps there may be ten, perhaps there may be 100. The
question is one which remains to be decided by statistics
which have yet to be compiled.

After a large earthquake, smaller shocks usually occur
at short intervals. At first the succession of disturbances
are separated from each other by perhaps only a few
minutes or hours. Later on, the intensity of these shocks
usually decreases, and the intervals between them become
greater and greater, until, finally, after perhaps a few
months, the seismic activity of the area assumes a qui-
escent state.

The great earthquake which overtook Concepcion on —

February 20, 1835, was followed by a succession of
shocks like those just referred to, there being registered,
between the date of the destructive shock and March 4,
300 smaller disturbances.

During the twenty-four hours succeeding the des-
truction of Lima (October 28, 1746), 200 shocks were

1 Am Jour. of Sci. vol. xxxvii. p. 1.

x i SS ae ae ae eer Saree ae BORG es Le rrae inhi heani or Scuedcen ll Sanaa
Reg a 2s eo i ae Md ac a can Rn ra eo i gy lg a cial fn eee
PPE ere Pee faye SE, eg cia aera Nee Oa gene x oN CP ee a Se el etre eye 5c ee ee Ree =

ee icte
ane ad

DISTRIBUTION OF EARTHQUAKES IN TIME. 247

counted, and up to the 24th of February in the following
year 451 shocks were felt.

At St. Thomas, in 1868, 283 shocks were counted in
nine and a quarter hours.

Similar examples might be taken from the description
of almost all destructive earthquakes of which we have
records. Fora large earthquake to occur, and not to be
accompanied by a train of succeeding earthquakes, is
exceptional. Sometimes we find that a large number of
small earthquakes have occurred without a large one
being felt. Seismic storms of this description have hap-
pened, even in England—for instance, in the year 1750,
which appears to have been a year of earthquakes for
many portions of the globe.

In this year, which is known as the ‘earthquake year,’
shocks were felt in England as follows: On March 14, in

‘Surrey; March 18, in south-west of England; April 2, at

Chester; June 7, at Norwich; August 23, in Lincoln-
shire; September 30, Northamptonshire.

Synchromsm of earthquakes.—One of the first writers
who drew attention to the fact that two shocks of earth-
quakes have been felt simultaneously at distant places
was David Milne, who published a list of these occur-
rences.! ;

In two instances, February and March 1750, shocks
were simultaneously felt in England and Italy. In
September 1833 shocks appear to have been simul-
taneously felt in England and Peru. These and many
other similar examples are discussed by Mallet, who
thinks with Milne that these coincidences are in every
probability matters of accident. According to Fuchs,
Calabria and Sicily appear often to have had earthquakes
at the same time, as for instance in 1169, 1535, 1638,

1 Milne, ‘ British Earthquakes,’ Edin. Phil. Journ. vol. xxXi.
12

248 EARTHQUAKES,

when the town Euphemia sank, and in the years 1770,
1776, 1780, and 1783.

A remarkable example of coincidence occurred on
November 16, 1827, when a terrible earthquake was felt
in Columbia, and at the same time a shock occurred on
the Ochotsk plains, nearly antipodal to each other.

Kluge also gives a large number of instances of
simultaneous earthquakes ; thus, on January 23, 1855, on
the same day that Wellington, New Zealand, so severely
suffered, there was a heavy earthquake in the Sieben-
geberge, and also in North America. To this might be
added the fact that the last destructive earthquake in
Japan occurred within a few days of this time.

Sometimes neighbouring countries where earthquakes
are common are equally remarkable by their utter want
of synchronism. For example, Southern Italy and Syria
are said never to be shaken simultaneously.

Secondary earthquakes.—Although it is possible that
the simultaneous occurrence of earthquakes in distant
regions may sometimes be a matter of chance, it must
also be remarked that the shaking produced by one earth-
quake may be sufficient to cause ground which is in a
critical state to give way, and thus the first disturbance
becomes the originator of a second earthquake. Admit-
ting that an earthquake, as it radiates from its centre,
may act in such a manner, we see that a feeble disturb-
ance might be the ultimate cause in the production of

-a destructive earthquake, just as the disturbance of a

stone upon the face of a scarp might, by its impact
upon other stones, cause many tons of material to be
dislodged.

It is also easy to conceive how the seismic activity of
two districts may be dependent upon each other. Inas-
much as these secondary shocks are direct effects of

‘
re
oe
re
oat
as?
nes
Nel
aa
Jay
sigs
dee
i
<x

DISTRIBUTION OF EARTHQUAKES IN TIME. 249

primary disturbances, they might have been treated in a
previous chapter.

As examples of consequent or secondary earthquakes
Fuchs tells us that when small earthquakes take place in
Constantinople and Asia Minor, earthquakes are felt in
Bukharest, Galazy, and Kronstadt.

The great Lisbon earthquake also appears to have
given rise to several consequent disturbances. One was
in Derbyshire, occurring at 11 a.m. It was sufficiently
violent to cause plaster to fall from the sides of a room
and a chasm to open on the surface of the ground. Some

miners working underground were so alarmed that they

endeavoured to escape to the surface. During twenty
minutes there were three distinct disturbances.

Another shock was felt at Cork.!

Although these disturbances own a consequence of the
Lisbon earthquake they might properly perhaps be at-°
tributed to the pulsations produced by the shock at Lis- |
bon, which spread through England and other countries
without being felt.

The shocks which men felt in New Zealand and New
South Wales in 1868 were probably secondary shocks,
due to the disturbance at Arequipa and other places on
the South American coast.

These so-called secondary earthquakes, although in
many instances they may be due to earth pulsations pro-
duced by earthquake, or to the immediate sensible shaking
of a large earthquake, may perhaps, in certain instances,
be attributed to some widespread disturbance beneath the
crust of the earth. The occurrence of periods where all
earthquake countries suffer, unusual disturbances indicate
the probability of such underground phenomena.

1 Phil. Trans. vol. xlix. pt. i.

250 EARTHQUAKES,

CHAPTER XIV.
DISTRIBUTION OF EARTHQUAKES IN TIME (continued).

The occurrence of earthquakes in relation to the position of the heavenly
bodies — Earthquakes and the moon—Earthquakes and the sun; and
the seasons; the months—Planets and meteors—Hours at which
earthquakes are frequent—EHarthquakes and sun spots—Earthquakes
and the aurora.

The position of the heavenly bodies and the oc-
currence of earthquakes.—Since the earliest times, in
searching for the cause of various natural phenomena,
man has turned his energies towards the heavens. One
of the earliest observations was the connection that exists
between the season of the year and the motions of the
heavenly bodies. ‘Tides were seen to be influenced by the
moou. In later times it has been discovered that periods
of maximum magnetic disturbances occur every ten or
eleven years with the sun spots, and Herr Kreil, of Vienna,
tells us our satellite, the moon, has also an influence
upon the magnet.

From day to day we see the bond connecting our
planet with the sun, the moon, and other heavenly bodies
which are outside us gradually becoming closer.

Inasmuch as many phenomena, like the motion of the
tides, the rise and fall of the barometer, fluctuations in
temperature, are all more or less directly connected with
the relative position of our planet with regard to the sun

af
;
5
a
a4
~
me
6
;
ny
z
F
4
rs
a

DISTRIBUTION OF EARTHQUAKES IN TIME. 251

and moon, any coincidence between the phases of these
bodies and the occurrence of earthquakes more or less
involves a time relationship with the other phenomena
resultant on lunar and solar influences.

Earthquakes and the position of the moon.—Many
earthquake investigators have attempted to show the
counection between earthquakes and the phases of the
moon.

The first and most successful worker in this branch of
seismology was Professor Alexis Perrey, of Dijon, who, after
many years of arduous labour in tabulating and examining
catalogues of earthquakes, showed that earthquakes were
more likely to occur at the following periods than at
others.

1. They are more frequent at new or full moon (syzy-
gies) than at half moon (quadratures).

2. They are more frequent when the moon is nearest
the earth (perigee) than when she is farthest off (apo-
gee).

3. They are more frequent when the moon is on the
meridian than when she is on the horizon.

These results were obtained by Perrey after analysing
his catalogues by three different and independent methods,
and they were confirmed by the report of a committee
appointed by the Academy of Sciences. It must, how-
ever, be remarked that in several instances anomalies
occur, and also that the difference between the number of
earthquakes at any two periods is not a very large one.
Thus, for instance, the annual catalogues compiled by
Perrey from 1844 to 1847, the earthquakes in perigee are
to those in apogee as 47 : 39. Between the years 1843
and 1872 Perrey finds that 3,290 shocks occurred at the
moon’s perigee, and 3,015 at the apogee.!

1 Compte Rendus, 1875, p. 690.

252 EARTHQUAKES.

Between 1761 and 1800 earthquakes occurred as
follows :—

iim! Perigee yy 9%. ‘ ° ° - 526
Apogee . ° : : - 465

The following table shows the results which enabled
Perrey to deduce his first law.

Dividing the period of lunation into quarters, with
the time of syzygies and quadratures as the centres of these
quarters, he found that the earthquakes were distributed
as follows.

Difference in

Totals Syzygies Quadratures favour of the
Syzygies
1843-18417 1,604 850°48 753°52 69:96
1848-1852 2,049 1,053°53 995-47 58°06
1853-1857 3,018 1,534°13 1,483:°87 50°26
1858-1862 3,140 1,602'99 1,5387°41 65:98
1863-1867 2,845 1,463°42 1,381°58 81°84
1868-1872 4,593 2,333°48 2,259°52 73°96

1843-1872 Tre 249 8,838°03 8,410°97 427-06

The reported earthquakes between 1751 and 1843 are
shown to conform with the same rule.! Julius Schmidt,
astronomer at Athens, found for the earthquakes of
Eastern Europe and adjacent countries for the years 1776
to 1873 that there were more earthquakes when the moon
was in perigee. Other maxima were at new moon, and
two days after the first quarter. There was a diminution
at full moon, and a minimum on the day of the last
quarter. As one example of results which are antagonistic
to the general results obtained by Perrey may be quoted
the results of an examination by Professor W. 8. Chaplin
of the earthquake recorded at the meteorological observa-
tory in Tokio. The list of earthquakes, 143 in number,
extending over a period of three years, was recorded by one
of Palmieri’s instruments. The results were as follows :—

1 Am. Jour. Sci. vol. xi. p. 233.

DISTRIBUTION OF EARTHQUAKES IN TIME. 253

1. There have been maxima of earthquakes when the
moon was two and nine hours east and seven hours west.
At the upper transit there is a minimum.

2. Considering the moon’s position with regard to the
sun, at conjunction there were 32, at opposition 37, and
at quadrature 74. East of the meridian the maximum
was at least four hours.

3. When the moon was north of the equator these
were 68, when south 82. }

4. A maximum of earthquakes seven and eleven days
after the moon’s perigee. The fact that these results were
obtained for the earthquakes of a special small seismic
area renders them more interesting.!

Frequency of earthquakes an relation to the position
of the sun.—The question as to whether there is a con-
nection between the frequency of earthquakes and the
relative position of the sun is to a great extent identical
with the question as to the relative frequency of earth-
quakes in the various seasons. It is a subject which we
find referred to by writers in the earliest ages. Pliny
and Aristotle thought that earthquakes occurred chiefly
in spring and autumn. In later times it has been a subject
which has been most carefully considered by Merian, von
Hoff, Perrey, Mallet, Volger, Kluge, and others who have
devoted attention to seismology. In a résumé of the
earthquakes of Europe, and of the adjacent parts of Asia
and Africa, from A.D. 306-1843, Mallet gives the following
results :—

For Nineteenth Century For the whele period
Winter Solstice . 177) Solstices 253) Solstices
Spring Equinox . 151 306 170 403
Summer Solstice . 129 Equinoxes 150 j Equinoxes
Autumnal Equinox 164 315 159 329

1 Transactions of the Asiatic Society of Japan, vol. vi. pt. i. p. 353,

254 EARTHQUAKES.

The above periods were called by Perrey critical epochs,
because as a general result of his researches be found that
at such periods there was a greater frequency of earth-
quakes. Fuchs, quoting from Kluge’s tables, extending
from 1850-1857, tells us that the recorded earthquakes
occurred as follows :—

In the Northern hein es

Equinoxes ° : . . 1324

Solstices . : : : . 1202
In the Southern Hemephee

Equinoxes Sie Le “ ° . 301

Solstices . : - . “261

Earthquakes are, heerclaces more frequent-at the equi-
noxes, and this especially at the autumnal equinox. In
the northern hemisphere, at the solstices, the greater
number of shocks occur about the winter solstices, whilst
in the southern hemisphere, about the summer solstices.

Exceptions, however, are found in Central America
and the West Indies, in the Caucasus, and ae Aigean
Sea.

The idea that earthquakes had a periodicity dependent
upon the position of the heavenly bodies is by no means
confined to Europe. Ina Japanese work called ‘ Jishin
Setsu’ (an opinion about earthquakes) by a priest called
Tensho, it is stated that the relative positions and move-
ments of the twenty-eight constellations with respect to
the moon cause earthquakes. This Tensho asserts after
careful calculation, and Falb tells us that all future earth-
quakes can be predicted.

In the Kuriles and Kamschatka, Sicily, and in parts of
South America, it is said that the equinoxes are regarded
as dangerous seasons.

Frequency of earthquakes in relation to the seasons
and months.—What is here said respecting the relative

Or See ee ees

ae i%
&

DISTRIBUTION OF EARTHQUAKES IN TIME. 255

frequency of earthquakes at the different seasons and
months is little more than an extension and critical ex-

- amination of the results which have been given respect-

ing the frequency of earthquakes in regard to the posi-
tion of the sun.

That there is a difference between the number of
earthquakes which are felt at one season of the year as
tompared with those felt at another is a fact which, as

-seismoscopic observations are extended, is becoming more

and more recognised.

Some of the more important results which were
arrived at by Mallet from 5,879 observations made in the
northern hemisphere, and 223 in the southern hemisphere,
may be expressed as follows :—

Maxima Minima

Northern Hemisphere . | January, alsoaslight| May, June, and July
rise in August and

October
Southern Hemisphere . | November, also May | March, extending
and June over one month,

also August .

Julius Schmidt, of Athens, who so carefully examined
the earthquakes of eastern Europe, came to the following
conclusions :—

For the earthquakes between 1200 and 1873, a -
maximum on September 26 and January 17; a
minimum on December 3 and June 13.

For the earthquakes between 1873 and 1874, a
maximum on March 1 and October 1; a minimum on
July 7 and December 15.

For all the earthquakes of eastern Europe, a maximum
on January 3; a minimum on July 8, or there was a
maximum at perihelion and aphelion.

a an ;

256 EARTHQUAKES.

When the months are grouped together according to
the seasons, spring, summer, autumn, and winter, we
find that in the northern hemisphere the minimum is
in summer and the maximum in winter, whilst in the
southern hemisphere (giving the proper months corre-
sponding to its seasons) we find two maxima, one at the
commencement of winter, and the other at midsummer,
whilst the minima are in spring and autumn.

223 Observations

aN Northern Yo
5879 Observations

Fic. 36.—Curves of Monthly Seismic Intensity (Mallet).

In the following table the difference in the number of
earthquakes felt at different seasons is given more in
detail.

In examining this table, we must remember that for
countries like Peru, Chili, and New Zealand, lying in the
southern hemisphere, the records given for the months
April to September correspond to the winter months of

aS edly 34 ae

DISTRIBUTION OF EARTHQUAKES IN TIME. Deke

those countries. The Roman numerals indicate the
centuries between which the records date.

to to

October April
March | September

( 1. Scandinavia and Iceland, xii-xix . “129 91
2. British and Northern Isles, xi-xix . | 123 94
| 3. Belgium, France, and Holland,iv—xix | 395 272
4, Rhone Basin, Vie be 5 115 69
5. Switzerland and Rhine Basin, ix_xix 327 205
| 6. Danube Basin, v—xix : : . | 147 128
7. Spanish Peninsula, xi_xiv i 114 87
8. Italy, Sicily, Sardinia, and Malta,
Northern | 4 RV AKIN ys 650 581
Regions || 9. Turco-Hellenic Territory, Syria,
f£gean Isles, and Levant, iv-xix .| 214 222
| 10. Northern Zone of Asia, xvili_xix : 46 36
11. Japan (Tokio area), 1872-1880
| (small earthquakes) . 213 157
12. Japan B.C. 295-A.D. 1872 (lange
| earthquakes) : . 165 188
13. Algeria and Northern Africa ; : 26 20
14. United States and Canada, xvii_xix 86 48
15. Java, Sumatra, and rie ear
Islands, 1873-4-7-8 . . 194 | 182
Central 16. Mexicoand Central America, xvi-xix 26 26
Regions 1 17. West Indies (Mallet), xvi-xix . =| hs 114
| 18. West Indies, xvi-xix . . .| 296 | 348
1, Cuba, Xvi-xix . ; 28 23
20. Chili, and La Plata Basin, Se ; 89 89
Southern | 21. Peru, Columbia, Basin of Amazons,
Regions XVI—X1X . : . | 506 541
| 22. New Zealand, 1869- 1879 . : 2 (2 166 176

Neglecting those records which show as many earth-
quakes for the winter months as for the summer months,
we see at a glance that generally the greater number of
shocks have happened during the colder seasons. In the
southern hemisphere, so far as the records go, this is not
true. In the northern regions, out of fourteen examples
there are two exceptions. In the central regions there
are two cases where the greatest number of earthquakes
have been recorded in the winter months, and two cases

258 EARTHQUAKES.

where the greatest number have been recorded for the
summer.

Altogether, out of twenty-two examples, there are only ©
six exceptions to the rule. These exceptions altogether
occur among records many of which are ancient, and
are, therefore, more open to error than lists which have
been compiled in modern times.

Because small earthquakes are seldom noticed by
persons out in the open air, it might be expected that
the number of earthquakes observed in warm countries
at one portion of the year would be equal to those
observed in any other season. Such an argument, how-
ever, would hardly apply to most of the records which
are quoted, as they refer to destructive disturbances.

If, however, we take the records made in tropical
countries from the table just given, we see that in such
countries there have been almost as many observations of
earthquakes at one season as at any other.

Another fact which might be adduced against the
rule that the greater number of earthquakes occur during
the winter months would be the comparison of a table of
earthquakes recorded previous to the nineteenth century.
By doing this we see that for certain countries the winter
rule is inverted, and that the greater number of shocks
are felt during ie summer.

Notwithstanding these objections to Perrey’s conclu-
sions, the balance of evidence is in favour of his general
result, and we may conclude that during the colder
portions of the year we may expect more shakings than
during the warmer portions. Comparing the number of
earthquakes of winter and autumn to those of summer and
spring, they are to each other in the proportion of 4 : 3.

A fairer way to examine this question, and to deter-
mine what is probably the present state of seismic
activity in our globe, would be only to consider the earth- _

DISTRIBUTION OF EARTHQUAKES IN TIME, 259

quakes which have taken place in comparatively recent
times, laying especial stress upon those observations
which have been made with the assistance of automatic
instruments, or those which have been collected by
persons interested in these investigations.

For this purpose the following table, showing the dis-
tribution of earthquakes in different countries during the
nineteenth century, has been compiled.

The arrangement is mensual. Where the number of
earthquakes in any month is above the average, the
number is printed in large type; where below the average,

r
aa
.
a
ey
a
Dn
;
ae

é
7 in small type.
§ EARTHQUAKES OF THE NINETEENTH CENTURY, CHIEFLY FROM PERREY.
= \ H = H
“ b ey © o o | od
3 Pees hah! & len) ech Boh gylese ele fae
y 3 = = a SI iS 3 a0 5) S 5 5 | 3 g
ye q 3S < = = ary = = 3) > Sie
+ S o = < a ro) ° © S
7" = 3 Pana
<-> See | Soa Sal ae | ae cee on
_ {Scandinavia and Iceland .| 17; 11! 11 7 7 6 8 8/ 10] 10/] 11 6 ao
_ | British Isles and Northern
Isles . 9 9°10 7 8 6 Ss aD Se ee Etlng
__ | France, Belgium, “Holland. A hn Qi i165 ]/ als? Sy econ AE) Sisley BAL Gist ater
_ |Basinofthe Rhone . 12) 12-8 3 3 2 2 4 6 6; 8] 14! 66
_ |Basin of the Rhine and
Switzerland . ei cme O55 ated Ly al tan US: | Gat CS ie Ge sai P a i Bek |p Sores az
Basin of the Danube . js Fa ies Be IS 9 8|/ 12 S|) 16 |) Ee ia), MS ee10 = a> enies
Spanish Peninsula . 10 Din G 7 4 6; 10 5 9|/ ll; 7 5
Italian Peninsula, Sicily,
Sardinia, and Malta. 44 44 48] 43; 40| 34] 41] 46) 27] 45] 26] 39) 39

Turco-Hellenic Territory,
Syria, Aigean Islands, and

| Levant. 22) 20/210], 10] Je}, 15} (141.22) 14) 7 ieee te
|Northern Zone of Asia; 41 6) 6 4 4 3 5 7 6 A a Ay
_ |1876-1881, Japan (Tokio
area) . 39| 41! 41] 30) 33] 30] 27] 21] 10] 28] $4] 43] 31-4
Japan (large earthquakes) = Sie 3 3 Loss 5 4}; —|— 1 Sia)
Algeriaand North’rn Africa| 5 2' 6 7 3 2 2 5 1/ 4] 8 1 | 3°8
United States and Canada . 4\| 4 3 3 3) ae 4 6 3 2 7 5} 3:8
Java, Sumatra, &c., 1873-4— |
5-7 anad9 ,. 35 30 38 33 221 36 27| 40 24! 35 30 OAD) SL
Mexico and Central America 3 Die D 2 6 2 2 1 1 2 3 | 955
2 DUT GE A rn 9 $19) |) 2:2) 2) ko 2 AG) ID 10) PS 1D) 118
Cuba . eee 3 ot hgh, WA eee 4, 4
Chiliand La Plata . -| 14] 10) 14 8/ 19} 11] 16] 15] 16 Dalian, Si eLS9)
Peru, Columbia, Basins of
Amazons, xvi-xix . -| 92; 83 92] 27.106| 79} 94] 93] 97| 77| 72! 90) 87
New Zealand, 1869-79 sok DHE ers 19 23 PA || = S31 27| 36| 37 21 27 23 | 28°5
Jan. 1850, Dec. 1857
Northern Hemisphere -|/153 162 143 |161] 126; 124] 141 |156/154)171/151/168) 15:0
Bag Hemisphere -| 75, 48 G61] G6) 46] 42} 53| 39] 54] 55) 57) 46! 53
Northern Hemisphere .| 31 36, 31] 29| 33/ 33] 20] 31] 24| 41] 26| 34/ 30
Southern Hemisphere é 2 — 1 1 3 1 Sie ie 3 2 1 1! 16

= LE ns aS

260 EARTHQUAKES.

A glance at this table shows that for most countries in
the northern hemisphere the rule that there are gene-
rally more earthquakes during the winter months—that
is, from October to March—holds good. For countries
which lie comparatively near to the Equator, and also for
those countries in the southern hemisphere, the rule is
not so clear. When examining this table it must be
remembered that it does not enable us to judge of the
relative frequency of earthquakes in different countries,
inasmuch as the periods over which the records were taken
are different in different cases.

To the above table might be added the records of
P. Merian, who examined the earthquakes felt in Basle
up to 1831. Asa result he found that during the winter
months eighty shocks had been felt, whilst during the
summer only forty. Taking the records for the two
hemispheres from 1850-1857, compiled by Kluge,' in the
northern hemisphere we have in the months between
October and March 948 shocks against 862 in the re-
mainder of the year. In the same months in the southern
hemisphere we have for the corresponding periods the
numbers 337 and 300, and thus both hemispheres would
appear to follow the same rule. If, however, we examine
the table we see that the two seasons are not so pro-
nounced for the southern hemisphere as they are for the
northern, and that there may be two or three periods of
maximum disturbance as has been previously indicated.

Earthquakes and the planets and meteors.—Just as
the moon and the sun may exert an attractive influence
upon the earth and cause earthquakes to predominate at
certain seasons rather than at others, several investigators
of seismic phenomena have thought that the planets might
act in a similar manner.

1 Kluge, Veber die Ursachen, &c., p. 74.

cee el oe ee)
= pee = a ¥

DISTRIBUTION OF EARTHQUAKES IN TIME, 261

M. J. Delauney, from a study of Perrey’s tables of
earthquakes from 1750-1842, found two groups of maxima
each with a period of about twelve years, one commencing
in 1759 and the other in 1756. Two other groups with
twenty-eight year periods respectively commence in 1756
and 1773. These groups coincide with the times when
Jupiter and Saturn reach the mean longitudes of 265°
and 135°. From this Delauney concludes that earth-
quakes have a maximum when the planets are in the
mean longitudes just mentioned.

The increased number of earthquakes, especially in
November, are attrituted to the passage of the earth
through swarms of meteors, and in like manner supposes
the influence of Jupiter and Saturn to be due to their
passing through meteor streams situated in mean longi-
tudes 135° and 265°. ,

As a consequence of this he predicts an increase of
earthquakes in the years 1886, 1891, 1898, 1900, &c.!

Dr. E. Naumann, who critically examined the large
earthquakes of Japan, showed that there was an approxi-
mate coincidence between many of the disturbances and
the thirty-three year period of meteoric showers.”

Humboldt states that a great shower of meteors was
seen at Quito before the great earthquake of Riobamba
(Feb. 4, 1797). The earthquakes of 1766 and 1799 at
Cumana are also said to have been accompanied with
meteoric showers. Mallet gives a list of large earth-
quakes which occurred at the times when meteors were
observed.?

The hours at which earthquakes are most frequent.—
From the examination of a catalogue of over 2,000 earth-

1 Am. Jour. Sci. vol. xix. p. 162.
2 Mitth. d. Deutsch. Ges., Aug. 1878.
8 Report to British Association, 1850, p. 74.

262 EARTHQUAKES.

quakes which occurred in various parts of the world
between the years 1850 and 1857, made by Kluge, it is
found that both for the northern and southern hemi-
spheres the observations which were made during the night
generally exceed those which were made during the day.

Number of Earthquakes
Day Night
In the Northern Hemisphere . : : 938 1592
In the Southern Hemisphere , : E 292 357

In the northern hemisphere the greatest number were
observed between 10 P.M. and 12 p.m. (360 shocks), and
the fewest between 12 and 2 P.M. (139 shocks). In the
southern hemisphere, the greatest number were observed
at night between 12 and 1, and the smallest number
between 1 and 2 and 4 and 5 in the afternoon.’ These
distinctions, however, are less distinctly marked as we
approach the Equator. Schmidt found for the earth-
quakes of the Orient between 1774 and 1873, that shocks
had been most frequent about half-past two 4.M., and less
frequent about 1 P.M. With regard to these conclusions,
which have been reached with much labour, we might be
inclined to think that they are partially to be explained
on the supposition that more observations are made during
the night than during the day—the personal experience
of residents in an earthquake country being, that many
earthquakes which occur during the day are passed by
unnoticed, whilst those which occur during the night are
recorded by thousands of observers. Such a view is cer-
tainly confirmed by the instrumental records obtained in
Japan. From 1872 to 1880 inclusive there were 261
shocks recorded, 132 of which occurred between the hours
of 6 P.M. and 6 A.M.

1 Fuchs, Die Vulkanischen Erscheinungen der Erde, p. 424.

DISTRIBUTION OF EARTHQUAKES IN TIME. 263

Earthquakes and sun spots.—Of late years con-
siderable attention has been drawn to a coincidence
between the occurrence of sun spots, magnetic disturb-
ances, rainfall, and other natural phenomena.

These periods of sun spots occur about every eleven
years, and appear to be coincident with the periodical
return of the planet Jupiter. In Japan, Dr. E. Naumann
sought for a coincidence between these periods of sun
spots and earthquakes, but without any marked results.

Schmidt, who carefully compared his lists of earth-
quakes with the appearance of sun spots, came to the
conclusion that there was no marked coincidence. The
occurrence of earthquakes had sometimes synchronised
with sun spots, whilst at other times there had been a
maximum of sun spots and no earthquakes.

M. R. Wolf! apparently considers that earthquakes,
like volcanic eruptions and the appearance of the aurora,
are coincident with sun spots.

Kluge, however, came to the conclusion that when
there are few sun spots, earthquakes, like voleanic
eruptions and magnetic disturbances, have been at a
maximum.

M. A. Poey, who examined a catalogue of the earth-
quakes of Mexicoand the Antilles, extending from 1634 to
1870, shows by a table that earthquakes have come in
groups, first at the maxima and then at the minima period
of sun spots. Out of thirty-eight groups, seventeen being
at the maximum and seventeen at the minimum, the re-
maining four are exceptions to the rule, being between the
maximum and minimum. Phenomena which are depen-
dent upon heat occur with the minima of sun spots, and
those dependent upon cold with the maxima.?

1 Bern. Naturf. Gesellschaft, 1852.
2 Comptes Rendus, 1874, Jan. to June, p. 51.

264 EARTHQUAKES.

Earthquakes and the aurora.—The possible connec-
tion between earthquakes and the aurora is a subject
which has attracted some attention. Boué has especially
made a careful examination of this subject.

He comes to the conclusion that if we compare the
monthly periods of earthquake frequency and the aurora
there is an agreement between the two. Comparing
Perrey’s tables of earthquakes from the fourth to the
nineteenth century, with tables of the aurora, one-third
of both phenomena have occurred, not only in the same
day, but often at the same hour. Between 1834 and
1847, 457 earthquakes are given and 351 notices of the
aurora.

Out of these :—

48 occur on the same day,
5 occur in the same hour,
30 approximate to the same time.

The nearer together that these phenomena have occurred
the stronger have they been.

Professor M. 8. di Rossi brings forward many examples
where there has been a coincidence between the appear-
ance of the aurora and earthquakes. On 139 nights out
of 211 days the aurora was seen in some parts of Italy, and
ninety-three times earthquakes were felt. On forty-six
occasions earthquakes and aurora took place together.?
In considering the probability of a connection existing
between these two phenomena, we must bear in mind
that the aurora is at no great height above the surface

of our earth, and, further, that it can be partially imi- x

tated. The fact that in earthquake countries, like Japan,
the aurora is practically never seen, would indicate that
1 Boué, Parallele der Erdbeben, Nordlichter und Erdmagnetismus, in ~

Sitz. der K. A. d. Wissensch. 1856, vol. iv. p. 395.
2 Meteorologia Endogena, vol. i. p. 107, &e.

Re? PS TP RS BS ee

es ey oe eee Ee SESE Es We te ide oe a gee, eta

DISTRIBUTION OF EARTHQUAKES IN TIME. 265

we can neither regard this imperfectly understood phe-
nomenon either as an effect or cause of earthquakes.
That earthquakes and the appearance of the aurora in
certain countries should not sometimes coincide is an
impossibility.

Dr. Stukeley, who, it must be remembered, attempted
to correlate the phenomena of earthquakes and electricity,
when writing of the disturbances which shook England in
1849 and 1850, says that the weather had been unusually
warm, the aurora borealis frequent and of unusually
bright colours, whilst the whole year was remarkable for
its fire-balls, lightnings, and corruscations.!

The aurora was observed before the commencement of
the Maestricht earthquakes in 17517; whilst at the time
of the shock flashes of light like lightning were observed
in the sky.

Glimmering lights were seen in the sky before the
New England earthquakes (Nov. 18, 1755), and again,
before the disturbances which occurred in the same
region in 1727, peculiar flashes of light were seen.

Preceding the Sicilian earthquake of 1692 strange
lights were seen in the sky. Ignis fatui have also been
observed with earthquakes. At the time of auroral dis-
plays Bertelli has observed microseismical disturbances,
and M.S. di Rossi, who has made similar observations,
thinks that there is an intimate connection between the
aurora and earthquakes; the aurora either occurring in
a period of earthquakes, or else taking the place of earth-
quakes.

) Phil. Trans, vol. \xviii. p. 221. 2 Gent. Mag. vol. xxvii. p. 508.

266 EARTHQUAKES.

CHAPTER XV.

BAROMETRICAL FLUCTUATIONS AND EARTHQUAKES—FLUCTUA-=
TIONS IN TEMPERATURE AND EARTHQUAKES,

Changes in the barometer and earthquakes.—Mallet,
who collected together a number of examples of earth-
quakes which have occurred with a fall of the barometer,
and a number which have happened with a rise, concludes
that there are as many instances of the one as of the
other. At the great earthquake of Calabria, in 1783, the
barometer was very low. The earthquake of the Rhine
(February 23, 1828) was preceded by a gradual fall of the
barometer, which reached its lowest point upon that day.
After the earthquake the barometer again rose. The earth-
quake of February 22, 1880, in Japan, was accompanied
by exactly similar phenomena. Caldcleugh, who observed
the heavy shocks in Chili (February 20, 1835), noticed that
on February 17 and 18 the barometer fell 5/10 inches,
Similar phenomena were observed before the succeeding
smaller shocks. After the shocks the barometer again
rose. Principal Dawson, speaking of the earthquakes of
Canada, observes that some of the shocks have been
accompanied with a low barometer.

P. Merian, who examined the connection between the
Swiss earthquakes and atmospheric pressure, found that
out of twenty-two earthquakes observed in Basle between

7
:
"4
>

BAROMETRICAL FLUCTUATIONS AND EARTHQUAKES. 267

1755 and 1836, thirteen of these were local shocks, of
which eight were accompanied with sudden changes of pres-
sure. Of the remaining nine, which were only felt slightly
in Basle, no change in atmospheric pressure was observed.
Of thirty-six earthquakes which, between 1826 and 1836,
were felt in Switzerland, thirty were chiefly confined to
Switzerland, and ten of these occurred with a low or
falling barometer.

Humboldt is of opinion that earthquakes only occur
with changes in barometric pressure in those countries
where earthquakes are few; and he gives examples where
the regular variations of the barometer have gone on
without interruption at the time of earthquakes.

Frederick Hoffmann, who examined fifty-seven earth-
quakes which occurred at Palermo between 1788 and
1838, came to the following result :-—

The barometer was sinking. ° ° ° in 20 cases
Pe * rising : F - in: Gi 5
55 9 ataminimum . A ¢ Ay, Teed
- ai = Maximum . = ine: Dames
= = undetermined . - : ne Ths

The observations of M. S. di Rossi apparently show
that the earthquakes in Italy chiefly oceur with a baro-
metrical depression and with sudden jumps in atmospheric
pressure.

Schmidt, who examined the earthquakes of the Orient,
which occurred between 1858 and 1873, says that they
were rare with a high barometer, but numerous when the

barometer was low.

From an examination of a table of 396 earthquakes
(May 8, 1875—Dec. 1881) felt in Tokio, furnished to me
by Mr. Arai Ikunosuke, the director of the meteorological
department, I obtained the following results :—

1 Die Vulkanischen Erscheinungen der Erde, p. 419

:
; 7
aa

268 | EARTHQUAKES,

The barometer was rising . ate - in 169 cases
5 oy, atalling (ee 5 5 4 in 154 ,,
Ba » Steady : es in TS %ogs
Ss » below the sAcineilaries mean . in P69Ney
Bi Es above is 4 in 92 eeee

From this it would appear that in Japan at least the
movements of the barometer do not show any marked
connection with the occurrence of earthquakes.

When considering this question we must remember
the marked effects which a lowering of the barometer
produces upon certain volcanoes and solfataras. The
volumes of steam emitted from Stromboli and from some
of the solfataras in Tuscany hold a marked connection
with atmospheric pressure as the quantity of fire damp
given off from coal seams—these being greatest when the
barometer is low. At certain changes of the weather itis
said that the volcano of Vulture, near Melfi, emits noises.
These phenomena at once place volcanic phenomena and
barometrical pressure in direct relationship. i

Changes im temperature.—lf, with an earthquake, it
should happen that there is a change in the height of
the barometer, we should naturally expect that this might
be accompanied with the changes in the temperature,
in the wind, and in other atmospheric phenomena which
are more or less connected with the height of the
barometer.

Many times it has been observed that after an earth-
quake there has been a sudden fall in the temperature.
Such was the case with the Yokohama earthquakes of |
1880.

Cotte endeavours to show that the earthquakes of
Lisbon produced a change upon the temperature of all
Europe. In the year which followed this at
storms were more common than usual.

Kluge has collected together a large number of

BAROMETRICAL FLUCTUATIONS AND EARTHQUAKES. 269

examples when there has been a fall of temperature at
the time of an earthquake.!

At Kiachta, in Siberia, at the time of the earthquake
of December 27, 1856, the thermometer fell from 12° to
25° R. We must, however, remember that there are
many cases known where the thermometer rose.

M. 8. di Rossi remarks that we have the highest
records of temperature in the years richest in earthquakes.
Thus, in 1873, at the time of the earthquakes in Central
and Northern Italy, an abnormal high temperature was
remarked. Japanese writers have remarked upon the
unusual heat which has shaken their countries. The
temperature of subterranean waters have been known to
increase before earthquakes.

1 Petermann’s G'cogr. Mitth. 1858, sec. 246,

270 EARTHQUAKES.

CHAPTER XVI.
RELATION OF SEISMIC TO VOLCANIC PHENOMENA.

Want of synchronism between earthquakes and volcanic eruptions—
Synchronism between earthquakes and volcanic eruptions—Con-
clusion.

Connection between earthquakes and volcanic erup-
tions.—Insomuch as it is a recognised fact that regions
which are characterised by their seismic activity are
chiefly those which are also characterised by the-number
of their volcanoes, it is generally assumed that these two
phenomena have an intimate relation. The residents in
a voleanic country, when seeking for the origin of an
earthquake, invariably turn towards the volcanoes which
surround them. If a neighbouring volcano is in a state
of activity, it is often regarded as a safeguard against
seismic convulsions, in other cases it is looked upon as
being the cause of such disturbances. In certain in-
stances both of these views have apparently been corro-
borated. When we consider that an earthquake and a
voleanic eruption may both be the result of some great
internal convulsion, and that first one and then the other
may take place in the same neighbourhood, it is natural
to expect that when these internal forces have expended
themselves in the production of one of these phenomena,
it is not so likely that they should exhibit themselves in ~
the other. The inhabitants of Sicily and Naples, we are

RELATION OF SEISMIC TO VOLCANIC PHENOMENA. 271

told, regard eruptions of Etna and Vesuvius as safeguards
against earthquakes. A similar belief is to be found in
portions of South America with regard to the volcanoes
for which that country is so celebrated.

From an examination of the records of the large
earthquakes and the volcanic eruptions which have taken
place in Japan during the last 2,000 years, Dr. Naumann
found that there was often an approximate coincidence
between the times of the occurrence of these phenomena,
suggesting the idea that the efforts which had been suffi-
cient to establish the volcano had at the same time been
sufficient to shake the ground.

Of destructive earthquakes which have occurred at
the time of voleanic eruptions, and of examples when
these phenomena have occurred at widely pene: in-
tervals, the records are extremely numerous.

Want of synchronism between earthquakes and
volcanic eruptions.—Many of the great earthquakes of
South America do not appear to have been connected with
volcanic eruptions.

The great earthquakes of the world, like dibae of
Calabria and Lisbon, which took place in regions which
are not voleanic, have not, Fuchs tells us, taken ie in
conjunction with volcanic Subbrarkts

In Japan, as in the Sandwich Islands and in many
other parts of the globe, the small earthquakes which
occur almost daily do not appear to show any marked
connection with volcanic disturbances.

In 1881, during the eruption of Natustake, a volcano
lying about a hundred miles north of Tokio, there was
neither an increase nor a decrease in the earthquakes which
were felt in Tokio. Similar remarks apply to the state of
seismic activity of 1876-77, when Oshima, a volcanic island
about seventy miles to the south of Tokio, was in eruption.

272 EARTHQUAKES.

In the Sandwich Islands Mauna Loa seems to have its
eruptions independently of the disturbances which shake
these islands.!

Synchronism of earthquakes and volcanic erwp-
tions.—Although many examples like the above may be ~
quoted, which apparently show an utter want of connection
between earthquakes and volcanoes, we must not over-
look that class of earthquakes which almost invariably
accompany all great volcanic disturbances. In fact the
sudden explosions which take place at volcanic foci, as, for
instance, at the commencement of an eruption, are enume-
rated as one of the causes which produce earthquakes.
Farthquakeslikethese usually continue until the pressureof
the steam and lava have found for themselves an opening.
As compared with the total number of earthquakes which
are recorded, they form but an insignificant portion.

The direct connection which exists between these
phenomena has, no doubt, done very much to spread
_ the popular belief that all earthquakes may be connected
with voleanic eruptions. As examples where this connec-
tion has existed we might quote from almost all the
volcanic countries in the world.

Thus, Fuchs tells us that on October 6, 1737, almost
the whole of Kamschatka and the Kurile Islands were
disturbed by movements which were. simultaneous with
the outbreak of the great volcano ae of North
Kamschatka.

One of the earliest records of a severe attbigeeeeee and
a voleanic eruption occurring simultaneously is found
in the accounts of the destruction of Herculaneum and
Pompeii. The throwing up of Monte Nuovo in the neigh-
bourhood of Pozzuoli was eer po with a dreadful
earthquake.’

1 Notes on volcanoes of the Hawaiian Islands, W.T. Brigham: sain:
Boston Soc. of Nat. Hist., 1868. 2 Gent. Mag. vol. xxiii., 1753.

RELATION OF SEISMIC TO VOLCANIC PHENOMENA. 273

In 1868 the earthquake of Arequipa was accompanied
by the opening of the volcano Misti, on its north side.
The distance to the volcano is about fourteen miles.

At the time of the eruptions of Kilauea in 1789 the
ground shook and rocked so that persons could not stand.

The first eruption of the volcano Irasu, in Costa Rica
(1783), was accompanied by violent earthquakes.! The
smoke and flames which are said to have issued from the
side of Mount Fojo at the time of the Lisbon earthquake
are regarded by some as having been volcanic. Others
thought that the phenomena, rather than being on the
side of Fojo, which showed no traces of volcanic action,
had taken place in the ocean.

At the time of the great earthquake at Concepcion
(1835), whilst the waves were coming in, two great
submarine eruptions were observed. One, behind the
Isle of Quiriquina, appeared like a column of smoke.
The other, in the bay of San Vicente, appeared to form
a whirlpool. The sea-water became black, and had a
sulphurous smell, there being a vast eruption of gas in
bubbles. Many fish were killed.?

_ With this same earthquake, near to Juan Fernandez,
about one mile from the shore, the sea appeared to boil,
and a high column of smoke was thrown intothe air. At
night flames were seen.

In 1861, when Mendoza was destroyed and 10,000
inhabitants killed, a volcano at the foot of which
Mendoza is bed burst into eruption.

The earthquake of 1822 at Valdivia was accompanied
by eruptions of the neighbouring mountains, which only
lasted a few minutes.

At the time of the Leghorn shocks (January 16-27,
1742) some fishermen observed a part of the sea to rage

_) Jour, Royal Geog. Soe. vol. vi. 2 Ibid. v1. vi.

G7e ~ FARTHQUAKES.

violently, to raise itself to a great height, and then —
landwards.! .

In 1797, when Riswalawk was destroyed, the be
bouring volcanoes were not affected, but Mount Pasto,
120 miles distant, suddenly ceased to throw out its
usual column of water.

On the night of December 10, 1874, a strong shock
was felt in New England, whilst at 4.45 a.M. on
December 11 a shock was felt in the Pic du Midi, in
the Pyrenees. In the middle of December there were
voleanic outbursts in Iceland.

It is possible that these occurrences might be the
results of some widespread disturbance beneath the crust
of the earth, or perhaps even of widely extended earth
pulsations. The probability, however, is that these coin-
cidences are accidental. When we remember that in a
small area like the northern half of Japan alone there
are periods when there are at least two shocks per day on
the average, it is impossible for these coincidences not to
exist. Less frequently coincidences between the larger
disturbances must occur. Over and above these accidental
coincidences, it would appear that in the world’s history
periods have occurred when earthquakes were unusually
frequent, and at such times distant countries have suffered
simultaneously. This approximate coincidence in period,
which has been referred to when speaking of the distri-
bution of destructive earthquakes in historical time, does
not imply an exact synchronism in the single shocks.

Small earthquakes, or, more properly speaking, local
tremblings, are a necessary accompaniment of almost all

volcanic eruptions. Tremors of this description are seldom,
however, felt beyond the crater, or at the most upon the

flanks of the mountain where the eruption is going on.
1 Phil. Trans. vol. xiii. 2 Am. Jour, Sci. vol. x. p. 191.

oe

=

RELATION OF SEISMIC TO VOLCANIC PHENOMENA, 275.

They are due to the explosive action of steam bursting
through the molten lava.

Volcanic erwption succeeding earthquakes.—Some-
times has happened that an earthquake, or a series of
earthquakes, have terminated with the formation of vol-
canic vents, ,

As an example of a volcanic outburst terminating a
seismic disturbance, may be mentioned the appearance
ef a new volcano in the centre of Lake Ilopango, as a
sequel to the shocks which had disturbed that neigh-
bourhood in 1879.! |

_ In 1750 there were continuous shakings lasting over
three months at Manilla. These terminated with an
eruption of a small island in the middle of a neigh-
bouring lake. Three days after the commencement of
this eruption, four other small islands rose in the same
lake?

Antonio d’Ulloa, when speaking of the Andes, remarks
that after a volcanic eruption the shocks cease.?

Conclusion.—Looking at this question generally, in-
somuch as the greatest number of volcanic eruptions
appear, according to Fuchs, to have taken place in summer,
whilst the greatest number of its earthquakes have
apparently taken place in winter, it would seem that
_ the two phenomena are without any direct connection,
unless it be that both are different effects of a common
cause. | |

Regarded in this manner, an earthquake may be looked
upon as an uncompleted effort to establish a voleano. To
use the words of Mallet, ‘The forces of explosion and
impulse are the same in both; they differ only in degree

1 « Earthquakes of San Salvador, December 21-30, 1879.’ Am. Jour.
Sci. vol. xix. p. 415.
2 Gent. Mag. 1757, p. 323. 8 Phil. Trans. vol. li., 1760.

276 EARTHQUAKES.

of energy, or on the varying sorts and degrees of resist-
ance opposed to them.”!

Although we have many examples of earthquakes
having occurred without volcanic eruptions, and, on the
other hand, of volcanic eruptions without earthquakes,
volcanoes may still be regarded as ‘safety-valves of the
earth’s crust,’ which, by giving relief to internal stresses,
guard us against the effects of earthquakes.

That many earthquakes are felt at Copiapo is at-
tributed to the fact that in the neighbouring mountains
there are no volcanic vents.

We must not, however, overrate the protective in-
fluence of volcanoes. In the Sandwich Islands we see
the columns of liquid lava in neighbouring mountains
standing at different heights, indicating a want of sub-
terranean connection between these vents. In conse-
quence of this it would seem that enormous pressures
might be generated in the neighbourhood of one of these
mountains without finding relief at the other. When we
have conditions like these, it would seem that the erup-
tion of a voleano may have little or no influence in pro-
tecting neighbouring districts.

This may possibly be the explanation of the fact that
in 1835 Concepcion was destroyed, notwithstanding there
being an unusual activity in the volcanic vents of the
neighbouring mountains.

1 Mallet, Report to Brit. Ass., 1858, p. 67.

4
F
Bs,
4

~ CHAPTER XVII.
THE CAUSE OF EARTHQUAKES, —

Modern views respecting the cause of earthquakes—Earthquakes due to
faulting—To explosions of steam—To volcanic evisceration—To
chemical degradation—Attractive influence of the heavenly bodies
—The effect of oceanic tides—Variation in atmospheric pressure—

. Fluctuation in temperature—Winds and earthquakes—Rain and
earthquakes—Conclusion.

As the results of modern inquiries respecting the
cause of earthquakes, we see many investigators chiefly
attributing these phenomena to special causes. A few
attribute them to several causes. It seems to us that
they might be attributed to very many causes which often
actinacomplex manner. The primary causes are telluric
heats, solar heat, and variations in gravitating influences.
These may be the principal, and sometimes the imme-
diate, cause of an earthquake. The secondary causes are
those dependent upon the primary causes, such as ex-
pansions and contractions of the earth’s crust, variations
in temperature, barometrical pressure, rain, wind, the
attractive influences of the sun and moon in producing
tides in the ocean or the earth’s crust, variations in the
distribution of stress upon the earth’s surface caused by
processes of degradation, the alterations in the position
of isogeothermal surfaces, &e.

The part which may be played by these various causes

)
:
|
;
|

278 EARTHQUAKES.

in the production of oscillations, pulsations, and tremors
will be referred to.

Earthquakes consequent on fawltiny.—In the chapter
on Earth Oscillations, the causes producing the phenomena
of elevation and depression are briefly indicated.

By the variations in stress accompanying elevations
and depressions, cracks are produced. Inasmuch as com-
pression would crush the rocks constituting the earth’s
crust, we must conclude with Captain Dutton that these
cracks are formed by tension. By elevation, the upper
rigid crust of the earth is stretched, and fissures are pro-
duced. The sudden formation of these fissures or faults
gives rise to earthquakes, and perhaps also to voleanic
vents. That earthquake and volcanic regions are situated
on areas where there is evidence of rapid elevation is
strikingly illustrated round the shores of the Pacific.

Lasaulx considered that the earthquake of Herzogen-
rath was more or less intimately connected with the great
mountain fissure—the Feldbiss—which crosses the coal
region of the Wurm.! The sudden elevation or sinking
of large areas at the time of an earthquake may be a
consequence of these dislocations.

It has already been pointed out that the earthquake
region of Japan is the one where we have evidence of
recent and rapid elevation. That certain earthquakes of
this region may possibly be the result of faulting we have
the evidence of our senses and of our instruments. The
sudden blows and jolts which are sometimes felt are in-
dicative of the sliding of one mass of rock across another.

Should the ground be simply torn asunder, this tearing
would give rise to a series of waves of distortion, vibrating
in directions parallel to the plane of the fissure. Sup-
posing this motion to be propagated to a number of

1 Von Lasaulx, Earthquakes of Herzogenrath.

THE CAUSE OF EARTHQUAKES. 279

surrounding stations, it would be recorded at each of
these as having the same direction. To those situated on
a line forming a continuation of the strike of the fissure,
the vibrations would advance so to speak end on, whilst
to those stations lying in a line perpendicular to the strike
of the fissure, the motion would advance broadside on.

Motions like these latter have been recorded in Tokio,
where earthquakes which from time observations were
known to have come from the faulted and rising region
to the south have been registered as a series of east and
west motions, or vibrations transverse to this line of
propagation.

It must, however, be here mentioned that the registra-
tion of only transverse motion may possibly be due to the
extinction of normal motion, although this is not generally
regarded as probable.

It would therefore appear that certain earthquakes
and faults are closely related phenomena, the former
being an immediate effect of the latter. Faults are due
to earth oscillations, and to a variety of causes producing
disturbances in the equilibrium of the earth’s crust; the
principal cause of all these phenomena being alterations
in the distribution of heat, and the attractive force of
gravity.

Earthquakes consequent on the explosion of steam.—
Humboldt regarded volcanoes and earthquakes as the
results of a common cause, which he formulated as ‘the
reaction of the fiery interior of the earth upon its rigid
crust.’ Certain investigators, who have endeavoured to
reduce Humboldt’s explanation to definite limits, have
suggested that earthquakes may be due to sudden out-
‘bursts of steam beneath the crust of the eazth, and its
final eseape through cracks and fissures.

Admitting that steam may accumulate by separating

280. EARTHQUAKES,

out from the cooling interior of our globe, its sudden
explosion might be brought about by its own expansive
force, or by the movements in the bubbling mass from
which it originated.

Others, however, rather than regard the steam as s being
a primeval constituent of the earth’s interior, imagine it
arises from the gradual percolation of water from the
surface of the earth down to volcanic foci, into which it is
admitted against opposing pressures, by virtue of capillary
action.

Mallet, in his account of the Neapolitan earthquake,
shows that the whole of the observed phenomena can be
accounted for by the admission of steam into a fissure,
which by the expansive force exerted on its walls was
rent open. Just as at the Geysers we hear the thud and
feel the trembling produced by the sudden evolution and
condensation of steam, so may steam by its sudden
evolution and condensation in the ground beneath us
give rise to a series of shocks of varying intensity, accom=
panied by intermediate vibratory motions—that is to say,
a motion which, as judged of by our feelings, is not unlike
many earthquakes. Often it may happen that the result
of the explosion may be the production of a fault, or at
least a fissure; and thus in the resulting movements we
may have a variety of vibrations, some being those of
compression and distortion, produced by the blow of the
explosion, and others being those of distortion alone,
produced by the shearing action which may have taken
place by the opening of the fault. Sometimes one set of
these vibrations may be prominent, and sometimes the
other. Thus, when we say that an earthquake has shown
evidence by the nature of its vibrations that it was pro-
duced by a fault, this by no means precludes the possi-
bility that an explosion of steam may also have been con-

= oe ive warts fife | f+, eee 4 ‘— e “ = nts =. i, ede ind oe sks es a ¥ Sa ee
of wa - 7 a e i - ee i pei ae SE Eee A ee ee ee a te
ee ware ee ae
’ 2 3
:

THE CAUSE OF EARTHQUAKES, 281

nected with the production of the disturbance. Mallet
threw out the suggestion that the opening of fissures
beneath the ocean might admit water to volcanic foci.
During the time that the water was in the spheroidal
state, the preliminary tremors, so common to many earth-
quakes, would be produced. These would be followed by
the explosion, or series of explosions, constituting the
shock or shocks of the earthquakes.

The chief reasons for believing that the earthquakes
of North-Eastern Japan are partly due to explosive efforts
are :—

1. That the greater number of disturbances, perhaps
ninety per cent., originate beneath the sea, where we may
imagine that the ground, under the superincumbent
hydrostatic pressure, is continuously being saturated with
moisture.

2. Many of the diagrams show that the prominent
vibrations, of which there are usually from one to three,
in a given disturbance have the same character as those
produced by an explosive like dynamite, the greatest
and probably the most rapid motions being inwards
towards the origin.

It may here be remarked that a very large proportion
of the destructive earthquakes of the world have originated
beneath the sea, as has often been testified by the
succeeding sea waves. Also, it must be observed, that
earthquake countries, like volcanic countries, are chiefly
those which have a coast line sloping at a steep angle
beneath the sea—that is to say, earthquakes are frequent
along coasts bordered by deep water.

The earthquakes which occur at volcanic foci con-
stitute another class of disturbances which may be ac-
credited to the explosive efforts of steam.

Earthquakes due to volcanic evisceration.—By the

282 - RARTHQUAKES.

ejection of ashes and lava from volcanic vents, there is
an extensive evisceration of the neighbouring ground.
When we look at a volcano like Fujiyama, 13,000 feet
in height, and at least fifty miles in circumference, and
remember that the mass of cinders and slag of which it

' is composed came from beneath the area on which it

rests, the point to be wondered at is, that earthquakes,
consequent on the collapse of subterranean hollows, are
not more frequent than they are. At the time of a single
eruption of a volcano, the quantity of lava ejected amounts
to many thousand millions of cubic feet. In 1783 the
quantity of lava ejected from Skaptas Joknee, in Iceland,
was estimated as surpassing ‘in magnitude the bulk of
Mont Blanec.’! Admitting that hollow spaces are the
results of these eruptions, and that in consequence of
this evisceration the ground is rendered unstable, the
instability being increased by the additional load placed
above the eviscerated area, it would seem that from time
to time earthquakes are inevitable.

Facts, however, teach us that volcanoes act as safety
valves, and that, as a rule, at or shortly after an eruption,
earthquakes cease. The relationship of earthquakes to
voleanic eruptions would therefore indicate, notwithstand-
ing the arguments put forward to show that an area
loaded by a volcano has in consequence of the eviseeration
and the load a quaquaversal dip, that evisceration does
not take place beneath volcanoes as is usually supposed,
and we may conclude that it is but few earthquakes
which have an origin due to these causes.

Earthquakes and evisceration by chemical degrada-
tion.—A powerful agent, which tends to the formation
of subterranean hollows, is chemical degradation. The
effects of this have been often measured by quantitative

1 Lyell, Principles, vol. ii. p. 51.

THE CAUSE OF EARTHQUAKES, 283

analysis of the solid materials which are daily carried
away by many of our springs. In limestone districts
this is very great. Prof. Ramsay estimates that the
mineral matter discharged annually by the hot springs
of Bath is equivalent in bulk to a column 140 feet
in height and 9 feet in diameter. At San Filippo, in
Tuscany, the solid matter discharged from the springs
has formed a hill a mile and a quarter long, a third of
a mile broad, and 250 feet in thickness.) Many other
examples of subterranean chemical degradation will be
found in text-books of geology.

By this chemical action large cavernous hollows are
produced. Beneath a volcano it is probable that liquid
material immediately takes the place of that which is
ejected, and that hollows are not formed as in the case of
chemical degradation. If a cavern becomes too large, it
eventually collapses.

Of the falling in of large excavations we have
examples in large mines. As a consequence, not only is
a trembling produced, but also a noise, which is so like
that produced by certain earthquakes that the South
American miners have but one word, ‘ bramido,’ to ex-
press both.?

Boussingault, who was an advocate for the theory that
many earthquakes are produced by the sinking of the
ground, calls attention to the fact that we have evidences
of the subsidence of great mountains, like the Andes, the
districts around which are so well known for their earth-
quakes. Capac Urcu is one of these mountains which
legends tell us has decreased in height.

The variation in the height of mountains is a subject
which deserves attention. That mountains may possibly
be hollow, we have the remarkable results attained by

! Lyell, Principles, vol. i. p. 402. 2 Fuchs, p. 464.

284 EARTHQUAKES.

Captain Herschel, who found that the attractive force of
gravity in the neighbourhood of the Himalayas was not
so great as it ought to have been had these mountains
been solid. The Rev. O. Fisher gives another explana-
tion of this phenomenon. Palmieri considers that the
terrible earthquake which devastated Casamicciola (1881)
was due to the hot springs having gradually eaten out
cavernous spaces beneath the town. The extremely local
character of this shock was certainly favourable to such a
view.

The earthquake which, in 1840, caused Mount Cernans,
in the Jura, to fall, is also attributed to the solvent action
of waters in undermining its foundations. This under-
mining action was in great measure probably due to a
large spring, which, twenty-five years previously, had dis-
appeared, and which subsequently may possibly have
been slowly disintegrating the foundations of the moun-
tain. Earthquakes of this order would be principally
confined to districts where there are rocks which are more
or less soluble, as, for instance, rock salt, gypsum, and
limestone.

Earthquakes and the attractive influences of the

heavenly bodies.—The most important attractions exer-
cised upon our planet are those due to the sun and moon.
To these influences we owe the tides in our ocean, and
possibly elastic tides in the earth’s crust. Some theorists
would also insist upon liquid tides in the fluid interior of
our earth. The nature of the earth’s interior is, however,
a question on which there is a diversity of opinion.

One doctrine, which, until recent years, received much
support, was that the interior of the earth was a reservoir
of molten matter contained within a thin crust. Hop-
kins showed that the least possible thickness of such a
crust must be from 800 or 1,000 miles, otherwise the

ee Oe a, :
ey ee Ye Poe ree eT

THE CAUSE OF EARTHQUAKES. 285

motions of precession and nutation would be subject to
interference. ;

M. Delauney objected to the views of Hopkins, on
the supposition that the fluid interior of the earth had a
certain viscosity. |

Sir William Thomson arrives at the conclusion that
the earth on the whole must be more rigid than a con-
tinuous solid globe of glass. Mr. George H. Darwin’s
investigations on the bodily tides of viscous or semi-
elastic spheroids tend to strengthen the arguments of
Sir William Thomson.

Some philosophers hold the view that the central
portion of the earth, although intensely hot, is solid by
pressure, whilst the outer crust is solid by cooling.
Between the two there is a shell of liquid or viscous
molten matter.

Another argument is, that although the interior of
the globe may be solid, it is only retained in that condi-
tion by: an immense pressure, on the relief of which it is
liquefied—it is potentially liquid.

_As these views, and the arguments for and against
them, are to be found in all modern text-books of
geology, we will at once proceed to consider the effect of
solar and lunar attractive influences in producing earth-
quakes upon a globe which is either solid, partially solid,
or which has an interior wholly liquid.

Effect of the attractive wnfluences of the sun and
moon. —In 1854 M. F. Zantedeschi put forward the view
—that it is probable there is a continual tendency of
the earth to protuberance in the direction of the radii
vectores of the two luminaries which attract it. In con-
sequence of these protuberances, pendulums ought at one
time to swing more slowly than at others. Zantedeschi
remarks that the periods of earthquakes appear to confirm ~

286 7.“ BARTHQUAKES,

such a view, insomuch as they occur more often at the
syzygies, or epoch of the spring tides, than at neap tides—
an observation. found in the works of Georges Baglivi
(1703) and Joseph Toaldo (1770).!

Prof. Perrey, of Dijon, who did so much for seismology,
held the view that the preponderance in the number of
earthquakes felt at particular seasons was possibly due to
the attractive influence of the sun and moon producing
a tide in the fluid interior of the earth, which, acting on
the solid crust, produced fractures.

Rudolf Falb, whose writings have of late years
attracted considerable attention, brings forward views
which may be regarded as amplifications of those sug-
gested by Perrey.

According to Falb, the inner portion of the earth
must be regarded as fluid. In the crust above this fluid
reservoir are cracks and channels, into which, by the
attraction of the moon and sun, the fluid is drawn. On
entering these cracks cooling takes place, together with
explosions of gas and subterranean volcanic disturbances.
The attractions producing the internal tides required by
Falb are chiefly dependent upon the following factors :—

1. The nearness and distance of the sun from the
earth (January 1 and July 1).

2. The position of the moon with roped to the earthy
which in every twenty-seven days is once near and once
distant.

3. The phases of the moon—whether full or new
moon (syzygies), or whether first or last quarter —
ratures ).

4. The equinoxes, the position of the sun in the
equator, and the relative position of the earth.

‘5. The position of the moon relative to the equator.
1 Comptes Rendus, August 1854.

:
=
:
E

THE CAUSE OF EARTHQUAKES. 287

6. The concurrence of the ‘centrifugal force’ of the
earth with the last quarter of the moon.

7. The entrance of the moon on the ecliptic—the
so-called nodes.

Assuming that earthquakes are wholly consequent on
these attractions, it at once becomes possible to predict
their occurrence. This Falb does, and when his predic-
tions have been fulfilled he has certainly gained notoriety.

He commenced by the predictions of great storms.
In 1873 he predicted the destructive earthquake of
Belluno, which earned for himself a eulogistic poem, which
he has republished in his ‘Gedanken und Studien tber
Vuleanismus.’ After this, in 1874, he predicted the erup-
tion of Etna. He also explained why, in B.c. 4000, there
should have been a great flood, and for a.D. 6400 he
predicts a repetition of such an occurrence.

When we approach the question of the extent to which
the attraction of the sun and moon may influence the
production of earthquakes, a question which we have to
answer is, whether it is likely that the attractive power
of the moon is so great that it could draw up the crust of
the earth beyond its elastic limits. We know what it
can do with water. It can lift up a hemispherical shell
8,000 miles in diameter about two or three feet higher
at its crown than it lifts the earth. Even supposing the
solid crust to be lifted 100 times the apparent rise of the
tide, is it likely that a hemispherical arch 8,000 miles in
diameter when it is raised 200 feet at its crown could by any
possibility suffer fracture ? If an arch is 12,000 miles in
length, all that we here ask is, whether the materials
which compose the arch are sufficiently elastic to allow
themselves to be so far stretched that the crown may be
raised 200 feet. The result which we should arrive at is
apparently so obvious that actual calculation seems hardly

288 . EARTHQUAKES.

necessary. If we regard the earth as being solid, the
question resolves itself into the inquiry as to whether a
column of rock, which is equal in length to the diameter
of the earth, or about 8,000 miles, can be elongated 200
feet without a fracture. This is equivalent to asking
whether a piece of rock one yard in length can be

stretched one seventy thousandth of a foot. Considering

that this is a quantity which is scarcely appreciable under
the most powerful of our microscopes, we must also
regard this as a question which it is hardly necessary to
enter into calculations about before giving it an answer.
To vary the method of treating such a question, may we
not ask what is the utmost limit to which it would be
possible to raise up or stretch the crust of the earth
without danger of a fracture? Thus, for instance, to
what extent might a column of rock be elongated without
danger of its being broken? From what we know of the
tenacity of materials like brick and their moduli of elas-
ticity, it would seem possible to stretch a bar of rock
8,000 miles in length for approximately half a mile
before expecting it to break. As to whether there is a
wave, the height of which is equal to half this quantity,
running round our earth as successive portions of its
surface pass beneath the attracting influences of the sun
and moon, is a phenomenon which, if it exists, would
probably long ago have met with a practical demonstra-
tion.

The deformation which a solid globe or spherical shell
would experience under the attractive influences of the
sun and moon has been investigated by Lamé, Thomson,
Darwin, and other physicists and mathematicians.

A conclusion that we are led to as one result of these
valuable investigations is, that if the interior of the earth
be fluid, and covered with a thin shell, then enormous

—

4
:
e
E
;
S
;
A
4

THE CAUSE OF EARTHQUAKES. 289

elastic tides must be produced. A consequent pheno-
menon, dependent on the existence of these tides, would
be a marked regularity in the occurrence of earthquakes.
As this marked regularity does not exist, we must
conclude that earthquakes are not due to the attractive
influences of the sun and moon acting upon the thin
crust of the earth covering a fluid interior. The period-
icity of earthquakes corroborates the conclusions of Sir
William Thomson, who remarks that if the earth were
not extremely rigid the enormous elastic tides which
must result would be sufficient to lift the waters of the
ocean up and down so that the oceanic tide would be
obliterated.

Assuming that the earth has the rigidity assigned to it
by mathematical and physical investigators, we neverthe-
less have travelling round our earth, following the attrac-
tions of the moon and sun, a tidal stress. This stress, im-
posed upon an area in a critical state, may cause it to give
way, and thus be the origin of an earthquake. Larth-
quakes ought therefore to be more numerous when these
stresses are the greatest.

The periods of maximum stress or greatest pull ex-
erted by the moon and sun will occur when these bodies
are nearest to our planet—that is, in perigee and peri-
helion, and again when they are acting in conjunction
or at the syzygies. That earthquakes are slightly more
numerous at these particular periods than at others
is a strong reason for believing that the attractions of
the moon and sun enter into the list of causes producing
these phenomena.

Had there been a strongly marked distinction in
the number of earthquakes occurring at these particular
seasons as compared with others, we might have attributed
earthquakes to the existence of elastic tides of a sensible

290 EARTHQUAKES.

magnitude. As the facts stand, it appears that the
maximum pulls exerted by the moon and sun are only
sufficient to cause a slight preponderance in the number
of earthquakes felt at particular seasons, and therefore
that these pulls only result in earthquakes when the
distorting effort has been exerted on an area which, by
voleanic evisceration, the pressure of included gases, and
other causes, is on the verge of yielding.

Earthquakes and the tides.—If we assume that
earthquakes are in many cases due to the overloading of
an area and its consequent fracture, such loading may
occur by the rising of the tide. A belief that the earth-
quakes of Japan were attributable to the tides may be
found in the diary of Richard Cocks under the date
November 7, 1618, who remarks :—

‘And, as we retorned, about ten aclock, hapned a
greate earthquake, which caused many people to run
out of their howses. And about the lyke hower the
night following hapned an other, this countrey being
much subject to them. And that which is comunely
markd, they allwais hapen at a hie water (or full sea);
so it is thought it chauseth per reason is much wind
blowen into hollow caves under ground at a loe water,
and the sea flowing in after, and stoping the passage
out, causeth these earthquakes, to fynd passage or vent
for wha wind shut up.’!

Although we may not acquiesce in Cock’s views re-
specting the imprisoned wind, it would seem that a
comparison of the occurrence of earthquakes and the
state of the tide would be a legitimate research. JInas-
much as the stresses which are brought to bear upon an
area by the rising of the tide are so very much greater
than those due to barometrical changes, it is not unlikely
1 Nature, April 26, 1883.

THE CAUSE OF EARTHQUAKES, 291

that a‘marked connection would be found. But it must
be remembered that because researches, so far as they
have gone, tend to show that earth movements are more
frequent when an area is relieved of a load, it is not
unlikely that the greatest number of earthquakes may
be found to occur at low water. Prof. W. 8. Chaplin
attempted to make this investigation in Japan, but not
being able to obtain the necessary information respecting
the tides, was compelled to relinquish this interesting
work. |

Every foot of rise in a tide is equivalent to a load
being placed on the area over which the tide takes place
of sixty-two pounds to the square foot. This load is not
evenly distributed, but stops abruptly at a coast line.
Lastly, it may be observed that many coast lines are not
simultaneously subjected to stresses consequent upon this

load. Japan, for instance, may be regarded as an arch
placed horizontally. The area near the crown of this

arch is loaded by the tidal wave crossing the Pacific before
the areas near the abutment, and farther there is a
horizontal pressure at the crown which, if Japan were
like a raft, would tend, as the tide advanced, to straighten
its bow-like form, but as the wave passed its abutments
to increase its curvature. |

__ Prof. G. Darwin has calculated the amount of rise and
fall of a shore line due to tidal loads (see p. 336, ‘ Earth
Pulsations’). The result of these calculations apparently
indicates that these loads may have a considerable in-
fluence upon the stability of an area in a more or less
critical condition.

Mr. J. Carruthers suggests that tidal action may hold
ageneral but indirect relationship to volcanic and seismic
action by the retardation it causes on the earth’s rotation.
By this retardation the polar axis tends to lengthen, and

292 . EARTHQUAKES.

tensile stresses are induced, resulting in fracture. The
fluid interior of the earth, being no longer restrained,
would move polewards, and, leaving equatorial portions
unsupported, this would gradually collapse. The primary
fractures would be north and south, while the secondary
fractures would be east and west.!

That the rise of the tide is accompanied by a greater
percolation of .water to volcanic foci, which, in conse-
quence, assume a greater state of activity, is a theory
which was advanced many years ago. To determine
how far tides may directly be connected with earthquakes,
the necessary records have yet to be examined.

Variations im atmospheric presswre.—When we
consider the immense load which, by a sudden rise of
the barometer, is placed upon the area over which this
rise takes place, it is not difficult to imagine that this
rise may occasionally be the final cause which makes the
crust of the earth to give way. A barometric rise of
an inch is equivalent to a load of about seventy-two
pounds being put upon every ‘square foot of area over
which this rise takes place. On the other hand, a fall
in the barometric column indicates that a load has been
removed, and whatever elastic effort may be exerted by
subterranean forces in endeavouring to escape, being
met by less resistance, they may burst these bonds, and
an earthquake will result. For reasons such as these
the final cause of earthquakes has often been attributed
to variations in atmospheric pressure. In Japan there
are practically as many earthquakes with a high barometer
as with a low one.

The extent to which barometric fluctuations have
acted as final causes in the production of earthquakes
may be judged of by a comparison of the times of baro-

1 Phil. Soc., Wellington, New Zealand, 1875. -

tad

ee

AAP ea Oe ee

Re at, Cree SRE Oe eee ee Pe ee ee ee i ee es

See he SEP A eR Sen. enae

THE CAUSE OF. EARTHQUAKES, 293

metric variation and the times at which ee have
occurred.

Three important laws of barometric variation are the
following :—

1. In the world generally the average barometric
pressure is highest in winter. (Exceptions occur near
Iceland and in the North Pacific.)

2. The summer and winter monthly mean barometer
differs least near the equator and over the. great oceans.
They differ most over the great continents and generally
with increasing latitude.

3. The greatest number of barometrical fluctuations
usually take place in winter.

Inasmuch as there are generally more earthquakes in
winter than in summer, the first of these laws would
indicate that this might be due to the greater load which
acts upon the crust of the earth at that season. The
second law would indicate that the distinction between
the winter and summer earthquakes ought to be most
marked in high latitudes, which, if we refer to the table
on p. 257, we observe to be borne out by the results of
observation. The countries where there are as many
earthquakes in winter as in summer are chiefly those in
low latitudes. The number of these countries from which
we have records are, however, few.

Facts opposed to the idea that earthquakes may be
caused by an increase of barometric pressure are the

results of observations like those of Schmidt and Rossi,

which show that earthquakes chiefly occur with a low
barometer.

Assuming that these latter observations will be found
by future investigators to be generally true, we must
conclude: that the relief of atmospheric pressure has an
influence upon the occurrence of earthquakes. Such a

294 EARTHQUAKES.

conclusion would partially accord with the third barome-
trical law, or the fact that there are more occasions on
which we get a low barometer during the winter months.

Other writers who have examined this question are
Volger, Kluge, Andrés, and Poly. The latter investigator
sought a connection between earthquakes and revolving
storms, in the centres of which there is usually an ab-
normal decrease of atmospheric pressure. If an area over
which such a sudden change in pressure took place was
in a critical state, it is not difficult to see that storms
such as Poly refers to might sometimes be accompa
by earthquakes.

Fluctuations in temperature.—Inasmuch as fluctua-
tions in temperature are governed by the sun, it may at
once be said that there is a connection between earth-
quakes and readings of the thermometer. Certainly
earthquakes occur mostly during the cold months or
in winter. Similarly, as changes in temperature are so
closely connected with barometric fluctuations, and these
are said to have a direct influence upon the yielding of
the earth’s crust, seismic phenomena are indirectly linked
to fluctuations in temperature. A rise in temperature is
usually accompanied by a fall in the barometer, and this
in turn may be a condition favourable for the occurrence
of an earthquake. :

If we regard solar heat as an agent causing expansions
or contractions in the earth’s crust, then fluctuations in
temperature become an immediate cause of earthquakes.
The probability, however, is that solar heat has little or
no connection with the final cause producing earthquakes,
although at the same time coincidences between the
occurrence of earthquakes and unusual fluctuations in
temperature may from time to time be observed.

Winds and earthquakes.—Although it may be

le
a
ay

- THE CAUSE OF EARTHQUAKES. 295

admitted that high winds exert enormous pressures upon
mountain ranges, and might occasionally give rise to
stresses causing rocky masses in unstable equilibrium to
give way, the coincidences which have been established
between the occurrence of storms and earthquakes can
usually only be regarded as occurrences which have
synchronised by chance.

Storms are usually accompanied with a barometric
depression, and the relation of diminutions in atmo-
spheric pressure to earthquakes has been discussed.

Rain and earthquakes.—It has already been shown
that earthquakes have occasionally been found to coin-
cide with rain and rainy seasons. Whether the saturation
of the ground with moisture or the percolation of the
same to volcanic foci may be a direct effect producing
earthquakes it is difficult to say. The probability,
however, is that, rain being dependent on phenomena
like changes in temperature, barometric fluctuations, and
winds, we must regard it and the earthquakes which
happen to coincide with these precipitations of moisture
as congruent effects of more general causes.

Conclusion.—Although it would be an easy matter to
discuss the relationship of earthquakes and other pheno-
mena, we must conclude that the primary cause of
earthquakes is endogenous to our earth, and that
exogenous phenomena, like the attraction of the sun and
moon and barometric fluctuations, play but a small part
in the actual production of these phenomena, their
greatest effect being to cause a slight preponderance in the
number of earthquakes at particular seasons. They may,
therefore, sometimes be regarded as final causes. The
majority of earthquakes are due to explosive efforts at
voleanic foci. The greater number of these explosions
take place beneath the sea, and are probably due to the

14

296 _.. EARTHQUAKES,

admission of water through fissures to the heated rocks
beneath. A smaller number of earthquakes originate at
actual volcanoes. Some earthquakes are produced by the
sudden fracture of rocky strata or the production of
faults. This may be attributable to stresses brought
about by elevatory pressure. Lastly, we have earth-
quakes due to the collapse of underground excavations.

eee are

CHAPTER XVIIL
PREDICTION OF EARTHQUAKES,

General nature of predictions—Prediction by the observation of un-
usual phenomena (alteration in the appearance and taste of springs;
underground noises; preliminary tremors; earthquake prophets
—warnings furnished by animals, &c.)—Harthquake warning.

General nature of predictions.—Ever since seismology
has been studied, one of the chief aims of its students has
been to discover some means which would enable them to
foretell the coming of an earthquake, and the attempts
which have been made by workers in various countries to
correlate these occurrences with other well-marked pheno-
mena may be regarded as attempts in this direction.

Ability to herald the approach of these calamities
would unquestionably be an inestimable boon to all who
dwell in earthquake-shaken countries, and the attempts
which have been made both here and in other places are
extremely praiseworthy. In almost all countries where
earthquakes are of common occurrence these movements
of the earth have been more or less connected with
certain phenomena which, in the popular mind, are
supposed to be associated with an approach of an
earthquake. _

If predictions were given in general terms, and they
only referred to time, inasmuch as on the average there
are in the world several shakings per day, we should

298 EARTHQUAKES.

always find that predictions were verified. We might
even go further and predict that on certain days earth-
quakes would occur in certain countries, and still find
that in many instances our supposed power of foresight had
not deceived us. Thus, for instance, in Japan, where on
the average there are probably one or two shakings every
day, if prognostications were never correct there would
be a violation of the laws of chance.

What is required from those who undertake to
forewarn us of an earthquake is an indication not only
of the time at which the disturbance will happen, but
also an indication of the area in which it is to occur.
Those who dwell in an area where there are certain well-
defined periods during which seismic activity is at a
maximum—if ten or fourteen days should have passed
without a shock—might, in many instances, find that a
prophecy that there would be an earthquake within the
next few days would prove itself correct. Also, if a severe
shock had taken place, a prophecy that there would be a
second or third smaller disturbance within a short period
would also meet with verification. .

Certain persons with whom I am intimate appear to
have persuaded themselves that they can foretell the
coming of an earthquake by the sultry state of the
atmosphere or a certain oppressiveness they feel, and an
instinctive feeling arises that an earthquake is at hand.

It is said that a few minutes before many of the
shocks which shook New England between 1827 and
1847 people could foretell the coming disturbance by an
alteration in their stomach.! No doubt many who dwell
in earthquake countries, and have been alarmed by earth-
quakes, are at times subject to nervous expectancy.

The author has had such sensations himself, due, per-

1 Phil. Trans., vol. xiii.

PREDICTION OF EARTHQUAKES, 290

haps, to a knowledge that it was the earthquake season,
that there had been no disturbance for some weeks, and a
consequent increasing state of nervous presentments. In
consequence of this, not only has he carefully prepared
his instruments for the coming shock, but he has written
and telegraphed to friends to do the same.

Sometimes these guesses have proved correct. One
remarkable instance was a few hours prior to the severe
shock of February 22, 1880, when he communicated with
his friends in Yokohama and asked them to see that
their instruments were in good order. Oftener, however,
his prognostications have been incorrect. The point in
connection with this subject which he wishes to be re-
marked is, that the instances where earthquakes occurred
shortly after the receipt of his letters are carefully re-
membered, and often mentioned, but the instances in
which earthquakes did not occur appear to be entirely
forgotten. He is led to mention these facts because they
appear to be an experimental proof of what has taken
place in bygone times, and what still takes place, espe-
cially amongst savages—namely, that the record of that
which is remarkable survives, whilst that which is of
every-day occurrence quickly dies. Had the records of
all prognostications been preserved, the probability is
that we should find that they had, in the majority of
cases, been incorrect, whilst it would have been but in
very few instances they had been fulfilled.

Prediction by the observation of natural pheno-
mena—The above remarks may perhaps help us to
understand the prognostications of the ancient philo-
sophers about which Professor Antonio Favaro, cf Padua,
has written.’ Cicero in the ‘ De Divinatione,’ speaking on
this subject, says that ‘God has not predicted so much

1 M.S. di Rossi, Zarthquakes of Casamicciols.

300 EARTHQUAKES.

as the divine intelligence of man.’—* Non Deus previdet
tantum, sed et divini ingenii viri.’ Favaro regards these
predictions, however, as the result of observations of nature
which show it is possible that indications of coming earth-
quakes had been announced by variations in the gas given
out from subterranean sources, the change in colour,
taste, level, temperature of the water in springs, &e.

In 1843 a bishop of Ischia forewarned his people of a
coming earthquake, and thus was instrumental in the
saving of many lives. Naturally, in an age of superstition,
the bishop would be regarded as a prophet, but Favaro
considers that the prognostication was probably due to a
knowledge of premonitory signs as exhibited in changes
in the characters of mineral waters.

The shock of 1851, at Melpi, was in this way predicted
by the Capuchin fathers, who observed that a lake near
their door became frothy and turbulent.

Underground noises have led persons to the belief
that an earthquake was at hand. It was in this way that

- Viduari, a prisoner at Lima, predicted the destruction of

that city. 3

Before the earthquake of 1868, so severely felt at
Iquique, the inhabitants were terrified by loud subter-
ranean noises.

That underground noises have preceded earthquakes
by considerable intervals appears to be a fact, but, at the
same time, it must be remembered that similar noises
have often occurred without an earthquake having taken
place.

Farmers predicted the earthquake of St. Remo, in
1831, by underground noises.

On the day before the earthquake which, in 1873,
shook Mount Baldo, the inhabitants of Puos, a village
north of Lake Santa Croce, heard underground noises.

PREDICTION OF EARTHQUAKES. 301

Before the earthquakes which, in 1783, shook Calabria
and Sicily, fish are said to have appeared in great numbers
on the coast of Sicily, and the whirlpool of Charybdis
assumed an unusual excited state.

It is said that Pherecydes predicted the earthquakes
of Lacedemon and Helmont, by the taste of the water in
the very deep well at the castle of Lovain.!

The writer of an article on the Lisbon meeps

says that ‘after the 24th I felt apprehensive, as I
observed the same prognostics as on the afternoon of
October 31, that is, the weather was severe, the wind
northerly, a fog came from the sea, the water in a foun-

etain ran of a yellow clay colour, and’ he adds, ‘ from

midnight to the morning of the 25th I felt five shocks.’ ?

At the present time Rudolf Falb, following a theory
based upon the attractive influences of the sun and moon,
tells us the time at which we are to expect earthquakes.

That occasionally there are signs attendant on earth-
quakes, although we cannot give them a physical ex-
planation, we cannot doubt. Also we know that in
certain areas earthquakes are more likely to occur at
one season than at another. Should earthquakes be
foretold with the assistance of knowledge of this de-
scription, the predictions at once become the result of
the application of certain natural laws, and are not to
be regarded as predictions in the popularly accepted sense
of that term, any more than the arrival of a friend is pre-
dicted by the previous receipt of a telegram announcing
his coming.

Rather than accredit the ancients and those of more
modern times who, in consequence of their feelings, have
recorded the coming of an earthquake, with a knowledge
of premonitory signs, we might in many instances regard

1 Phil. Trans., vol. xviii. 1683- 6. 2 Thid. vol. xix.

302 EARTHQUAKES.

the records of those prognostications as the survival of
accidental guesses, and, as such, examples of the survival
of the useless.

The effect of accidental occurrences of this description
upon an uneducated mind, in engendering superstition, is
a subject which has often been dwelt upon, and the diffi-
culty of eradicating the same—as may be judged of by the
following accident which came under the observation of
Mr. T. B. Lloyd and the author, in 1873, when travelling
in Newfoundland—will be easily appreciated.

At the time to which I refer, my companion was
bringing a canoe down the rapids below the Grand Pond

in a country which is practically uninhabited, and where.

an Indian trapper would perhaps be the only person met
with, and this not more than once a year. Whilst
shooting the rapids one of the Indians, Reuben Soulian,
shot at a deer passing up one bank of the river. That
the deer had been hit was testified by a trail of blood
which bespattered the rocks. Subsequently several more
shots were fired, and it was believed by all that the deer
was killed. Soulian quickly followed the animal to the
spot where it was supposed to have fallen. Some time
after he returned, having failed to find any trace of the
animal. He was greatly agitated, but eventually became
melancholy, saying that the sudden disappearance of the
animal was a sure sign that some of his relations had
suddenly died. About two hours afterwards Mr. Lloyd’s
party met with a party of Indians coming up the river,
the first they had seen for four weeks, who told them
that Soulian’s sister had just died on the coast.

In the northern part of South America certain shocks
are anticipated by preliminary vibrations which cause a
little bell attached to a T-shaped frame (cruz sonante) to
ring. There are, however, persons (trembloron) who are

a ae oe ee ME ey

PREDICTION OF EARTHQUAKES. 303

supposed to be endowed with seismic foresight, whose
verdicts are much relied upon.

In Caraccas it is said that nearly every street in the
river suburb has an earthquake Cassandra or two. Some
of these go so far not only as to predict the coming
seisms, but also the vicissitudes of particular streets.!
Earthquake prophets are, however, by no means confined
to the new world, and many examples of them may be
found in the histories of countries where earthquakes have
been felt.

The story of the crazy lifeguardsman who prophesied
an earthquake to take place in London on April 4, 1691,
is an example. The Rev. Sig. Pasquel R. Perdini,
writing on the earthquakes at Leghorn in 1742, says
that ‘a Milanese astrologer predicted this earthquake
for January 27, by which “misfortune” the faith and
credit given to the astrologer gained him more rever-
ence and honour than the prophets and holy gospel.’
Before the time at which he predicted a second shock,
people removed away from Leghorn.

Warnings furnished by animals.—A study of the
warnings furnished by animals is also interesting. Several
of the natives in Caraccas possess oracular quadrupeds,
such as dogs, cats, and jerboas, which anticipate coming
dangers by their restlessness.

Before the catastrophe of 1812, at Caraccas, a Spanish
stallion broke out from its stable and escaped to the high-
lands, which was regarded as the result of the prescience
of a coming calamity. Before the disturbances of 1822
and 1835, which shook Chili, immense flocks of sea birds
flew inland, as if they had been alarmed by the com-
mencement of some suboceanic disturbance. Before this

‘H. D. Warner, ‘The City of Usa asa Atlantic Monthly,
March 1833. é

304 EARTHQUAKES.

last shock it is also related that all the dogs escaped from
the city of Taleahuano.

Earthquake warning.—What has here been said
respecting the prediction of earthquakes is necessarily
imperfect—many of the signs which are popularly sup-
posed to enable persons to foretell the coming of an earth-
quake having already been mentioned in previous chapters.
That we shall yet be able to prepare ourselves against
the coming of earthquakes, by the applications of laws
governing these disturbances, 1s not an unreasonable hope.

- With an electric circuit which is closed by a movement
‘of the ground, we are already in a position to warn the
dwellers in surrounding districts that a movement is
approaching.

An earthquake which travelled at the rate of four
seconds to the mile might, if it were allowed to close a
circuit which fired a gun at astation fifteen miles distant,
give the inhabitants at that place a minute’s warning to
leave their houses. The inhabitants of Australia and the
western shores of the Pacific might, by telegraphic com-
munication, receive eighteen to twenty-five hours’ warn-
ing of the coming of destructive sea waves resulting from
earthquakes in South America.

Although warnings like these might have their vais
that which is chiefly required is to warn the dwellers
at and near an earthquake centre of coming disturbances.

What the results of the observations on earth tremors
will lead to is problematical.

Should microseismic observation enable us to say when
and where the minute movements of the soil will reach a
head, a valuable contribution to the insurance of human
safety in earthquake regions will have been attained.

As to whether the movements of tromometers are
destined to become barometric-like warnings of increased

PREDICTION OF EARTHQUAKES. 305

activity beneath the earth crust, or whether they are only
due to vibrations of the earth crust produced by variations
in atmospheric pressure, has yet to be investigated.

Other phenomena which may probably forewarn us of
the coming of an earthquake are phenomena resultant on
the stresses brought to bear upon the rocky crust previous
to its fracture, or phenomena due to changes in the posi-
tion and condition of heated materials beneath the earth’s
surface. Amongst these may be mentioned electrical
_ disturbances, which appear to be so closely related to
seismic phenomena. 5

At the time of earthquakes telegraph lines have been
disturbed, but as to what may happen before an earth-
quake we have as yet but little information. The subject
of earthquake warning is of importance to many countries,
and is deserving of attention.

As our knowledge of earth movements, and their at-
tendant phenomena, increases, there is but little doubt
that laws will gradually be formulated, and in the future,
as telluric disturbances increase, a large black ball gradu-
ally ascending a staff may warn the inhabitants on the
land of a coming earthquake, with as much certainty as
the ball upon a pole at many seaports warns the mariner
of coming storms,

:

306 EARTHQUAKES.

CHAPTER XIX.
EARTH TREMORS.

Artificially produced tremors—Observations of Kater, Denman, Airy,
Palmer, Paul— Natural tremors— Observations of Zdllner, M.
d’Abbadie, G. H. and H. Darwin—HExperiments in Japan—With
seismoscopes, microphones, pendulums — Work in Italy—Bertelli,
Count Malvasia, M. 8. di Rossi—Instruments employed in Italy—
Tromometers,-microseismographs, microphones—Results obtained in
Italy—in Japan—Cause of microseismic motion.

Durinc the past few years considerable attention has

been drawn towards the study of small vibratory motions
of the ground, which to the unaided senses are usually
passed by without recognition. These motions are called
earth tremors. Their discovery appears to have been
due to accident, and not to the results of inductive
reasoning. No sooner had philosophers contrived astro-
nomical and other instruments for the purpose of making
refined measurements and observations than they at once
discovered that they had an enemy to contend against in
the form of microscopic earthquakes.

Artificially produced tremors.—Artificial disturb-
ances of this description exist in all our towns, and near
a railway line they are perceptible with every passing
train. Those who have used microscopes of high power
will readily appreciate how small a disturbance of the
ground is visible in the apparent movement of the object
under examination. 3

;
.
x
;
|

EARTH TREMORS. 307

Captain Kater found that he could not perform his
pendulum experiments in London on account of the
vibrations produced by the rolling of carriages. Captain
Denman, who made some observations on artificially
produced tremors, found that a goods train produced an
effect 1,100 feet distant in marshy ground over sand-
stone. Vertically, however, above a tunnel through the
sandstone, the effects only extended 100 feet.

A remarkable example of the trouble which artificially
produced earth vibrations have occasioned those who
make astronomical observations occurred some twenty
years ago at the Greenwich Observatory. When deter-
mining the collimation error of the transit circle by
means of the reflexion of a star ina tray of mercury, it was
found that on certain nights the surface of the mercury
was in such a state of trembling that the observers were
unable to complete their observations until long after
midnight. After obtaining a series of dates on which
these disturbances occurred, it was found that they coin-
cided with public and bank holidays, on which days crowds
of the poorer classes of London flocked to Greenwich
Park, and there amused themselves with running and
rolling down the hill on which the observatory is situated.
On these occasions it was found that the disturbances
in the mercury were such that observations could not be
made until two or three hours after the crowds had been
turned out of the neighbouring park.!

- To obviate this difficulty Sir George Airy suspended
his dish of mercury in a system of indiarubber bands, and
in this way succeeded in eating the intruders up.

Lieutenant-Colonel H. 8. Palmer, R.E., when engaged
with the transit of Venus expedition in New Zealand, in
1874, was troubled with vibrations produced from a

Palmer, Trans. Seis. Soc. of Japan, vol. iii. p. 148.

308 EARTHQUAKES.

neighbouring railway. To escape the enemy he in-
trenched his instruments by placing them in pits. With
pits 34 feet deep he found himself sufficiently protected.
The distance from the line was about 400 yards, and the
soil through which the disturbances were propagated was
a coarse pebbly gravel.!

Before the United States Naval Observatory was
established at Washington, Professor H. M. Paul was
deputed to make a tremor survey to discover stable
ground. The results of these experiments were exceed-
ingly interesting. By watching the reflected image of a
star in a dish of mercury a passing train would be noticed
at the distance of a mile. Its approach could be detected
by the trembling of the image before its coming could
be heard. At one point of observation the disturbance
appeared to be cut off bya ravine. The strata was gravel
and clay.? ;

These few examples of artificially produced tremors,
to which many more might be added, have been given
because they teach us something respecting their nature.
Hitherto earth tremors have only been regarded as
intruders, which it was necessary to escape from or des-
troy. From what has been said they appear to be a
superficial disturbance which is propagated to an enor-
mous distance. This distance appears to depend upon
the propagating medium, upon the intensity of the
initial disturbance, and upon its duration. In the obser-
vation of these artificial disturbances, which are accessible
to every one, and which hitherto have been so neglected,
we have undoubtedly a fruitful source of study.

Natural tremors.—Next let us turn to those micro-
scopical disturbances of our soil which are due to natural

1 Palmer, Trans. Seis. Soc. of Japan, vol. iii. p. 148.
2 Paul, Trans. Seis. Soc. of Japan, vol. ii. p. 41.

j
wet: eae

aN ey eee ee a eke EN

eas EN wien ot iin

4
j
i

EARTH TREMORS. 309

causes. Thus far they seem to have been recorded wher-
ever instruments suitable for their detection have been
erected, and it is not improbable that they are common
to the surface of the whole globe.

Some of the more definite observatious which have
been made upon earth tremors were those made in con-
nection with experiments on the deviation of the vertical
due to the attractive influence of the moon and sun.

Professor Zollner, who invented the horizontal pendu-
lum which he used in the attempt to measure the change
in level due to lunar and solar attraction, found his instru-
ments so sensitive that the readings were always changing.

The most interesting observations which were made
upon small disturbances of the soil were those of M.
d’Abbadie, who carried on his experiments at Abbadia, in
Subernoa, near Hendaye, 400 métres distant from the
Atlantic, and 62 métres above sea level. The soil was a
loamy rock. Here M. d’Abbadie constructed a concrete
cone 8 métres in height, which was pierced down the
centre by a vertical hole or well, which was continued two
métres below the cone into the solid rock. At the
bottom of this hole or well a pool of mercury was formed
which reflected the image of cross wires placed at the
top of the hole. These cross wires and their reflection
were observed by means of a microscope. The observa-
tions consisted in noting the displacement and azimuth
of the reflected image relatively to the real image of the
wires. After allowing this structure five years to settle,
M. d’Abbadie commenced his observations. To find the
surface of the mercury tranquil was a rare occurrence.
Sometimes the mercury appeared to be in violent motion,
although both the air and neighbouring sea were perfectly
calm. At times the reflected image would disappear as
if the mercury had been disturbed by a microscopic
earthquake.

310 EARTHQUAKES,

The relative positions of the images were in part
governed by the state of the tide. Altogether the move-
ments were so strange that M. d’Abbadie did not venture
any speculations as to their cause, but he remarks that
the cause of the changes he observed were sometimes
neither astronomical nor thermometrical. These observa-
tions, the principal object of which was to determine
changes in level rather than earth vibrations, were carried
on between the years 1868 and 1872.!

Observations at Cambridge.—Another instructive set
of observations were those which were made in the years
1880-1882, by George and Horace Darwin, in the Caven-
dish Laboratory, at Cambridge. The main object in these
experiments was to determine the disturbing influence of
gravity produced by lunar attraction. The result which
was obtained, however, showed that the soil at Cambridge
was in such an incessant state of vibration that whatever
pull the moon may have exerted upon the instrument
which was employed was masked by the magnitude of
the effects produced by the earth tremors, and the ex-
periments had, in consequence, to be abandoned.

The principle of this instrument was similar to one
devised by Sir William Thomson, and put up by him in
his laboratory at Glasgow. As erected by the brothers
Darwin, at Cambridge, it was briefly as follows: A
pendulum, which was a massive cylinder of pure copper,
was hung by a copper wire, about four feet long, inside a
hollow cylindrical tube rising from a stone support. A
small mirror was then hung by two silk fibres, one
of which was fastened to the bob and the other to the
stone basement. A ray of light sent from a lamp on to
the mirror was reflected to a scale seven feet distant, and
by this magnification any motion of the bob relatively to

1G. H. and H. Darwin, Reports of British Association, 1881.

ee i =

a ee en

EARTH TREMORS. 311

the stone support was magnified 50,000 times. In
several ways the apparatus was insulated from all accidental
disturbances. The spot of light was observed from
another room by means of a telescope. This instrument
was so delicate that even at the distance of sixteen feet
the shifting of your weight from one foot to the other
caused the spot of light to run along the scale. So
sensitive was, the instrument that, notwithstanding its
being cut off from the surrounding soil. by a trench filled
with water and the whole instrument being immersed in
water to damp out the small vibrations, it would seem
that the ground was in aconstant state of tremor ; in fact,
so persistent and irregular were these movements that it
seemed impossible to separate them from the perturbations
due to the attraction of the moon.!

As a result of observations like these, the world had
gradually forced upon it the fact that the ground on
which we live is probably everywhere in what is practically
an incessant state of vibration.

This led those who were interested in the study of
earth movements to establish special apparatus for the
purpose of recording these motions with the hope of
eventually discovering the laws by which they were
governed.

Experiments in Japan.—The simpler forms of appa-
ratus which have been used in Japan may be described
as delicate forms of seismoscopes, which, in addition to
recording earth tremors, also record the occurrence of
small earthquakes.

A simple contrivance which may be used for the pur-
pose of recording small earthquakes can be made with a
small compass needle.

Ifa light, small sensitive compass needle be placed on

1 Reports of British Association, 1881.

312 EARTHQUAKES,

a table, it will be found that a small piece of iron like a
nail may be pushed so near to it that the needle assumes
a position of extremely unstable equilibrium. If the
table now receives the slightest tap or shake this condition
is overcome, and the needle flies to the iron and there
remains. By making the support of the needle and the
iron the poles of an electric circuit it is possible to
register the time at which motion took place with con-
siderable accuracy.

With crude apparatus like this a large number of
small earth disturbances have been recorded.

Another form of apparatus, employed in Japan, has
been a delicately constructed circuit closer. ‘The motions
of this instrument were recorded by causing an electro-
magnet to deflect a pencil which was tracing a circle on
a revolving dial. The revolving dial was a dise of wood
covered with paper fixed to the hour-hand axle of a
common clock.

A third form of apparatus used in Japan consisted er
a small piece of sheet lead about the size of a threepenny
piece suspended by a short loop from a rigid support.
Projecting from the lead a fine wire, about two inches in
length, passed freely through a hole in a metallic plate.
By the slightest motion of the support the small pendulum
of lead was set into a state of tremor and caused its
pointer to come in contact with one or other side of the
hole in the metal plate and thus to close an electric circuit.

A more refined kind of apparatus which has been
employed in Japan was similar to that used by the
Darwins at Cambridge. This was so arranged that any
deflection of the mirror was permanent until the instru-
ment was reset, and in this way the maximum disturbance
which had taken place between each observation was
recorded.

:
j
;
:

9
:

‘

}
-.
ss
A

EARTH TREMORS. } 313

In addition to these and other contrivances, experi-
ments were made with microphones.

The microphones used were small doubly pointed
pencils of carbon about three centimetres long, saturated
with mercury, and supported vertically in pivot holes bored
in other pieces of carbon, which were the terminals of an
electric circuit. These microphones were screwed down on
the top of stakes driven deeply into the ground. They
were covered with a glass shade thickly greased at its base.
The stakes were in the ground at the bottom of a small
pit—about two feet square and two feet deep—which was
lined with a box. The box was covered with a lid, and
earth to the depth of nine inches or one foot. One of.
these pits was in the middle of a lawn in the front of my
house, and the other was at the foot of a hill at the back
of the house. The wires from the microphone passed
through the side of the box into a bamboo tube and
thence up to my dining-room and bed-room. In one of
the circuits there were three Daniell’s cells, a telephone,
and a small galvanometer. I used the galvanometer
because I found that when there was sufficient motion in
the microphone to produce a sound in the telephone a
motion in the needle of a galvanometer was produced.
If in any case motion took place in the magnetic needle
during my absence, it was held deflected by a small piece
of iron with which it was brought into contact by the
movement.

The sensitiveness of the arrangement may be judged
of from the fact that if a person walked on the grass
within six feet of the microphone, each step caused a
creak in the telephone, and the needle of the galvano-
meter was caused to swing and come in contact with the
iron. Dogs running on the grass had no effect. A small
stone one or two inches in diameter thrown from the

314 EARTHQUAKES.

house so that it fell near to the microphone pit cattsed
a sharp creak in the telephone and a movement in the
needle.

The nature of the records I received from this con-
trivance may be judged of from the following extract from

my papers.
1879. Nov. 12th 7

h. m.
7 O P.M. contact of needle

7 2 ,, difficult to set the needle

7 3 4, needle swings and telephone creaks
Cs ” 39 ” 99

7 5 ” 29 ” Pp =
7 6

7 10 . 3 sabe auINES é ‘
711°, again *
Here I went out, took away the covering, and examined
the microphone. Nothing wrong was to be observed.
All that I saw was one small ant. I do not think that
this could have caused the disturbance, because it could
not get near the instrument.

On the succeeding nights I experienced similar disturb-
ances, and it seemed as if they might possibly have been
the prelude to several small shocks which occurred about
this time (November 15, 16, and 17). On November 17,
at 8 A.M., the needle was found in contact, and again at
5 P.M., and at 6 P.M. the shock of a small earthquake was
felt which caused a rattling sound in the telephone
for about one minute after the motion had appeared
to cease. The needle swung considerably, but did not
come in contact.

The great objection to these observations is that it is
possible that the movements and sounds which J have
recorded might, with the exception of one case when the
shaking was actually felt, possibly have been produced by
causes other than that of the movement of the ground.
To determine this I subsequently put up two distinct sets

EARTH TREMORS. als

of apparatus to determine whether the motions of each
were synchronous. So far as I went this appeared only
to be sometimes the case :—but this is a question difficult
to determine, unless a recorder of time be added to the
apparatus. |

The greatest objection to observations of this sort is
that the sensibility of the instrument is not constant.
After a current has been running for several days it is no
longer sensible to slight shocks, it appears as if its resist-
ance had been increased. To overcome this it is neces-
sary to resharpen the carbon points and bore out the
pivot holes every three or four days. Farther, the battery
varies. This might to some extent be overcome by using
a battery with large plates. These two causes tend to
reduce the sensitiveness of the galvanometer-like recorder
—the deflection of the needle gradually becoming less
and less, and therefore day by day needing a greater
swing to bring it into contact with the iron. For reasons
such as these this instrument, to be used successfully,
appears to require considerable attention.

Another form of microphone employed by the author
consisted of an aluminium wire standing vertically on a
metallic plate, its upper end passing loosely through a
hole in an aluminium wire standard.

The upper end of the vertical wire was loaded with
lead. This contrivance possesses all the sensitiveness of
an ordinary microphone, whilst, if it receives a sudden
impulse, there is a sudden break in the current, and
the vertical wire is thrown from one side to the other of
the hole in the standard.

After many months of tiresome observation with
instruments of this description, and after eliminating all
motions which might have been produced by accidental
causes, the general result obtained showed that in Tokio

316 EARTHQUAKES.

there were movements of the soil to be detected every
day, and sometimes many times per day, which to ordinary
persons were passed by unnoticed.

Work im Italy.—The most satisfactory observations
which have been made upon microseismic disturbances
are those which have been made during the last ten years
in Italy. The father of systematical microseismical re-
search appears to have been Father Timoteo Bertelli, of
Florence.

In 1870: Father Bertelli suspended a pendulum in
a cellar, and observed it with a microscope. As the
result of his observations it was announced that he had
perceived the earthquakes which shook Romagna, although
to the ordinary observer in Florence these shakings had
not been perceptible.

In 1873 Bertelli, by means of microscopes fixed in
several azimuths, made 5,500 observations on free pen-
dulums. He also made observations on reflections from
the surface of mercury.! |

One result of these observations was to show that
microseismic motions increased with a fall of the baro-
meter. Similar observations were made at Bologna by
M. le Conte Malvasia, and also by M. S. di Rossi, near
Rome. On January 14, 15, and February 25 these three
observers at their respective stations simultaneously ob-
served great disturbances.

Similar investigations were made at Nice by M. le
Baron Prost. |

Although doubt was cast upon Bertelli’s observations
they appear to have been the origin of a series of micro-
seismical observations, a distinguished leader in which is
Professor Rossi, who, in 1874, found that large earthquakes
were almost always preceded or accompanied with micro-

gi Comptes Rendus, 1875, January to June, p. 685.

EARTH TREMORS. 317

seismical storms. In 1878 Professor Rossi worked upon
these small disturbances with the assistance of the micro-
phone and telephone, and his first results were published
by Professor Palmieri.

Many of Professor Rossi’s observations were made
in the grotto of Roca de Papa, 700 métres high and
eighteen métres under the soil. Here over 6,000 obser-
vations were made by means of microscopes, on pendu-
lums of different lengths, suspended in tubes cut in
the solid rock.

Instruments employed in Italy.—It is impossible to
describe in detail the various forms of apparatus which
have been used by the Italian investigators. A descrip-
tion of one or two of the more important instruments may
not, however, be out of place, inasmuch as they will assist
the reader to understand the manner in which the various
results respecting the laws governing microseismic move-
ments have been arrived at.

The most important of these instruments is the
Normal Tromometer of Bertelli and Rossi.

This consists of a pendulum 14 metres long, carrying,
by means of a very fine wire, a weight of 100 grammes.
To the base of the bob a vertical stile is attached, and
the whole is enclosed in a tube terminated, at its base,
by a glass prism of such a form that when looked through
horizontally the motion of the stile can be seen in all
azimuths. In front of this prism a microscope is placed.
Inside the microscope there is a micromatic scale, so
arranged that it can be turned to coincide with the
apparent direction of oscillation of the point of the stile.
In this way not only can the amplitude of the motion of
the stile be measured, but also its azimuth. The extent
of vertical motion is measured by the up and down
motion of the stile due to the elasticity of the supporting

318 EARTHQUAKES,

wire. This instrument is shown in the accompanying
drawing.
: Another apparatus is
~~? the Mvcroseismograph of
Professor Rossi. Here we
havean arrangement which
gives automatic records of
slight motions. It consists
of four pendulums, each
about three feet long, sus-
pended so that they form
the corners of a square
platform. In the centre
of this platform a fifth, but
rather longer, pendulum is
suspended. The four pen-
dulums are each connected
just above their bobs to
the central pendulum with
loose silk threads. Fixed
to the centre of each of
these threads, and held
» bob of pendula; Ppriem; Aeaererape; Verticallyby a light spring,
pr inatol cele: is a needle, so adjusted
that each thread is depressed to form an obtuse angle
of about 155°. These needles form the terminals of an
electric circuit, the other termination of which is a small
cup of mercury placed just below the lower end of the
needle. By a horizontal swing of one of the pendulums
this arrangement causes the needle to move vertica‘ly, but
with a slightly multiplied amplitude. By this motion
the needle comes in contact with the mercury, and an
electro magnet with a lever and pencil is caused to make
a mark on a band of paper moved by clockwork. The

EARTH TREMORS. 319

five pendulums being of different lengths allows the
apparatus to respond ‘to seismic waves of different velo-
cities.’ !

Lastly, we have Professor Rossi’s Microphone. This
consists of a metallic swing arranged like the beam of a
balance. By means of a moveable weight at one end of
the beam this is so adjusted that it falls down until it
comes in contact with a metallic stop. This can be so
adjusted that a slight tap will cause the beam to slightly
jump from the stop. The beam and the stop form two
poles of an electric circuit, in which there is a telephone.
The slightest motion in a vertical direction causes a
fluctuation in the current passing between the stop
and the beam, and a consequent noise is heard in
the telephone.

With instruments analogous to these, observations
have been made by various observers in all portions of
Italy, extending over a period of ten years. Every
precaution appears to have been taken to avoid accidental
disturbances, and the experiments have been repeated in
a variety of forms.

Results obtained in Italy.—The results which from
time to time have been announced are of the greatest
interest to those who study the physics of the earth’s
crust, and they appear to be leading to the establishment
of laws of scientific value.

It would seem that the soil of Italy is in incessant
movement, there being periods of excessive activity
usually lasting about ten days. Such periods are called
seismic storms. These storms are separated by periods
of relative calm. These storms have their greater regu-
larity in winter, and sharp maximums are to be observed
in spring and autumn. In the midst of such a period or

1 Tel. Jowrn., November, 15, 1881.
15

320 EARTHQUAKES.

at its end there is usually an earthquake. Usually these
storms are closely related to barometric depressions. To
distinguish these movements from those which occur
under high pressure, the latter are called baro seismic
movements, and the former vulcano seismic movements.
The relation of these storms to barometric fluctuation has
been observed to have been very marked during the time
of a volcanic eruption.

At the commencement of a storm the motions are
usually small, and one storm, lasting two or three days,
may be joined to another storm. In such a case the
action may be a local one. It has been observed that a
barometrical depression tended to bring a storm to a
maximum, whilst an increase of pressure would cause it
to disappear. Sometimes these actions are purely local,
but at other times they may affect a considerable tract of
land.

If a number of pendulums of different length are
observed at the same place, there is a general similarity
in their movements, but it is also evident that the free
period of the pendulum more or less disturbs the character
of the record. The greatest amplitude of motion in a set
of pendulums is not reached simultaneously by all the
pendulums, and at every disturbance the movement of
one will predominate. From this Rossi argues that the |
character of the microseismical motions is not constant.
Bertelli observed that the direction of oscillationyof the 3
pendulums is different at different places, but each place
will have its particular direction dependent upon the F
direction of valleys and chains of mountains in the neigh- |
bourhood. Rossi shows that the directions of movement
are perpendicular to the direction of lines of faults, the
lips of these fractures rising and falling, and producing
two sets of waves, one set parallel to the line of fracture,

EARTH TREMORS. 321

and the other perpendicular to such a direction. These
movements, according to Bertelli, have no connection
with the wind, rain, change of temperature, and atmo-
spheric electricity.
The disturbances, as recorded at different. towns, are
not always strictly synchronous, but succeed each other at
short intervals. If, however, we take monthly curves of
the disturbances as recorded at different towns in Italy,

Bologna 1874-1875

Rome i874 —1875

Florence 1874-1875

Mallets Curve
6879 Earthquakes

Mean Microsiesmie Curve
for Florence

1872-1876

Fie. 38.

we see that these are similar incharacter. The maximum
of disturbance occurs about the winter solstice, and the
- minimum about the summer solstice, and in this respect
they exhibit a perfect accordance with the curves drawn
by Mallet to show the periodicity of earthquakes. The
accompanying curves taken from one of Bertelli’s original
memoirs not only show this general result but also show

322 EARTHQUAKES.

the close accord there is between the results obtained at
different towns during successive months.

At Florence, before a period of earthquakes there is
an increase in the amplitude and frequency of vertical
movements. These vertical movements do not appear
to coincide with the barometrical disturbances, but they
appear to be connected with the seismic disturbances.

They are usually accompanied with noises in the tele-
phone, but as the microphone is so constructed as to
be more sensitive to vertical motion than to horizontal
motion, this is to be expected. This vertical motion would
appear to bea local action, inasmuch as the accompanying
motions of an earthquake which originates at a distance
are horizontal.

Storms of microseismical motions appear to travel
from point to point.

Sometimes a local earthquake is not noticed in the
tromometer, whilst one which occurred at a distance,
although it may be small, is distinctly observed. To
explain this, Bertelli suggests the existence of nodes.
Similar conclusions were arrived at by Rossi when experi-
menting on different portions of the sides of Vesuvius.
Galli noticed an augmentation in microseismic activity
when the sun and moon are near the meridian. Gra-
blovitz found from Bertelli’s observations a maximum two
or three days before the syzygies, and a minimum three
days after these periods. He also found that the prin-
cipal large disturbances occurred in the middle of periods
separating the quadrature from the syzygies, the apogee
from perigee, and the lunistigi period from the nodes,
whilst the smallest disturbances happened in the middle
of periods opposed to these.

P. C. Melzi says that the curves of microseismical
motions, earthquakes, lunar and solar motions, show a
concordance with each other.

EARTH TREMORS, 323

With the microphone Rossi hears sounds which he
describes as roarings, explosions, occurring isolated or in
volleys, metallic and bell-like sounds, ticking, &c., which,
he says, revealed natural telluric phenomena. Sometimes
these have been intolerably loud. At Vesuvius the ver-
tical shocks corresponded with a sound like volleys of
musketry, whilst the undulatory shocks gave the roaring.
Some of these sounds could be imitated artificially by
rubbing together the conducting wires in the same
manner in which the rocks must rub against each other
in an earthquake. Other sounds were imitated by placing
the microphone on a vessel of boiling water, or by putting
it on a marble slab and scratching and tapping the under
side of it.

These, then, are some of the more important results
which have been arrived at by the study of microseismic
motions. One point which seems worthy of attention is
that they appear to be more law-abiding than their more
violent relations, the earthquakes, and as phenomena in
which natural laws are to be traced they are certainly
deserving our attention. As to whether they will ever
become the means of forewarning ourselves against earth-
quakes is yet problematical. Their systematic study,
however, will enable us to trace the progress of a micro-
seismic storm from point to point, and it is not impossible
that we may yet be enabled to foretell where the storm
may reach its climax as an earthquake. These, I believe,
are the views of Professor di Rossi, who is at the present
time engaged in the establishment of a system of micro-
seismic observations throughout Italy.

Before the earthquake of San Remo (Dec. 6, 1874)
Rossi’s tromometer was in a state of agitation, and similar
disturbances were observed at Livorno, Florence, and
Bologna.

324 EARTHQUAKES,

Since February 1883 I have observed a tromometer
in Japan, and such results as have been obtained accord
with results obtained in Italy. The increase in micro-
seismical activity with a fall of the barometer is very
marked. Other peculiarities in the behaviour of the
instrument will be referred to under ‘ Earth Pulsations.’

Cause of microseismic movements.—As to the cause
of tromometric movements, we have a field for speculation.
Possibly they may be due to slight vibratory motions
produced in the soil by the bending and crackling of
rocks produced by their rise upon the relief of atmospheric
pressure. If this were so we should expect similar move-
ments to be produced at the time of an increase of
pressure. Rossi suggests that they may be the result of
an increased escape of vapour from the molten materials
beneath the crust of the earth, consequent upon a relief
of pressure. The similarity of some of the sounds which
are heard with the microphone to those produced by
boiling water are suggestive of this, and Rossi quotes
instances when underground noises like those which we
should expect to hear from a boiling fluid have been
heard before earthquakes without the aid of microphones.
One instance was that of Viduari, a prisoner in Lima,
who, two days before the shock of 1824, repeatedly pre-
dicted the same in consequence of the noises he heard.

A possible cause of disturbances of this order may be
small but sudden fluctuations in barometric pressure, which
are visible during a storm. During a small typhoon on
September 15, 1881, when in the Kurile Islands, I ob-
served that the needle of an aneroid worked back and forth
with a period of from one to three seconds. This con-
tinued for several hours. With every gust of wind the
needle suddenly rose and then immediately fell. At times
it trembled. These movements were observed in the open

|

EARTH TREMORS. 325

air. The extent of these sudden variations was approxi-.

mately from :03 to ‘05 inches. Reckoning an increase
of barometrical pressure of one hundredth of an inch as
equivalent to a load of twenty million pounds on the square
mile, during this storm there must have been the equiva-
lent of loads of from 60 to 100 million pounds to the square
mile continually placed on and removed from a considerable
tract of the earth’s surface. If the period of application
of these stresses approximately coincide with the natural
vibrational period of the area affected, it would surely
seem, especially when we reflect upon the effect of an
ordinary carriage, that tremors of considerable magnitude
ought to be produced.

An inspection of the following few observations taken
from my note-book for the same typhoon will suggest that
even the large and slower variations are capable of pro-
ducing tremulous motions.

Time Barometer
hy m: reading
12 5 P.M. . * . . : . 29-02
12 40--, ; ° . : : » | & (29105
1 (ST Li ees . : . ° 5 e 29°07
17 12. |, Sih lian Sane init Relate ate Bier a 0018 (94
12 25 ,, BE IUNEIIN E B ES OO ATG
12:50 ,, ra P aa Gs st wave itaddks web pir 2oe00

1,10}, 55 . . . . . . 29:00
120 ,, “ ° ° . : ° 29°07

326 EARTHQUAKES.

CHAPTER XX.

EARTH PULSATIONS.

Definition of an earth pulsation—Indications of pendulums—Indications
of levels—Other phenomena indicating the existence of earth pulsa-
tions—Disturbances in lakes and oceans—Phenomena resultant on
earth pulsations—Cause of earth pulsations.

THE object of the present chapter is to show that from
time to time it is very probable that slow but large wave-
like undulations travel over or disturb the surface of the
globe.

These movements, which have escaped our attention
on account of their coe in period, for want of another
term I call earth pulsations.

The existence of movements such as these may be
indicated to us by changes in the level of bodies of water

like seas and lakes, by the movements of delicate levels,

by the displacement of the bob of a pendulum relatively
to some point on the earth above which it hangs, and by
other phenomena which will be enumerated.

Indication of pendulwms.—Pendulums which have
been suspended for the purposes of seismometrical obser-
vations have, both by observers in Italy and Japan, been
seen to have moved a short distance out from, and then
back to, their normal position.

This motion has simply taken place on one side of
their central position, and is not due to a swing. The

—_— ee -eee

EARTH PULSATIONS. 327

character of these records is such that we might imagine
the soil on which the support of the pendulum had rested
to have been slowly tilted, and slowly lowered. They are
the most marked on those pendulums provided with an
index writing a record of its motions on a smoked glass
plate, which index is so arranged that it gives a multi-
plied representation of the relative motion between it and
the earth. As motions of this sort might be possibly due
to the action of moisture in the soil tilting the support
of the pendulum, and to a variety of other accidental
causes, we cannot insist on them as being certain indica-
tions that there are slow tips in the soil, but for the
present allow them to remain as possible proof of such
phenomena.

Evidence of displacement of the vertical, which are
more definite than the above, are those made by Bertelli,
Rossi, Count Malvasi, and other Italian observers, who,
whilst recording earth tremors, have spent so much time
in watching the vibrations of stiles of delicate pendulums
by means of microscopes. As a result of these observa-
tions we are told that the point about which the stile of
a pendulum oscillates is variable. These displacements
take place in various azimuths, and they appear to be
connected with changes of the barometer. I have made
similar observations in Japan.

From this, and from the fact that it is found that a
number of different pendulums differently situated on
the same area give similar evidence of these movements,

it would hardly seem that these phenomena could be

attributed to causes like changes in temperature and
moisture. M.S. di Rossi lays stress on this point, especially
in connection with his microseismograph, where there are
a number of pendulums of unequal length which give
indications of a like character. The direction in which

- 328 EARTHQUAKES.

these tips of the soil take place—which phenomena are
noticeable in seismic as well as microseismic motions—
Rossi states are related to the direction of certain lines
of faulting.

Indications of levels—Bubbles of delicate levels
can be easily seen to change their position with meteoro-
logical variations ; but Rossi also tells us that they change
their position, sometimes not to return for a long time,
during a microseismic storm. Here again we have another
phenomenon pointing to the fact that microseismic dis-
turbances are the companions of slow alterations in
level.

One of the most patient observers of levels has been
M. Plantamour, who commenced his observations in 1878,
at Sécheron, on the Lake of Geneva. He used two levels,
one placed north and south, and the other east and west.
During the summer of 1878 the east end rose, but at
the end of September a depression set in. The diurnal
‘movements had their maximum and minimum at 6 and
7.45 AM. and P.M. The total amplitude was 4°89”.
The variations of the east and west level appeared to
be due to the temperature, bunt the movements of the
north and south level were dependent upon an unknown
cause.

Between October 1, 1879, and September 30, 1880,
the east end fell rapidly, from the middle of November
up to December 26, amounting to 88°71”. It then rose
6°55” to January 5, and then fell again. On January 28
it reached 89-95”, after which it rose.

Between October 4, 1879, and January 28, 1880,
the movement was 95°8”, against 28°08” of the previous
year.

These movements were not due alone to temperature.
The north and south level, which was not influenced by

win

EARTH PULSATIONS. 329

the cold of the winter, moved 4°56”. In the previous
year 4°89”,!

From February 17 to June 5, 1883, the author ob-
served in Tokio the bubbles of two delicate levels, one
placed north and south, and the other east and west.
They were placed under glass cases on the head of a stone
column. The column, which is inside a brick building,
rests on a concrete foundation, and is about ten years
old. It is in no way connected with the building. The
temperature of the room has a daily variation of about
1° Fahr.

_ In both these levels diurnal changes are very marked.
Occasionally they are enormously great. Thus, on March 25,
the readings of the south end of the north south level were
as follows :—

Time Readings.
h m

25th. 4 00 P.M. e e e e 104:5
i eae BN an re (0
£710", 102
Apo BENS 101
4) BOm 35 100
440 ,, 98
Hel a 99-5
445 ,, 100
Ai50 ,, 101
455 ,, 5 * ‘ “ 101
5 00 5 : : A 100

26th. 7 00 ae : 105

Usually this level moves through aneptt three divisions
per day.

From March 25 to May 4 it travelled from 98 to 127.
Since then, to June 5, it has descended to 116. During
this period the east west level has been comparatively
quiet. One division of the north south level equals about
2” of arc.

1 Minutes and proceedings of the Institute of Civil Engineers, vol. 1x.
p. 412, and vol. lxiv. p. 343.

330 EARTHQUAKES,

Many of these changes may be due to changes in
temperature, variations in moisture, and other local
actions. Some of them, however, are hardly explicable
on such assumptions. The fact that the general direction
in change of the vertical, as indicated by a tromometer
standing on the same column with the levels, showed
that the change which was taking place was rather in the
column than in the instruments.

The fact also that at the time of a barometrical
depression a pulse-like surge can be seen in the levels,
having a period averaging about three seconds and some-
times amounting to about one second of arc, is a pheno-
menon hardly to be attributed to sudden fluctuations in
moisture or temperature, but indicates real changes in
level.! |

In addition to variation in the bubbles of levels
which come on more or less gradually, we have many
recorded instances of sudden alterations taking place in
these instruments.

Examples of what may have been a slow oscillating
motion of the earth’s crust are referred to by Mr. George
Darwin in a Report to the British Association in 1882.

One of them was made by M. Magnus Nyrén, at
Pulkova, who, when engaged in levelling the axis of a
telescope, observed spontaneous oscillation in the bulb of
the level.

This was on May 10 (April 28), 1877. The complete
period was about 20 seconds, the amplitude being 1°5”
and 2’. One hour and fourteen minutes before this he
observes that there had been a severe earthquake at
Iquique, the distance to which in a straight line was
10,600 kilométres, and on an arc of a great circle, 12,500
kilométres. On September 20 (8), in 1867, Mr. Wagner

a See ‘Earth Tremors,’ p. 309, experiments of M. d’Abbadie, &c.

EARTH PULSATIONS. 331

had observed at Pulkova oscillations of 3”, seven minutes
before which there had been an earthquake at Malta.
On April 4 (March 23), 1868, an agitation of the level
had been observed by Mr. Gromadzki, five minutes before
which there had been an earthquake in Turkestan.
Similar observations had been made twice before. These,
however, had not been connected with any earthquakes—
at least, Mr. Darwin remarks—with certainty.

Phenomena analogous to the pendulum and level
observations.—As examples of phenomena which are
analogous to those made on pendulums and levels, the
following may be noticed. On March 20, 1881, at 9 P.M.
a watchmaker in Buenos Ayres observed that all his
clocks oscillating north and south suddenly began to
increase their amplitude, until some of them became
twice as great as before. Similar observations were made
in all the other shops. No motion of the earth was
detected. Subsequently it was learnt that this corre-
sponded with an earthquake in Santiago and Mendoaa.!

Another remarkable example illustrating the like
phenomena is furnished by the observations which were
made on December 21,1860, by means of a barometer in
San Francisco, which oscillated, with periods of rest, for half
an hour. No shock was felt, nor is it likely that it was a
local accident, as it could not be produced artificially. On
the following day, however, a violent earthquake was
experienced at Santiago.’

At the time or shortly after the great Lisbon earth-
quake, curious phenomena were observed in distant
countries, which only appear to be explicable on the
assumption of the existence of earth pulsations.

Thus at Amsterdam and other towns, chandeliers in
churches were observed to swing. At Haarlem water was

1 Metcorologia Endogena. 2 Ibid.

332 EARTHQUAKES.

thrown over the sides of tubs, and it is expressly mentioned
that no motion was perceived in the ground.

At the Hague a tallow chandler was surprised at the
clashing noise made by his candles, and this the more so
because no motion was felt underfoot.

Unusual disturbances vn bodies of water.—At the
time of large earthquakes it would appear that earth
pulsations are produced, which exhibit themselves in
countries where the actual shaking of the earthquake is
not felt, by disturbances in bodies of waters like lakes and
seas.

Some remarkable examples of these disturbances are
to be found in the records of the great Lisbon earthquake.
This earthquake, as a violent movement of the ground,
was chiefly felt in Spain, Portugal, northern Italy, the
south of France and Germany, northern Africa, Madeira,
and other Atlantic islands. In other countries further
distant, as, for instance, Great Britain, Holland, Scandi-
navia, and North America, although the records are
numerous, the only phenomena which were particularly
observed was the slow oscillations of the waters in lakes,
ponds, canals, &c. In some instances the observers
especially remark that there was no motion in the
soil. 7
Pebley Dam, in Derbyshire, which is a large body of

water covering some thirty acres, commenced to oscillate
from the south. A canal near Godalming flowed eight
feet over the walk on the north side.

Coniston Water, in Cumberland, which is about five
miles long, oscillated for about five minutes, rising a yard
up its shores. Near Durham a pond, forty yards long
and ten broad, rose and fell about one foot for six or seven
minutes. There were four or five ebbs and flows per
minute.

EARTH PULSATIONS. 333

Loch Lomond rose and fell through about two and a
half feet every five minutes, and all the other lochs in
Scotland seem to have been similarly agitated.

At Shirbrun Castle, in Oxfordshire, where the water in
some moats and ponds was very carefully observed, it was
noticed that the floods began gently, the velocity then
increased, till at last with great impetuosity they reached
their full height. Here the water remained for a little
while, until the ebb commenced, at first gently, but finally
with great rapidity. At two extremities of a moat about
100 yards long, it was found that the sinkings and risings
were almost simultaneous. The motions in a pond a
short distance from the moat were also observed, and it
was found that the risings and sinkings of the two did
not agree.

During these motions there were several maxima.

These few examples of the motions of waters, without
any record of the motions of the ground, at the time of
the Lisbon earthquake, must be taken as examples of a
very large number of similar observations of which we
have detailed accounts.

Like agitations, it must also be remembered, were
perceived in North America and in Scandinavia, and if
the lakes of other distant countries had been provided
with sufficiently delicate apparatus, it is not unlikely that
similar disturbances would have been recorded.

Besides these movements in the waters of seas and
lakes, at or about the time of great earthquakes, we
have records of like movements, which take place as
independent phenomena.

Thus we read that on October 22, 1755, the waters of
Lake Ontario rose and fell five and a half feet several
times in the course of half an hour.) On March 31,1761,

1 Phil. Trans. vol. xlix. p. 544.

i
ji
f

|

CO ee

334 EARTHQUAKES.

Loch Ness rose suddenly for the period of three quailty
of an hour.!

As another example of the disturbance of water at the
time of a great earthquake in districts where the earth-
quake was not felt, may be mentioned the swelling of the
waters of the Marafion, in 1746, on the night when Callao
was overwhelmed.

Sudden variations in the level of the water have been
many times observed in the North American lakes. The
changes in level which sometimes take place in the
Genfer and Boden lakes are supposed to have some
relation to the condition of the atmosphere. A rising
and falling of especial note took place on April 18, 1855.

In Switzerland these sudden changes are known as
‘seiches’ or ‘rhussen.’

From the observations and calculations of Prof. Forrel
it would seem that the period of the ‘seiches’ depends
upon the dimensions of the lakes; the calculated periods
dependent on the depths of the lakes being approximately
equal to the observed periods.”

W. T. Bingham, writing on the volcanoes of the
Hawaian Islands, remarks that it is not unusual for the sea
to be agitated by great and unusual tides, and that such
sea waves have not been attended with volcanic eruptions
or seismic disturbances. Thus in May 1819 the tide rose
and fell thirteentimes. On November 7, 1837, there was

an ebb and flow of eight feet every twenty-eight minutes.

Again, on May 17, 1841, like phenomena, unaccompanied
by any other unusual occurrences, were recorded.?
Phenomena which may possibly hold a relationship to
earth pulsations are the periodical swellings of the ocean
on the coast of Peru. Dr. C.F. Winslow, who made a long

1 Annual Register, vol. iv. 1761, p. 92.
2 Phil. Mag., May 1876, p. 447. 8 Boston Soc. Nat. Hist., 1868.

ee Te eee ee TS —

i ee P| a a he een ke

EARTH PULSATIONS. 335

period observation upon the coast of Peru, found ‘the highest
tides to prevail at Callao and Paita in December and Jan-
uary,’ and ‘also a series of enormous waves or sea-swells
to be thrown from time to time upon the coast, varying
from twenty-four to twenty-seven hours in continuance,
accompanied by unusual height of the tide during the
same period.’ During June and July the ocean was
unusually tranquil. These phenomena do not appear to
be connected with great atmospheric storms, nor do they
hold any relation to the prevailing wind. They increase
with and accompany the swelling of the tides, and occur
generally, but not always, about full moon.

Sometimes they break suddenly upon the coast.
‘ They are annual and constant in their periodicity,’

The periodical swellings are most noticeable between
Tumbez 3° §.L. and the Chincha Islands 14° S8.L.

These oceanic phenomena synchronise with the
periodic intensity of earthquake phenomena in that part
of the globe, and these with tidal movements.!

Other phenomena sossibly attributable to earth
pulsations.—If we assume that earth pulsations have
an existence, these many phenomena which are otherwise
difficult to understand meet with an explanation. The
curious effects which were produced in the springs at
Toplitz at the time of the Lisbon earthquake may have
been due to a pulse-like wave. The flow of the principal
spring was greatly increased. Before the increase it
became turbid and at one time stopped. Subsequently
it became clear and flowed as usual, but the water was
hotter and more strongly mineralised. Sudden changes
in the flow of underground waters which from time to
time are observed may be attributed to like causes.
Secondary earthquakes such as occurred after the Lisbon

1 “Notes on Tides at Tahiti,’ &c., Am. Jour. Sci. 1866, vol, xlii. p. 45.

336 EARTHQUAKES.

earthquake, as for instance in Derbyshire, may have been
produced by pulsations disturbing the equilibrium of
ground in a critical state.

The falling in of subterranean excavations is also
possibly connected with these phenomena.

Possible causes of earth pulsations.—Mr. George
Darwin, in a report to the British Association (1882), has
shown that movements of considerable magnitude may
occur in the earth’s crust in consequence of fluctuations
in barometrical pressure. (A rise of the barometer over
an area is equivalent to loading that area with a weight,
in consequence of which it is depressed. When the
barometer falls, the load is removed from the area, which,
in virtue of its elasticity, rises to its original position.
This fall and rise of the ground completes a single
pulsation.)

On the assumption that the earth has a rigidity like
steel, Mr. Darwin calculates that if the barometer rises
an inch over an area like Australia, the load is sufficient
to sink that continent two or three inches.

The tides which twice a day load our shores cause
the land to rise and fall in a similar manner. On the
shores of the Atlantic, Mr. Darwin has calculated that
this rise and fall of the land may be as much as 5 inches.
By these risings and fallings of the land the inclination
of the surface is so altered that the stile of a plummet
suspended from a rigid support ought not always to hang
over the same spot. There would be a deflection of the
vertical.

In short, calculations respecting the effects of loads
of various descriptions, which we know are by natural
operations continually being placed upon and removed
from the surface of various areas of the earth’s surface,
indicate that slow pulsatory movements of the earth’s

EARTH PULSATIONS. 337

surface must be taking place, causing variations in
inclination of one portion of the earth’s crust relatively
to another.

Although it is possible that phenomena like the
surging of levels may be attributable to causes like these,
we can hardly attribute the other phenomena to such
agencies.

Rather than seek an explanation from agencies
exogenous to our earth, we might perhaps with advantage
appeal to the endogenous phenomena of our planet.
When the barometer falls, which we have shown corre-
sponds to an upward motion of the earth’s crust, we know,
from the results of experiments, that microseismic motions
are particularly noticeable.

As a pictorial illustration of what this really means,
we may imagine ourselves to be residing on the loosely
fitting lid of a large cauldron, the relief of the external
pressure over which increases the activity of its internal
ebullition—the jars attendant on which are gradually
propagated from their endogenous source to the exterior
of our planet. This travelling outwards would take
place much in the same way that the vibrations con-
sequent to the rattle and jar of a large factory slowly
spread themselves farther and farther from the point
where they were produced.

Admitting an action of this secetauiin 4 to take place,
it would then follow that this extra liberation of gaseous
material beneath the earth’s crust would result in an
increased upward pressure from within, and a tendency
on the part of the earth’s crust to elevation. If we
accept this as an explanation of the increased activity
of a tremor indicator, then such an instrument may be
regarded as a barometer, measuring by its motions the
variations in the internal pressure of our planet.

338 EARTHQUAKES.

The relief of external pressure and the increase of
internal pressure, it will be observed, both tend in the
same direction—namely, to an elevation of the earth’s
crust.

This explanation of the increased activity of earth
tremors, which has also been suggested by M.S. di Rossi, is
here only advanced as a speculation, more probable per-
haps than many others.

We know how a mass of sulphur which has been fused
in the presence of water in a closed boiler gives up in
the form of steam the occluded moisture upon the relief
of pressure. In a similar manner we see steam escaping
from voleanic vents and cooling streams of lava. We also
know how gas escapes from the pores and cavities in a
seam of coal on the fall of the barometrical column. We
also know that certain wells increase the height of their
column under like conditions. The latter of these pheno-
mena, resulting in an increase in the rate of drainage of
an area by its tendency to render such an area of less
weight, facilitates its rise. If we follow the views of Mr.
Mallet in considering that the pressures exerted on the
crust of our earth may in volcanic regions be roughly esti-
mated by the height of a column of lava in the volcanoes
of such districts, we see that in the neighbourhood of a
volcano like Cotopaxi the upward pressures must be enor-
mously great. Further, the phenomena of earthquakes
and volcanoes indicate that these pressures are variable.
Before a volcano bursts forth we should expect that there
would be in its vicinity an upward bulging of the crust,
and after its formation a fall. Further, it is not difficult
to conjecture other possible means by which such pres-
sures may obtain relief.

Should these pressures then find relief without ruptur-
ing the surface, it is not difficult to imagine them as the

EARTH PULSATIONS, 339

originators of vast pulsations which may be recorded on
the surface of the earth as wave-like motions of slow
period.

As an explanation of the strange movements observed
on seas and lakes, Kluge brings forward the following
strange and remarkable theory. The oxygen of the air =
magnetic, whilst water is diamagnetic and the earth mag-
netic: we have, therefore, in our seas and lakes a dia-
magnetic body lying between and being, consequently,
repelled from two magnetic bodies. By variation in tem-
perature, the balance of repulsions exerted by the air and
the earth is destroyed. Thus, by an elevation of tem-
perature the air expands and flows away from the heated
area, where, in consequence, there is less oxygen. The
result of this is, that the repulsion of the air upon the
waters is less than that of the earth upon the waters, and
the waters are in consequence raised up. By a falling of
temperature the waters may be depressed, and by either
of these actions waves may be produced without the in-
tervention of earthquakes or earth pulsations.

The more definite kinds of information which we have
to bring forward, tending to prove the existence of earth
pulsations, too slow in period to be experienced by ordin-
ary observers, are those which appear to ie resultant
phenomena of great earthquakes.

The phenomena that we are certain of in connection
with earth vibrations, whether these vibrations are pro-
duced artificially by explosions of dynamite in bore-holes,
or whether they are produced naturally by earthquakes,
are, first, that a disturbance as it dies out at a given
point often shows in the diagrams obtained by seismo-
graphs a decrease in period; and, secondly, a similar
decrease in the period of the disturbance takes place as
the disturbance spreads.

340 EARTHQUAKES.

As examples of these actions I will quote the following.

The diagram of the disturbance of March 1, 1882,
taken at Yokohama, shows that the vibrations at the
commencement of the disturbance had a period of about
three per second, near the middle of the disturbance the
period is about 1-1, whilst near the end the period has
decreased to°46. That is to say, the backward and forward
motion of the ground at the commencement of the
earthquake was six times as great as it was near the end,
when to make one complete oscillation it took between
two and three seconds. Probably the period became still
less, but was not recorded owing to the insensibility of
the instruments to such slow motions.!

We have not yet the means of comparing together
diagrams of two or more earthquakes, one having been
taken near to the origin, and the other at a distance.
The only comparisons which I have been enabled to make ~
have been those of diagrams taken of the same earth-
quake, one in Tokio and the other in Yokohama. As
this base is only sixteen miles, and the earthquake
may have originated at a distance of several hundreds
of miles, comparisons like these can be of but little
value.

Other diagrams illustrating the same point are those
obtained at three stations in a straight line, but at differ-
ent distances from the origin of a disturbance produced
by exploding a charge of dynamite in a bore-hole. A
simple inspection of these diagrams shows that at the
near station the disturbance consisted of backward and
forward motions, which, as compared with the same dis-
turbance as recorded at a more distant station, were very
rapid. Further, by examining the diagram of the motions,

- 1 Trans. Seis. Soc. of Japan, vol. iv. Milne, Systematic Observation
of Earthquakes.

EARTH PULSATIONS, 341

say, at the near station, it is clearly evident that the
period of the backward and forward motion rapidly decreased
as the motion died out.

These illustrations are given as examples out of a
large series of other records, all showing like results.

An observation which confirms the records obtained
from seismographs respecting the increase in period of an
earthquake as it dies out I have had opportunities of
twice making with my levels. After all perceptible
motion of the ground subsequent upon a moderately severe
shock had died away, I have distinctly seen the bubble
in one of these levels slowly pulsating with an irregular
period of from one to five seconds.

Although we must draw a distinction between earth
waves and water waves, we yet see that in these points
they present a striking likeness. Let us take, for ex-
ample, any of the large earthquake waves which have
originated off the coast of South America, and then
radiated outwards, until they spread across the Pacific, to
be recorded in Japan and other countries perhaps twenty-
five hours afterwards, at a distance of nearly 9,000 miles
from theirorigin. Near this origin they appeared as walls
of water which were seen rapidly advancing towards the
coast. These have been from twenty to two hundred feet
in height, and they succeeded each other at rapid inter-
vals, until finally they died out as a series of gentle waves.
By the time these walls of water traversed the Pacific, to,
let us say, Japan, they broadened out. to a swell so flat
that it could not be detected on the smoothest water
excepting along shore lines where the water rose and fell
like the tide. Instead of a wall of water sixty feet in
height, we had long flat undulations perhaps eight feet in
height, but with a distance from crest to crest of from one
to two hundred miles. wai

342 EARTHQUAKES,

If we turn to the effects of large earthquakes as
exhibited on the land, I think that we shall find records
of phenomena which are only to be explained on the
assumption of an action having taken place analogous —
to that which takes place so often in the ocean, or an
action similar to that exhibited by small earthquakes,
and artificially produced disturbances, if greatly exagge-
rated.

The only explanation for the phenomena accompanying
the Lisbon earthquake appears to be that the short quick
vibrations which had ruined so many cities in Portugal
had, by the time that they had radiated to distant countries,
gradually become changed into long flat waves having a
period of perhaps several minutes. In countries like
England these pulse-like movements were too gentle to be
perceived, except in the effects produced by tipping up
the beds of lakes and ponds.

The phenomenon was not unlike that of a swell pro-
duced by a distant storm. It would seem possible that
in some cases pulsations producing phenomena like the
‘seiches’ of Switzerland might have their origin beneath the
ocean, or deep down beneath the earth’s crust. Perhaps,
instead of commencing with the ‘snap and jar’ of an
earthquake, they may commence as a heaving or sinking
of a considerable area, which may be regarded as an un-
completed effort in the establishment of an earthquake or
a volcano.

From what has now been said it would seem that
earth pulsations are phenomena with a real existence, and
that some of these are attributable to earthquakes. On
the other hand, certain earthquakes are attributable to
earth pulsations. Some of the phenomena which have
been brought forward have only a possible connection
with these movements, and they yet require investigation.

EARTH PULSATIONS. 343

Elastic tides in the earth’s crust have for long been
realities in the minds of physicists. These, however, are
due to lunar and solar influences, and are regular in their
action. The tidal-like movements called pulsations are
of greater magnitude, and their goings and comings are
irregular.

16

344 EARTHQUAKES,

CHAPTER XXI.
EARTH OSCILLATIONS.

Evidences of oscillation—Examples of oscillation—Temple of Jupiter
Serapis— Observations of Darwin —Causes of oscillation.

Evidences of oscillation.—By earth oscillations are
meant those slow and quiet changes in the relative level
of the sea and land which geologists speak of as eleva-
tions or subsidences. These movements are especially
characteristic of volcanic and earthquake-shaken coun-
tries.

As evidences of elevations we appeal to phenomena
like raised beaches, sea-worn caves, raised coral reefs, and
the remains of other dead organisms like barnacles, and
the borings of lithodomous shells in and on the rocks of
many coasts high above the level of the highest tides.
As a proof that subsidence has taken place, there is the
evidence afforded by submerged forests, the prolongation
of certain valleys beneath the bed of the ocean, the
formation of coral islands, the peculiar distribution of the
plants and animals which we find in many countries, and
the submergence of works of human construction. Inas-
much as these phenomena are discussed so fully in many
treatises on physical geology, the references to them here
will be made as brief as possible. Elevations and depres-
sions which have taken place at the time of large earth-

EARTH OSCILLATIONS. 345

quakes in a paroxysmal manner have already been men-
tioned. The movements referred to in this chapter, al-
though generally taking place with extreme slowness, in
certain instances, by an increase in their rapidity, have
approached in character to earth pulsations. In most
instances it would appear that the upward movement of
the ground, which may be likened to a process of tumefac-
tion, goes on so gently that it only becomes appreciable
after the lapse of many generations.

Examples of movements.—Lyell estimated that the
average rate of rise in Scandinavia has been about two and a
half feet per century. At the North Cape the rise may have
been as muchas five or six feet per century. Observations
made at the temple of Jupiter Serapis, between October
1822 and July 1838, showed that the ground was sinking
at the rate of about one inch in four years. Since the
Roman period, when this temple was built,the ground has
sunk twenty feet below the waves. Now the floor of the
temple is on the level of the sea. Lyell remarks that if
we reflect on the dates of the principal oscillations at this
place there appears to be conneetion between the move-
ments of upheaval and a local development of volcanic
heat, whilst periods of depression are concurrent with
periods cf volcanic quiescence.!

As examples of movements even more rapid than those
at the Temple of Jupiter Serapis we refer to an account
of the earthquakes in Vallais (November 1755), when
the ground about a mountain at a small distance from
Brigue sank about a thumb’s-breadth every twenty-four
hours. This took place between December 9 and Feb-
ruary 26.”

Another remarkable example of earth movement is

1 Principles of Geology, vol. ii. 177.
® Gent. Mag., vol. xxvii. p. 448.

2

346 EARTHQUAKES,

given in the account of the earthquake at Scarborough, on
December 29,1737, when the head of the spa water well
was forced up in the air about ten yards high. At this
time the sands on the shore are said to have risen so slowly
that people came out to watch them.!

Two other examples of rapid earth movement are
taken from Professor Rossi’s ‘Meteorologia Endogena.’
Professor D. Seghetti, writing to Professor Rossi, says that
a few lustres ago (one lustre=twenty years) Mount S.
Giovanni hid the towns Jenne and Subiaco from each
other. From Subiaco the church at Jenne is now visible,
which a few years ago was invisible. The people at
Jenne also can see more than formerly. The supposition
is that the side of Mount S. Giovanni is lowered. This
fact corresponds to a fact stated by Professor Carina, who
says that forty or fifty years ago from Granaiola you could
not see. either the church of 8. Maria Assunta di Citrone
or the church of S. Pietro di Corsena. Now you can see
both.?

For a remarkable example illustrating the connection
between seismic activity and elevation we are indebted
to the patient labours of Darwin, who carefully investi-
gated the evidences of elevation which are visible upon
the western coasts of South America. These evidences,
consisting of marks of erosion, caves, ancient beaches,
sand dunes, terraces of gravel, &c., were traced between
latitudes 45° 35’ to 12° 5’, a distance north and south of
2,075 geographical miles, and there is but little doubt
that they extend much farther. As deduced from
observations upon upraised shells alone, a summary of
Mr. Darwin’s observations are contained in the following
table :— .

1 Phil. Trans., vol. xli. p. 805.
2 Meteorolegia Endogena, vol. i. pp. 186, 187.

EARTH OSCILLATIONS. 317

At Chiloe the recent elevation has been - ‘ 4 350

» Concepcion ‘3 ‘ . 625 to 1,000
» Valparaiso 5 = - : a L360
:, Coquimbo j = . : - 252
” Lima ” 9 . . e 85

Shells, similar to those clinging to uplifted rocks,
which are evidences of these elevations, still exist in the
neighbouring seas, and in the same proportionate numbers
as they are found in the upraised beds. In addition to
this, Mr. Darwin shows us that at Lima, during the Indo-
human period, the elevation has been at least eighty-five
feet. At Valparaiso, during the last 220 years, the rise
was about nineteen feet, and in the seventeen years sub-
sequent to 1817 the rise has been ten or eleven feet, a
portion only of which can be attributed to earthquakes.
In 1834 the rise there was apparently still in progress.

At Chiloe there has been a gradual elevation of about
four feet in four years. These, together with numerous
other examples, testify to the gradual but, as compared
with other parts of the globe, exceedingly rapid rise of
the ground upon the western shores of South America.!
The most important point to be noticed is that this
district of rapid elevation is one of the most earthquake-
shaken regions of the world. And further, judging from
Darwin’s remarks, in those portions of it where the move-
ments have been the most extensive, and at the same time
probably the most rapid, the seismic disturbances appear
- to have been the most noticeable.

Similar remarks may be applied to Japan, it being
in those districts where evidences of recent elevation are
abundant that earthquakes are numerous. Thus, in the
bay of Yedo, where we have borings of lithodomi in the
tufaceous cliffs ten feet above high-water mark, which,

1 Darwin, Geological Observations, p. 275 et seg.

348 EARTHQUAKES,

inasmuch as the rock in which they are found is soft and
easily weathered, indicate an exceedingly rapid elevation,
earthquakes are of common occurrence.

From the evidences of elevation which we have upon
the South American coast, Japan, and in other countries,
it appears that these movements are intermittent, there
being periods of rest, when sea cliffs are denuded, and
perhaps even periods of subsidence. There is also evi-
dence to show that, although these movements have been
gradual from time to time, they have been aided by
starts occasioned by earthquakes.

As to whether earthquakes are more numerous during
periods of elevation, or of subsidence, or during the inter-
mediate periods of rest, we have no evidence.

Sudden displacements which occasionally accompany

earthquakes might, it was said, sometimes be regarded as
the cause of an earthquake, and sometimes as the effect.
_ The slow elevations here referred to may be looked
upon as being one of the more important factors in the
production of earthquakes. By various causes the rocky
coast is bent until, having reached the limit of its elas-
ticity, it snaps, and, in flying back like a broken spring,
causes the jars and tremors of an earthquake.

If this is the case, then the number of earthquakes
felt in a district which is being elevated may possibly be
a function of the rate of elevation.

APPENDIX.

—_*o—

List oF THE PrincrpAL Books, Papers, PERIODICALS, WHICH
ARE REFERRED TO IN THE PRECEDING PAGES.

For a more complete bibliography of earthquakes refer to Mallet’s
catalogue of works given in his report to the British Association in
1858.

A True and Particular Relation of the Dreadful Earthquake which
happened at Lima, &c. (1746). 1768.

Abbot, Gen. H. L. On the Velocity of Transmission of Earth Waves.
Am. Jour. Sct. XV., March 1878.

— Shock of the Explosion at Hallet’s Point, Nov. 14, 1876. Batta-
lion Press.

Alexander, Prof. T. See Trans. Seis. Soc. of Japan.

American Journal of Science.

Annali del reale osservatorio meteorologico Vesuviano.

Annual Register, The.

Anonymous, A Chronological and Historical Account of the most
Memorable Earthquakes in the World, &e. 1750.

— A Vindication of the Bishop of London’s Letter occasioned by
the Late Earthquake. 1750.

— Phenomena of the Great Earthquake of Nov. 1, 1755.

— Serious Thoughts occasioned by the Late Earthquake at Lisbon.
1755.

Asiatic Society of Japan, Transactions of.

Ayrton, Prof. W. E. See Perry, J.

Barceno, M. Estudio del Terremoto (May 17, 1879) Mexico. 1879.
Beke, Dr. C. T. Mount Sinai a Volcano.

390 APPENDIX.

' Bissett, Rev. J. A Sermon (on account of the Earthquake at Lisbon,
Nov. 1, 1755). 1757.

Bittner, A. Beitraige zur Kenntniss des Erdbebens von Belluno vom
29, Juni 1873.

— Sitzungsb. der K. Akad. d. Wissensch., Ixix. II. Abth., 1874.

Bollettino del Vulcanismo Italiano.

Boué, Dr. A. Ueber das Erdbeben welches Mittel-Albanien im
October d. J. so schrecklich getroffen hat. Die K. Akad. d.
Wissenschaften, Nov, 1851.

— Parallele der Erdbehen, des Nordlichtes und des Erdmagnetismus.

— Ueber die Nothwendigkeit die Erdbeben und vulcanischen Er-
scheinungen genauer als bis jetzt beobachten zu lassen. Dre K.
Akad. d. Wissenschaften, 1851 and 1857.

Bouguer, M. Of the Volcanoes and Earthquakes in Peru.

British Association, Reports of. .

Brunton, R. H. Constructive Art in Japan. Trans. Asiatic Soc. of
Japan, II. and IIL, Pt. 2.

Bryce, J. Report to British Association, 1841.

Buffour, M. The Natural History of Earthquakes and Volcanoes.

C.H. A Physical Discussion of Earthquakes, &e. 1693.

Canterbury, Thomas, Lord Archbishop of. The Theory and History
of Earthquakes.

Casariego, E. A. See Trans. Sets. Soc. of Japan.

Cawley,G. Some Remarks on Construction in Brick and Wood, &e.
Trans. Asiatic Soc. of Japan, VI. Plate ii.

Chaplin, Prof. W.S. An Examination of the Earthquakes recorded
at the Meteorological Observatory, Tokio. Trans. Astatie Soe.
of Japan, VI. Part ii.

Comptes Rendus.

Credner, H. Das Dippoldiswalder Erdbeben vom Oktober 1877.

— Zeitschr. f. d. Naturwiss. f. Sachsen u. Thiiringen.

— Das Vogtlindisch-erzgebirgische Erdbeben, 23. Nov. 1875.

— Zeitschr. f. d. gesammt. Naturwissenschaften, xlviil., Oktober.

Dan, T. See Trans. Seis. Soc. of Japan.

Darwin, Charles. Researches on Geology and Natural History.

— Geological Observations.

Darwin, G. H. Reports on Lunar Disturbance of Gravity to British
Association, 1881. 1882.

APPENDIX. 351

Diffenbach, F, Plutonismus und Vulkanismus in der Periode von
1868-1872, und ihre Beziehungen zu den Erdbeben im Rheinge-
biet.

Doelter, C. von. Ueber die Eruptivgebilde von Fleims, nebst einigen
Bemerkungen tiber den Bau alterer Vulcane.

— lxxiv. Band d. Sitzungsb. d. K. Akad. d. Wissensch., ¥. Abth.,
Dec. Heft, Jahre. 1876.

Doolittle, Rev. T. Earthquakes eee rer eee and Practically Improved,
&e. 1693.

Doyle, P. See Trans. Seis, Soc. of Japan.

Emerson, Prof., B.A. Review of Von Seebachs’ Earthquake of
March 6, 1872. Am. Jour. Sct., Series IIT.

_ Ewing, Prof. J. A. Earthquake Measurement, A memoir published
by the Tokio University. 1883.

— See Trans. Seis. Soc. of Japan.

Falb, R. Gedanken und Studien tiber den Vulcanismus, &e. 1875.

— Grundziige zu einer Theorie der Erdbeben und Vulkanausbriiche.

— Das Erdbeben von Belluno. ‘Sirius,’ Bd. VI1.,-Heft ii.

Flamstead, J. A Letter concerning Earthquakes. 1693.

Forel, F. A. Les Tremblements de Terre (Suisse). Azch. des Sciences
Physiques et Naturelles, VI. p. 461.

— Tremblement de Terre du 30 Décembre 1879.

Fuchs, Karl. Vulkane und Erdbeben.

— Die Vulkanischen Erscheinungen der Erde.

Garcia, J.C. See Trans. Ses. Soc. of Japan.

Geinitz, Dr. E. Das Erdbeben von Iquique am 9. Mai 1877, &c.
Die K. Leop.-Carol.-Deutschen Akademie der Naturforscher,
Band xl., Nr. 9.

Gentleman’s Magazine, The.

Geographical Society, Proceedings of.

Geological Society, Proceedings of.

Girard, Dr. H. Ueber Erdbeben und Vulkane. 1845.

Gray, T. See Trans. Seis. Soc. of Japan.

— On Instruments for Measuring and Recording Earthquake Motions.
Phil. Mag. Sept. 1881.

— On Recent Earthquake Investigation. The Chrysanthemum, 1881.

Guiscardi, Prof. G. Notizie del Vesuvio. 1857.

— Il terremoto di Casamicciola del 4 Marzo. 1881.

352 APPENDIX.

Hales, $., D.D., F.R.S. Some Considerations on the Causes of Earth-
quakes. 1750,

Hamilton, Sir W. Observations on Mount Vesuvius, Mount Etna,
&e. 1774.

Hattori, I. Destructive Earthquakes in Japan. Trans. Asiatic Soe.
of Japan, V. Plate i.

Heim, Prof. A. Les Tremblements de Terre et leur Etude Scientifique.
1880. .

— Prof. A. Die Schweizerischen Erdbeben in 1881-1882.

Hoeffer, Prof. H. Die Erdbeben Karntens und deren Stosslinien.
Die Kais. Akademie d. Wissenschaften, Band xlii.

Hofer, Prof. H. Das Erdbeben von Belluno, am 29. Juni 1873.
Sitzungsb. der K, Akad. d. Wissensch., I. Abth., Band Ixxiv.
Hoff, K. E. A. von. Geschichte der durch Ueberlieferung nachgewie-

senen natiirlichen Verinderungen der Erdoberflache. 1822.
Hooke, R., M.D., F.R.S. Discourses concerning Earthquakes.
Hopkins, William. Report to the British Association on the Geolo-

gical Theories of Elevation and Earthquakes. 1847.

Horton, Rev. Mr. An Account of the Earthquake which happened

at Leghorn in Italy (Jan. 1742). 1750.

Humboldt, Alexander yon. Cosmos.
— Travels.

~Jeitteles, L. A. Bericht iber das Erdbeben am 15. Januar 1858.

— Sitzunysberichte der mathem.-naturw. Classe d. K. Akad. d.
Wissensch., xxxv. 8. 511.

Judd, J. W., Prof. Volcanoes, What they Are and What they Teach.

Knipping, E. Verzeichniss von Erdbeben wahrgenommen in Tokio,
&e. Mitt. d. Deutsch. Gesellsch. fur eos und Volkerkunde
Ostasiens, Heft 14.

— See Trans. Sets. Soc. of Japan.

Lasaulx, A. von. Das Erdbeben von Herzogenrath am 22. October
1873.

Lemery, M. A Physico-Chemical Explanation of Subterranean Fires,
Earthquakes, &c.

Lescasse, M. J. Etude sur les Constructions Japonaises, &c, Mé-
mowres de la Société des Ingénieurs Civils.

Lister, M., M.D., F.R.S. Of the Nature of Earthquakes.

Little, Rev. J. Conjectures on the Physical Causes of Earthquakes
and Volcanoes. 1820.

APPENDIX. 353

Mallet,R. The Neapolitan Earthquake, Vol. IL. Reports tothe British
Association, 1850, 1851, 1852, 1854, 1858, 1861.

— Secondary Effects of the Earthquake of Cachar. Proc. Geolog.
Soc., 1872.

— Dynamics of Earthquakes. Trans. Ruyal Irish Acad. 1846.

Michell, Rev. J. Conjectures Concerning the Cause and Observations

-. upon the Phenomena of Earthquakes. 1760.

Milne, David. Reports to British Association, 1841, 1848,
1844.

Milne, John. See Jrans. Seis. Soc. of Japan.

— On Seismic Experiments (with T. Gray, B.Sc., F.R.S.E.) Trans.
Royal Soc. 1882.

— On Seismic Experiments (with T. Gray, B.Sc., F.R.S.E.) Proc.
Royal Soc. No. 217, 1881.

— Earthquake Observations and Experiments in Japan (with T. Gray,
B.Sc., F.R.S.E.) Phil. May., Nov. 1881.

— On the Elasticity and Strength Constants of certain Rocks (with

‘7. Gray, B.Sc., F.R.S.E.) Jour. Geolog. Soc., 1882.

— A Visit to the Volcano of Oshima. Geolog. Mag., Dec. 2, Vol.
IV., pp. 193-197, 255.

— On the Form of Volcanoes. Geolog. Mag., Dec. 2, Vol. V., and
Dec. 2, Vol. VI.

— Note upon the Cooling of the Earth, &c. Geology. Mag., Dec.
2>Vol.. VII., p. 99.

— Investigation of the Earthquake Phenomena of Japan. Rep. Brié.
Assoc., 1881 and 1882.

— A Large Crater. Popular Science Review.

— The Volcanoes of Japan (a series of Articles), Japan Gazette.

— Earthquake Literature of Japan (a series of Articles), Japan
Gazette.

— The Earthquake of Dec. 23, 1880. The Crysanthemum, 1881.

— Earthquake Motion. Zhe Crysanthemum, 1882.

— Seismology in Japan. Nature, Oct. 1882.

— Earth Movements. Zhe Times, Oct. 12, 1882.

Mohr, Dr. F. Geschichte der Erde. 1875.

Naturkundig Tijdschrift voor Nederlandsch Indie. 1875-1880.

Naumann, Dr. E. Ueber Erdbeben und Vulkanausbriiche in Japan.
Mitt. d. Deutsch. Geselisch. fiir Natur- und Volkerkunde Ostastens,
Heft 15.

354 APPENDIX.

Noggerath, Dr. J. Die Erdbeben vom 29. Juli 1846 im Rheingebiet, &c.

— Die Erdbeben im Vispthale (1855).

— Die Erdbeben im Rheingebiet in den Jahren 1868, 1869, 1870.

— Jahrgiinge d. Verhandlungen d. Natur. Vereins fiir 1870. Rhezn-
land u. Westphalen, xxvii. .

Oldham, Dr. Secondary Effects of the Earthquake of Cachas. Proc.
Geolog. Soc. 1872.

— Thermal Springs of India. Memoirs of Geolog. Survey of India,
XIX. Plate 2.

— A Catalogue of Indian Earthquakes. Memoirs of Geolog. Survey
of India, XIX. Plate 3.

— The Cachas Earthquake. Memoirs of Geolog. Survey of India.
XIX. Plate 1.

Palmer, Col. H. 8. See Trans. Sevs. Soc. of Japan.

Palmieri, Prof. L., e Scacchi, A. Della Regione Volcanica del Monte
Vulture, e del Tremuoto ivi avvenuto nel di 14 Agosto 1851.
1852,

— Annali del reale Osservatorio Meteorologico Vesuviano.

— J! Vesuvio, il Terremoto d’ Isernia e l’eruzione sottomarina di
Santorino. RR. Accad. d. Sci. Fis. e Mat. di Napoli, iv. 1866.

— Sul recente Terremoto di Corleone. R. Accad. d. Sct. Fis. e Mat.,
v. 1876.

— TI Terremoto di Scio del di 4 Aprile. R. Accad. d. Sci. Fis. e
Mat. di Napol. v. 1881.

— Sul Terremoto di Casamicciola del 4 Marzo 1881. R. Acead. d.
Sct. Fis. e. Mat. di Napoli. 1881.

Paul, Prof. H. M. See Z7ans. Seis. Soc. of Japan.

Perrey, Prof. A. Harthquake Catalogue and Memoirs. (For list see
Mallet’s Report to British Association. 1858.)

— See Trans. Seis. Soc. of Japan.

Perry, J.,and W. E. Ayrton. Ona Neglected Principle that may be
Employed in Earthquake Measurement.

— See Zrans. Seis. Soc. of Japan.

Philosophical Magazine.

Pickering, Rey. R. An Address to those who have either retired
or intend to leave Town under the Imaginary Apprehension of
the Approaching Shock of another Earthquake. 1750.

Ray, J., F.R.S. A Summary of the Causes of the Alterations which
have happened to the Face of the Earth.

pO ee

APPENDIX. 355

Rockstroh, E. Informe de la Comision Cientifica del Instituto
Nacional de Guatemala, nombrada por el Sr. Ministro de In-
struccion Publica para el Estudio de los Fenédmenos Volcanicos
en el Lago de Tlopango. 1880.

Rockwood, Prof.C.G. Notes on Earthquakes. Annually in the Am.
Jour. Sct.

— Japanese Seismology. Am. Jour. Sci., XXII. Dec. 1881.

Romaine, W. A Discourse occasioned by the Late Earthquake.
1755.

Rossi, Prof. M. 8, di. Intorno all’ odierna fase dei Terremoti in
Italia, esegnatamente sul Terremoto in Casamicciola del 4 Marzo
1881. Socteta Geografica Italiana. 1881.

— La Meteorologia Endogena, 2 vols.

Royal Society, Transactions of.

Scacchi, A. See Palmieri.

Schmidt, Dr. J. F. Untersuchungen tiber das Erdbeben am 15. Januar
1858,

— Studien iiber Erdbeben. 1879.

— Die Eruption des Vesuv (1855). 1856.

Scrope, G. P. Volcanoes.

Seebach. Das mittle Deutsche Erdbeben (1872). Mitt. der K.K.
geograph. Gesellsch., Il. Jabrg., 2. Heft, 1873.

Serpieri, Prof. A.C. S. Nuove Osservazioni sul Terremoto avvenuto
in Italia il 12 Marzo 1873. Istituto Lombardo. 1873.

— Il Terremoto di Rimini della notte 17-18 Marzo 1875,

— Documenti nuove e Riflessioni sul Terremoto della notte 17-18
Marzo 1875. Meteorologia Italiana, iv. 1875.

— Determinazione delle fasi e delle leggi del grande Terremoto
ayvenuto in Italia nella notte 17-18 Marzo 1875. Istituto
Lombardo. 18785.

— Dell’ influenza del Lume Solare sui Terremoti. Istztuto Lombardo.
1882,

Sherlock, T., D.D. (Lord Bishop of London). A Letter on the
occasion of the late Harthquakes. 1750.

Shower, Rey. J.,D.D. Practical Reflections on the Earthquakes that
have er pened i in Europe and America, &c. 1750.

Stiibel, A. (see Reiss, W.)

Stukeley, Rev. W., M.D., F.R.S. The Philosophy of Earthquakes,
Natural and Religious, &c. Plates 1,2, and 3. 1756,

Sturmius, J.C. A Methodical Account of Earthquakes.

356 APPENDIX.

Suess, E. Die Erdbeben Niederésterreiches. Die Kats. Akademie
der Wassenschaften, Bd. xxxiii. .

— Die Erdbeben des stidlichen Italiens. Die Kais. Akademie der
Wissenschaften, Bd. xxxiv.

Volger, Dr. G. H. Untersuchungen iiber das Phinoman der Erdbeben.
J&57.

Wagener, Dr. G. Bemerkungen iiber Erdbebenmesser und Vor-
schlige zu einem neuen Instrumente dieser Art. Mvtt. d. Deutsch.
Gesellsch, fiir Natur- und Volkerkunde Ostasiens, Heft 15.

— See Trans. Sets. Soc. of Japan.

Winchilsea, The Earl of. A True and Exact Relation of the late
Prodigious Earthquake and Eruption of Mount Etna. 1669.
Woodward, J., M.D., F.R.S. Earthquake caused by some Actideatet

Obst ee of 2 Continual Subterranean Heat.

SEISMOLOGICAL SOCIETY OF JAPAN.
The following are a list of the papers published by this Society :—
VOL. I.

Milne, J. Seismic Science in Japan. 385 pages.

Ewing, J. A. New Form of Pendulum § eismograph. 6 pages,
3 plates.

Gray, T. Seismometer and Torsion Pendulum Seismograph. 8 pages,
2 plates.

Mendenhall, T. C. Acceleration of Gravity at Tokio (abstract).
2 pages.

Wagener, G., and E. Knipping. New Seismometer and Obervations
with same. 18 pages, 1 plate.

Milne, J. Earthquake in Japan of Feb. 22, 1880. 116 pages,
5 plates, 8 woodcuts.

VOL. II.

Milne, J. Recent Earthquakes of Yeddo, Effects on Buildings, &e.
38 pages, 2 plates, and many tables.

Mendenhall, T. C. Gravity on Summit of Fujiyama (abstract).
2 pages.

Paul, Hi M. Earth Vibrations from Railroad Trains (abstract).
4 pages.

Ewing, J. A. Astatic Horizontal Lever Seismograph (abstract).
5 pages, 1 plate,

ee a

APPENDIX. 357

Milne, J. Peruvian Earthquake of May, 9,1877. 47 pages, 2 plates,
tables. Constitution, Rules, Officers and Members of the Society,
Dec., 1881.

VOT. IIT. )

Gray, T. Steady Points for Earthquake Measurements. 11 pages,
3 plates.

Milne, J. Experiments in Observational Seismology. 953 pages,
1 plate, tables.

— The Great Earthquakes of Japan. 38 pages, 1 plate, many tables.

Perry, J. Theory of a Rocking Column. 4 pages.

Knipping, E. Earthquake of July 25, 1880, with Dr. Wagener’s
Seismometer. 4 pages.

Ewing, J. A. Earthquake Observation at three or more Stations,
&e. 4 pages.

— Records of three recent Earthquakes. 6 pages, 3 plates.

— Earthquake of March 8, 1881. 8 pages, 1 plate.

Milne, J. Horizontal and Vertical Motion in Earthquake of March 8,
1881. 8 pages, 3 plates.

Gray, T. Seismograph for Registering Vertical Motion. 3 pages,
I plate.

Ewing, J. A. Seismometer for Vertical Motion. 3 pages, 1 plate.

Gray, T. Seismograph for Large Motions. 2 pages.

— Compensating a Pendulum to make it Astatic. 3 pages.

Palmer, H.S. Note on Earth Vibrations. 3 pages.

Kuwabara, M. The Hot Springs of Atami. 2 pages.

VOL. IV.
Milne, J. Distribution of Seismic Activity in Japan. 30 pages,
1 plate.
Wada, T. Notes on Fujiyama. 7 pages.
Casariego, E. Abella y. Earthquakes of Nueva Vizcaya in 1881.
23 pages, 2 maps.
Milne, J. Utilisation of Earth’s Internal Heat. 12 pages.
Ewing, J. A. Earthquake of March 11,1882. 5 pages.
Doyle, P. Note on an Indian Earthquake. 6 pages.
Milne, J. Systematic Observation of Earthquakes. 31 pages, 5 plates.

VOL. V.
Naumann, Dr. E. Notes on Secular Changes of Maenetic Declination
in Japan. p. 1-18.
Casariego, Don E. Abella y. Monografia Geoldgica del Volcan de
Albay 6 El Mayon. p. 19-43.

358 APPENDIX.

Garcia, Don J. Centeno y. Abstract of a Memoir on the Earth-
quakes on the Island of Luzon in 1880. p. 45-89.

Ewing, Prof. J. A. Seismological Notes.

— A Duplex Pendulum Seismometer.

— The Suspension of a Horizontal Pendulum.

— A Speed Governor for Seismograph Clocks. p. 89-95.

Dan, T.,S.B. Notes on the Earthquake at Atami, in the Province
of Idzu, on September 29, 1882. p. 95-105.

VOL. VI.

Alexander, Prof. T. The Development of the Record given by a
Bracket Machine.

Milne, J. Earth Pulsations.

Ewing, J. A. Note on a Duplex Pendulum with a Single Bob.

Gergens, F. Note on an Iron Casting, Supposed to have been Dis-
turbed whilst Cooling by an Earthquake.

West, C.D. Ona Parallel Motion Seismograph.

Ewing, J. A. Certain Methods of Astatic Suspension.

Alexander, T. Ball and Cup Seismometer.

Knipping, Messrs. Paul and. Report on a System for Earthquake

Observation.
Catalogues of Earthquakes.

ae eee ia e

EN DE Xx.

ee Ok

ABB

ABBADIE, M. d’, on earth tremors,
309

Abbot, General H. L., on the trans-
mission of vibrations, 62

Abella, M., on the earthquake in
the Philippines in 1881, 77

Activity, on seismic, 6

Aristotle, on the classification of
earthquakes, 41

Artificial earthquakes, experi-
ments on, 57

— — intensity of, 61

Aurora, on the occurrence of, with
earthquakes, 264

Ayrton and Perry, on the effect of
soft foundations, 130

— — on the period of vibration of
buildings, 115

— — on the principle of, 31

BAROMETER, effect of changes of,
on earthquakes, 266

Bertelli, on aurora and earth-
quakes, 265

— on earth tremors, 316, 320

—on the normal tromometer of,
317

Bittner, A., on the buildings of
Belluno, 100

Bridges, on earthquake, 140

Brunton, R. H., on buildings in
earthquake countries, 123

Buckle, on the history of civilisa-
tion, 1

Builders, interest of the study of
earthquakes to, 3

CEN

Buildings, on cracks in, 98, 108

— the effect of earthquakes on
96

— on the irregular destruction of,
96

— — effect on the end house in
a row, 112

— — church of St. Augustine at
Manilla, 113

— — relation of destruction of, to
earthquake motion, 103

— — protection of, 143

-— — pitch of the roof of, 110

— — position of openings in the
walls of, 111

— — swing of, 115

— — period of vibration of, 115

— — principle of relative periods
in, 116

—-—types of, for earthquake
countries, 121

— — effect of underlying rocks
on, 130

— general conclusions regarding,
144

CACCIATORE, definition of the, 18

Caldcleugh, A.,on earthquake fre-
quency, 245

— onbarometric height and earth-
quakes, 266

Carruthers, J., on earthquakes
and tides, 291

Centrum, definition of, 9

— on the depth of, 213

— on the maximum depth of 218

360 | INDEX.

CEN

Centrum, dete m ‘nation of position
of, see origirs

Chaplin, W. S., on the bracket
seismometer of, 27

— on earthquakes and the posi-
tion of the moon, 252

Coast line, on the movement of,
160

Cocks, R., on earthquakes and
tides, 290

Coseismic lines, definition of, 10

Curves, on microseismic, 321

DARWIN, Charles, on the move-
ment of coast. lines, 160

— George H., on earth tides, 285

— on tidal loads, 291

— on earth pulsation, 330

— on the effect of fluctuations of
barometric pressure, 336

— experiments at Cambridge, 310

Delauney, M. J., on the influence
of the planets on earthquakes,
261

Diagonic, definition of, 11

Diastrophic, definition of, 11

Direction of motion, from instru-
mental records, 198

Distribution, on earthquake, 226

— examples of, 231

Disturbance, on the propagation
of, 50

Douglas, J.. on South American
houses, 126

EARTH-PARTICLE, on the velocity
and acceleration of, 79

Earthquake motion, nature of, as
deduced from the feelings, 67

— direction of, derived from in-
strumental records, 69

— duration of, 71

— period of vibration in, 74

— examples of extent of, 75-77

— absolute intensity of force in,
83

— radiation of, 85

— velocity of propagation of, 87

FUC

Earthquake at Lisbon, velocity
of propagation of, 88

Earthquakes, general examples of
effects of, 142

— geological changes produced
by, 161

— hunting, 187

— distribution of, 226

— maps, 189

— secondary, 248

— table of, for nineteenth century,
259

— on the course of, 277-281

— and tides, 290

— prediction of, 297-304

Elastic waves, nature of, 44

Emergence, angle of, 9

Energy, dissipation of, in earth-

quakes, 52

— seismic, in relation to geologi-
cal time, 234 ’

— — table of, 240

Epicentrum, definition of, 9

Euthutropic, definition of, 11

Ewing, J. A., pendulum seismo-
graph of, 25

— astatic pendulum of, 26,

— bracket seismograph of, 26

FALB, R., on the influence of the
sun and moon on earthquakes,
286

Fissures, on the material dis-
charged from, 148

— on the explanation of, 151

Focal cavity, definition of, 9

— on the form of, 221 :

Forbes, D., on an earthquake in
Mendoza, 151

Frequency of earthquakes, 243

Frere, Sir H. Bartle, on geologi-
cal changes produced by earth-
quakes, 161

Fuchs, on sea waves, 176

—- on the movement of theseismic
centre, 223

— on earthquakes and volcanic —

outbursts, 271
— on hot springs, 157

ee ee

FUM

Fumaroles, the effect of earth-
quakes on, 156

GEINITZ, Dr., on sea waves, 182

Geologists, on the interest of seis-
mology to, 2

Gray, T., astatic pendulum of, 26

— bracket seismometer of, 27 |

_-- conical pendulum of, 29

— dead heat pendulum of, 22

— on the rotation of bodies, 196

— rolling spheres and cylinders
of, 29

— torsion pendulum seismometer
of, 25

— vertical motion seismometers
of, 32, 33

— and Milne, seismograph of, 38

HATTORI, I., on the large earth-
quakes of Japan, 244

Haughton, Prof., list of active
volcanoes of, 227

— method of finding earthquake
origins of, 209

Hills, on the want of support on
the face of, 136

Hofer, on an earthquake at Bel-
luno, 225

Hoffman, F., on the barometer
and earthquakes, 267

Hooke, on earthquake motion, 42

Hopkins, on the thickness of the
earth’s crust, 284

Humboldt, on meteors and earth-
quakes, 261

— on the barometer and earth-
quakes, 267

—on volcanoes and earthquakes,
279

IMAGINATION, effect of earth-
quakes on the, 2
Instruments, direction of motion
derived from, 198
Intensity, on earthqvake, 51, 71
/ — seismic curve of, for Kioto, 242

INDEX. 361

MAL

Isoseismic circles, definition of, 10
— areas, definition of, 10

KLUGE, on sea waves, 175

— on earthquake frequency, 246

—on simultaneous earthquakes,
248

— on earthquakes and sun spots,
263

— on earth pulsations, 339

Kreil, pendulum seismometer of,
25

LAKES, on disturbances in, 154

Land, effect of earthquakes on,
146-162

— on the reason of movements of,
162

— on cracks and fissures formed
in, 146

Level, on the use of for earth pul-
sations, 328

Literature, on seismic, 6

— on Japanese earthquake, 7

MALLET, R., on area of disturb-
ance as a test of seismic energy,
78

— on clock stopping, 36

— list of works on earthquakes of,

— curve of seismic energy of, 238

— definition of earthquake of, 43

— on earthquake frequency, 243

— on the influence of the heavenly
bodies on earthquakes, 253

—on maximum depth of origin,
218

— on pendulum seismometers, 20

— projection seismometer of, 17

-— on the Neapolitan earthquake,
69, 77, 83, 97, 103, 132, 142, 218,
280

— on sea waves, 170

— on the swing of mountains, 135

— on propagation from a fissure,
217

oe

362 INDEX. wee

MAL

Mallet on the temperature of focal
cavity, 84

Malvasia, M. le Conte, on earth
tremors, 316

Martin, D.§S., on the New England
earthquake of 1874, 142

Meizoseismic area, definition of, 10

Melzi, on curves of microseismic

- motion, 322

Meteors, on earthquakes and, 260

Microseismic movements, on cause
of, 324

Milne, D., on the Lisbon earth-
quake, 87

— on earthquake synchronism,247

Mitchell, on earthquake motion, 42

Moon, effect of, on earthquakes,
251, 285

Mountains, on the swing of, 135

NAUMANN, E., on meteors and
earthquakes, 261

— on sun spots and earthquakes,
263

OCEAN, on disturbances in, 163-—
186

Origin, definition of, 9

-— on the determination of, 187

— position of, deduced from di-
rection of motion, 192

— —from destruction of build-
ings, 194

— — from rotation of bodies, 195

— — from time of occurrence, 199

— — examples of methods of cal-
culating, 200-212

Oscillations, on earth, 344

Overturning moment, on the area
of greatest, 53

PALMER, Col. H. S., on earth tre-
mors, 307

Palmieri, on clock stopping, 36, 62

Paul, H. M., on earth tremors, 308

Perrey, A., on the influence of the
moon on earthquakes, 251

SEA

Perrey on the periodicity of earth-
quakes, 8

Perry, J., on position of yes
in walls, PEE

Physicists, on the interest of earth-
quakes to, 2

Planets, influence of, on earth-
quakes, 260

Plantamour, M., on earth pulsa-
tions, 328

Pleistoseists, definition of, 10

Poly, M. A., on earthquakes and
sun spots, 263

— on earthquakes and revolving
storms, 294

Prost, M. le Baron, on earth tre-
mors, 316

Pulsation, on earth, 4, 326-343

RECORDS, on receivers of, 33

Rivers, on disturbances in, 154

Rockwood, Prof., on American
earthquakes, 6

Ronaldson, T., on San Francisco
houses, 129

Rossi, M. 8. di, on an eruption of
gas in the Tiber, 153

— aurora and earthquakes, 264

— earth tremors, 317, 320

— earth oscillations, 346

— earth pulsations, 327

— microseismograph of, 318

—microphonic observations of,
319, 323

— normal tromometer of, 317

SCHMIDT, on the influence of
barometric pressure on earth-
quakes, 267

Sea waves, on nature of, 165

— on cause of, 171

—seldom produced by earth-
quakes which originate inland,
175

—on velocity of propagation of,
AT7

— examples of, 179

Seasons, frequency of earthquakes
at different, 254

a:

‘ INDEX. 363

SEE

Seebach, on the determination of
origins, 211

— on the focal cavity, 224

Seismic vertical, definition of, 9

Seismic and volcanic phenomena,
relation of, 270

— — conclusions regarding, 275,
295

Seismology, definition of, 9

Seismometers, on various forms of,
17-40

Seismoscopes, on various forms of,
13-20

Serpieri, P. A., on distribution of
seismic movement, 231

Shadows, on earthquake, 137

Spring, on frequency of earth-
quakes during, 156

Stuckeley, on earthquake motion,
42

— earthquakes and aurora, 265

Succussatore, definition of, 10

Sun, on the effect of, on eaith-
quakes, 253, 285

TEMPERATURE, effect of changes
of, on earthquakes, 268, 294

Terremotto, definition of, 10

Thomson, Sir W., on the rigidity
of the earth, 285

Time, on recording apparatus for,
3

Travagini, F., on earthquake mo-
tion, 42

Trembelores, definition of, 10

Tremors, on earth, 3, 306-325

UNDERSTANDING, effects of earth-
quakes on, 2

ZOL

VERBECK, on the ball and plate
seismometer of, 31

Vibration, on the nature of earth-
quake, 12

Vorticose motion, on, 70

— definition of, 10

WAGENER, on the pendulum seis-
moter of, 25

— vertica motion seismometer
of, 33

— list of earthquakes, 76

Wave paths, definition of, 9

Waves, on thenature of earthquake,
55)

— on the interference of, 138

Wells, on the effect of earthquakes
on, 156

Wenthrop, on the New Zealand
earthquake of 1855, 79

West, on the parallel motion seis-
mometer of, 28

Winslow, on pulsations of the
ocean, 334

Wolf, R., on earthquakes and sun
spots, 263

Woodward, on earthquake motion,
42

Younc, Dr. T., on earthquake
motion, 43

ZANTEDESCHI, M. F., on the in-
fluence of the sun and moon on
earthquakes, 285

Zollner, on the bracket seismo-
meter of, 27

— on earth tremors, 309

a a ee

VOL CAA OES:

WHAT FHEY ARB AND WHAT THEY TEACH,

By J. W. JUDD,
Professor of Geology in the Royal School of Mines (London).

With Ninety-six Illustrations. 12mo0. Cloth, $2.00.

‘The volume before us is one of the pleasantest science manuals we
have read for some time.” —.Atheneum.

“Mr. Judd’s summary is so full and so concise, that it is almost im-
possible to give a fair idea in a short review.’—Pall Mall Gazette.

“Professor Judd discusses the nature of volcanic action, the internal
structure of volcanic mountains, the distribution of volcanoes upon the
surface of the globe, their activity in different periods of the earth’s exist-
ence, the use of volcanoes in the economy of nature, the various theories
that have been made to explain volcanic action. He has abbreviated in
this volume a vast amount of information, which has a fascinating in-
terest for many minds by reason of its relation to the past history and
future destiny of this little bubble of earth upon which we sail through
the infinite spaces of ether.”—New York Home Journal.

“The book gives an exhaustive statement of the phenomena of volca-
noes, and of the facts in the formation of mountain-chains, and relates a
mass of interesting observations and facts, the results of patient and ex-
tensive personal investigation and study, mostly in different places in
Southern Europe, but not neglecting the world’s larger volcanoes in other
regions.” —Hartford Times.

“A fascinating example of patient observation, sound judgment, and
acute reasoning. Under Professor Judd’s skillful treatment the volcano
is forced not only to tell its own history, but also to solve a number of
earth problems seemingly disconnected with it; and the story is told in
strong, nervous language, and with an earnestness and subdued enthu-
siasm that are delightfully stimulating.”— Boston Gazette.

‘“‘Professor Judd first points out the errors in the old definition of a
voleano. The volcanic hole is very often not on the summit, but on the
side, sometimes at the base of the mountain or hill, and it- sends forth
steam rather than smoke, and the supposed raging flames are nothing
more than the glowing light of a mass of molten material reflected from
those vapor-clouds. So our old-ignorance vanishes, and in this admirable
work the internal structure of volcanic mountains, the nature and prod-
ucts of volcanic action, and the distribution of the materials rejected
from volcanic vents, the succession of operations taking place at volcanic
centers, are all very ably and clearly discussed.”—Philadelphia Times.

‘A succinct and excellent treatise on a very interesting subject.”—
Philadelphia North American.

For sale by all booksellers; or sent by mail, post-paid, on receipt of price.
New York: D. APPLETON & CO., 1, 3, & 5 Bond Street.

THE CONCEPTS AND THEOFi=.
OF MODERN PHYSICS.

By J. B. STALLO.

Homo’ Cloth yh) Ate eaten elena

** Judge Stallo’s work is an inquiry into the validity of those mechanical

conceptions of the universe which are now held as fundamental in physical

science. He takes up the leading modern dvctrines which are based upon
this mechanical conception, such as the atomic constitution of matter, the
kinetic theory of gases, the conservation of energy, the nebular hypothesis
and other views, to find how much stands upon solid empirical ground, an
how much rests upon metaphysical speculation. Since the appearance of
Dr. Draper’s ‘ Religion and Science,’ no book has been published in the
country calculated to make so deep an impression on thoughtful and edu-
cated readers as this volume. ... The range and minuteness of the au-
thor’s learning, the acuteness of his reasoning, and the singular precision
and clearness of his style, are qualities which very seldom have been jointly
exhibited in a scientific treatise.’—WVew York Sun.

‘“‘ Judge J. B. Stallo, of Cincinnati, is a German by birth, and came to
this country at about the age of seventeen. He was early familiar with
science, and he lectured for some years in an Eastern college; but at length
he adopted the profession of law. He is also remembered by many as an
author, having a number of years ago written a metaphysical treatise of
marked ability for one of his youthful years. His present book must be
read deliberately, must be studied to be appreciated; but the students of
science, as well as those of metaphysics, are certain to be deeply interested
in its logical developments. It is a timely and telling contribution to the
philosophy of science, imperatively called for by the present exigencies in
the progress of knowledge. Itis to be commended equally for the solid
value of its contents and the scholarly finish of its execution.’”—The Pop-
ular Science Monthly.

‘‘ The book is of vital interest to a much larger class than specialists—
to all, in fact, who value clear thinking or are interested in the accuracy
more than the progress of scientific thought. It deals with the results and
theories of physical science, and in no sense with the processes of the labo-
ratory. It is written with a clearness that is uncommon in philosophic
works and with a desire to find truth, conscious of the fact that a prime
prerequisite of tinding it isto clear the way of accumulated and fast-settling
untruths. It is a scientific rebuke, as severe as it is lucid, of the scientists
who leave their apparatus and go star-gazing: here is the pit into which
they have fallen.””"—Wew York World.

““The volume is an important contribution to scientific discussion, and
is marked by closeness of reasoning, and clearness and cogency of staie-
ment.’’— Boston Journal.

For sile by all bookseilers; or sent by mail, post paid, on receipt of price.

New York: D. APPLETON & CO., 1, 8, & 5 Bond 8t.

o>

oe:
re eats

(%

| TW a
| | WI MMM ae
ATA ATA
|

1 | im |
| 1] Hy
| | ry Wg
1 | Ta |
vant HL aH

Ue ie el | Wiel Hil/ 1H Hi |
NTE i

ae ees

a3

*
FO em