DESTROYING AND TRANSPORTING EFFECTS OF TIDES AND CURRENTS.
Difference in the rise of tides--Lagullas and Gulf
currents--Velocity of currents--Causes of currents--Action of the
sea on the British coast--Shetland Islands--Large blocks
removed--Isles reduced to clusters of rocks--Orkney isles--Waste of
East coast of Scotland--and East coast of England--Waste of the
cliffs of Holderness, Norfolk, and Suffolk--Sand-dunes, how far
chronometers--Silting up of estuaries--Yarmouth estuary--Suffolk
coast--Dunwich--Essex coast--Estuary of the Thames--Goodwin
Sands--Coast of Kent--Formation of the Straits of Dover--South coast
of England--Sussex--Hants--Dorset--Portland--Origin of the Chesil
Bank--Cornwall--Coast of Brittany.
Although the movements of great bodies of water, termed tides and
currents, are in general due to very distinct causes, their effects
cannot be studied separately; for they produce, by their joint action,
aided by that of the waves, those changes which are objects of
geological interest. These forces may be viewed in the same manner as we
before considered rivers, first, as employed in destroying portions of
the solid crust of the earth and removing them to other places;
secondly, as reproductive of new strata.
_Tides._--It would be superfluous at the present day to offer any
remarks on the cause of the tides. They are not perceptible in lakes or
in most inland seas; in the Mediterranean even, deep and extensive as is
that sea, they are scarcely sensible to ordinary observation, their
effects being quite subordinate to those of the winds and currents. In
some places, however, as in the Straits of Messina, there is an ebb and
flow to the amount of two feet and upwards; at Naples and at the
Euripus, of twelve or thirteen inches; and at Venice, according to
Rennell, of five feet.[378] In the Syrtes, also, of the ancients, two
wide shallow gulfs, which penetrate very far within the northern coast
of Africa, between Carthage and Cyrene, the rise is said to exceed five
feet.[379]
In islands remote from any continent, the ebb and flow of the ocean is
very slight, as at St. Helena, for example, where it is rarely above
three feet.[380] In any given line of coast, the tides are greatest in
narrow channels, bays, and estuaries, and least in the intervening
tracts where the land is prominent. Thus, at the entrance of the estuary
of the Thames and Medway, the rise of the spring tides is eighteen feet;
but when we follow our eastern coast from thence northward, towards
Lowestoff and Yarmouth, we find a gradual diminution, until at the
places last mentioned, the highest rise is only seven or eight feet.
From this point there begins again to be an increase, so that at Comer,
where the coast again retires towards the west, the rise is sixteen
feet; and towards the extremity of the gulf called "the Wash," as at
Lynn and in Boston Deeps, it is from twenty-two to twenty-four feet, and
in some extraordinary cases twenty-six feet. From thence again there is
a decrease towards, the north, the elevation at the Spurn Point being
from nineteen to twenty feet, and at Flamborough Head and the Yorkshire
coast from fourteen to sixteen feet.[381]
At Milford Haven in Pembrokeshire, at the mouth of the Bristol Channel,
the tides rise thirty-six feet; and at King-Road near Bristol, forty-two
feet. At Chepstow on the Wye, a small river which opens into the estuary
of the Severn, they reach fifty feet, and sometimes sixty-nine, and even
seventy-two feet. A current which sets in on the French coast, to the
west of Cape La Hague, becomes pent up by Guernsey, Jersey, and other
islands, till the rise of the tide is from twenty to forty-five feet,
which last height it attains at Jersey, and at St. Malo, a seaport of
Brittany. The tides in the Basin of Mines, at the head of the Bay of
Fundy in Nova Scotia, rise to the height of seventy feet.
There are, however, some coasts where the tides seem to offer an
exception to the rule above mentioned; for while there is scarcely any
rise in the estuary of the Plata in S. America, there is an extremely
high tide on the open coast of Patagonia, farther to the south. Yet even
in this region the tides reach their greatest elevation (about fifty
feet) in the Straits of Magellan, and so far at least they conform to
the general rule.[382]
_Currents._--The most extensive and best determined system of currents,
is that which has its source in the Indian Ocean under the influence of
the trade winds; and which, after doubling the Cape of Good Hope,
inclines to the northward, along the western coast of Africa, then
across the Atlantic, near the equator, where it is called the equatorial
current, and is lost in the Caribbean Sea, yet seems to be again revived
in the current which issues from the Gulf of Mexico. From thence it
flows rapidly through the Straits of Bahama, taking the name of the Gulf
Stream, and passing in a northeasterly direction, by the Banks of
Newfoundland, towards the Azores.
We learn from the posthumous work of Rennell on this subject, that the
Lagullas current, so called from the cape and bank of that name, is
formed by the junction of two streams, flowing from the Indian Ocean;
the one from the channel of Mozambique, down the southeast coast of
Africa; the other from the ocean at large. The collective stream is from
ninety to one hundred miles in breadth, and runs at the rate of from two
and a half to more than four miles per hour. It is at length turned
westward by the Lagullas bank, which rises from a sea of great depth to
within one hundred fathoms of the surface. It must therefore be
inferred, says Rennell, that the current here is more than one hundred
fathoms deep, otherwise the main body of it would pass across the bank,
instead of being deflected westward, so as to flow round the Cape of
Good Hope. From this cape it flows northward, as before stated, along
the western coast of Africa, taking the name of the South Atlantic
current. It then enters the Bight, or Bay of Benin, and is turned
westward, partly by the form of the coast there, and partly, perhaps, by
the Guinea current, which runs from the north into the same great bay.
From the centre of this bay proceeds the equatorial current already
mentioned, holding a westerly direction across the Atlantic, which it
traverses, from the coast of Guinea to that of Brazil, flowing
afterwards by the shores of Guiana to the West Indies. The breadth of
this current varies from 160 to 450 geographical miles, and its velocity
is from twenty-five to seventy-nine miles per day, the mean rate being
about thirty miles. The length of its whole course is about 4000 miles.
As it skirts the coast of Guiana, it is increased by the influx of the
waters of the Amazon and Orinoco, and by their junction acquires
accelerated velocity. After passing the island of Trinidad it expands,
and is almost lost in the Caribbean Sea; but there appears to be a
general movement of that sea towards the Mexican Gulf, which discharges
the most powerful of all currents through the Straits of Florida, where
the waters run in the northern part with a velocity of four or five
miles an hour, having a breadth of from thirty-five to fifty miles.[383]
The temperature of the Gulf of Mexico is 86 degrees F. in summer, or 6
degrees higher than that of the ocean, in the same parallel (25 degrees
N. lat.), and a large proportion of this warmth is retained, even where
the stream reaches the 43 degrees N. lat. After issuing from the Straits
of Florida, the current runs in a northerly direction to Cape Hatteras,
in North Carolina, about 35 degrees N. lat., where it is more than
seventy miles broad, and still moves at the rate of seventy-five miles
per day. In about the 40 degrees N. lat., it is turned more towards the
Atlantic by the extensive banks of Nantucket and St. George, which are
from 200 to 300 feet beneath the surface of the sea; a clear proof that
the current exceeds that depth. On arriving near the Azores, the stream
widens, and overflows, as it were, forming a large expanse of warm water
in the centre of the North Atlantic, over a space of 200 or 300 miles
from north to south, and having a temperature of from 8 degrees to 10
degrees Fahr. above the surrounding ocean. The whole area, covered by
the Gulf water, is estimated by Rennell at 2000 miles in length, and, at
a mean, 350 miles in breadth; an area more extensive than that of the
Mediterranean. The warm water has been sometimes known to reach the Bay
of Biscay, still retaining five degrees of temperature above that of the
adjoining ocean; and a branch of the Gulf current occasionally drifts
fruits, plants, and wood, the produce of America and the West Indies, to
the shores of Ireland and the Hebrides.
From the above statements we may understand why Rennell has
characterized some of the principal currents as oceanic rivers, which he
describes as being from 50 to 250 miles in breadth, and having a
rapidity exceeding that of the largest navigable rivers of the
continents, and so deep as to be sometimes obstructed, and occasionally
turned aside, by banks, the tops of which do not rise within forty,
fifty, or even one hundred fathoms of the surface of the sea.[384]
_Greatest velocity of currents._--The ordinary velocity of the principal
currents of the ocean is from one to three miles per hour; but when the
boundary lands converge, large bodies of water are driven gradually into
a narrow space, and then wanting lateral room, are compelled to raise
their level. Whenever this occurs their velocity is much increased. The
current which runs through the Race of Alderney, between the island of
that name and the main land, has a velocity of about eight English miles
an hour. Captain Hewett found that in the Pentland Firth, the stream, in
ordinary spring tides, runs ten miles and a half an hour, and about
thirteen miles during violent storms. The greatest velocity of the tidal
current through the "Shoots" or New Passage, in the Bristol Channel, is
fourteen English miles an hour; and Captain King observed, in his survey
of the Straits of Magellan, that the tide ran at the same rate through
the "First Narrows," and about eight geographical miles an hour, in
other parts of those straits.
_Causes of currents._--That movements of no inconsiderable magnitude
should be impressed on an expansive ocean, by winds blowing for many
months in one direction, may easily be conceived, when we observe the
effects produced in our own seas by the temporary action of the same
cause. It is well known that a strong southwest or northwest wind
invariably raises the tides to an unusual height along the west coast of
England and in the Channel; and that a northwest wind of any
continuance causes the Baltic to rise two feet and upwards above its
ordinary level. Smeaton ascertained by experiment, that in a canal four
miles in length, the water was kept up four inches higher at one end
than at the other, merely by the action of the wind along the canal; and
Rennell informs us that a large piece of water, ten miles broad, and
generally only three feet deep, has, by a strong wind, had its waters
driven to one side, and sustained so as to become six feet deep, while
the windward side was laid dry.[385]
As water, therefore, he observes, when pent up so that it cannot escape,
acquires a higher level, so, in a place _where it can escape_, the same
operation produces a current; and this current will extend to a greater
or less distance, according to the force by which it is produced. By the
side of the principal oceanic currents, such as the Lagullas and the
Gulf Stream, are parallel "counter-currents" running steadily in an
opposite direction.
Currents flowing alternately in opposite directions are occasioned by
the rise and fall of the tides. The effect of this cause is, as before
observed, most striking in estuaries and channels between islands.
A third cause of oceanic currents is evaporation by solar heat, of which
the great current setting through the Straits of Gibraltar into the
Mediterranean is a remarkable example, and will be fully considered in
the next chapter. A stream of colder water also flows from the Black Sea
into the Mediterranean. It must happen in many other parts of the world
that large quantities of water raised from one tract of the ocean by
solar heat, are carried to some other where the vapor is condensed and
falls in the shape of rain, and this, in flowing back again to restore
equilibrium, will cause sensible currents.
These considerations naturally lead to the inquiry whether the level of
those seas out of which currents flow, is higher than that of seas into
which they flow. If not, the effect must be immediately equalized by
under-currents or counter-currents. Arago is of opinion that, so far as
observations have gone, there are no exact proofs of any such difference
of level. It was inferred from the measurements of M. Lepare, that the
level of the Mediterranean, near Alexandria, was lower by 26 feet 6
inches, than the Red Sea near Suez at low water, and about 30 feet lower
than the Red Sea at the same place at high water,[386] but Mr. Robert
Stevenson affirms, as the result of a more recent survey, that there is
no difference of level between the two seas.[387]
It was formerly imagined that there was an equal, if not greater,
diversity in the relative levels of the Atlantic and Pacific, on the
opposite sides of the Isthmus of Panama. But the levellings carried
across that isthmus by Capt. Lloyd, in 1828, to ascertain the relative
height of the Pacific Ocean at Panama, and of the Atlantic at the mouth
of the river Chagres, have shown, that the difference of mean level
between those oceans is not considerable, and, contrary to expectation,
the difference which does exist is in favor of the greater height of the
Pacific. According to this survey, the mean height of the Pacific is
three feet and a half, or 3.52 above the Atlantic, if we assume the mean
level of a sea to coincide with the mean between the extremes of the
elevation and depression of the tides; for between the extreme levels of
the greatest tides in the Pacific, at Panama, there is a difference of
27.44 feet; and at the usual spring tides 21.22 feet; whereas at Chagres
this difference is only 1.16 feet, and is the same at all seasons of the
year.
The tides, in short, in the Caribbean Sea are scarcely perceptible, not
equalling those in some parts of the Mediterranean, whereas the rise is
very high in the Bay of Panama; so that the Pacific is at high tide
lifted up several feet above the surface of the Gulf of Mexico, and then
at low water let down as far below it.[388] But astronomers are agreed
that, on mathematical principles, the rise of the tidal wave above the
mean level of a particular sea must be greater than the fall below it;
and although the difference has been hitherto supposed insufficient to
cause an appreciable error, it is, nevertheless, worthy of observation,
that the error, such as it may be, would tend to reduce the small
difference, now inferred, from the observations of Mr. Lloyd, to exist
between the levels of the two oceans.
There is still another way in which heat and cold must occasion great
movements in the ocean, a cause to which, perhaps, currents are
principally due. Whenever the temperature of the surface of the sea is
lowered, condensation takes place, and the superficial water, having its
specific gravity increased, falls to the bottom, upon which lighter
water rises immediately and occupies its place. When this circulation of
ascending and descending currents has gone on for a certain time in high
latitudes, the inferior parts of the sea are made to consist of colder
or heavier fluid than the corresponding depths of the ocean between the
tropics. If there be a free communication, if no chain of submarine
mountains divide the polar from the equatorial basins, a horizontal
movement will arise by the flowing of colder water from the poles to the
equator, and there will then be a reflux of warmer superficial water
from the equator to the poles. A well-known experiment has been adduced
to elucidate this mode of action in explanation of the "trade
winds."[389] If a long trough, divided in the middle by a sluice or
partition, have one end filled with water and the other with
quicksilver, both fluids will remain quiet so long as they are divided;
but when the sluice is drawn up, the heavier fluid will rush along the
bottom of the trough, while the lighter, being displaced, will rise,
and, flowing in an opposite direction, spread itself at the top. In like
manner the expansion and contraction of sea-water by heat and cold, have
a tendency to set under-currents in motion from the poles to the
equator, and to cause counter-currents at the surface, which are
impelled in a direction contrary to that of the prevailing trade winds.
The geographical and other circumstances being very complicated, we
cannot expect to trace separately the movements due to each cause, but
must be prepared for many anomalies, especially as the configuration of
the bed of the ocean must often modify and interfere with the course of
the inferior currents, as much as the position and form of continents
and islands alter the direction of those on the surface. Thus on
sounding at great depths in the Mediterranean, Captains Berard and
D'Urville have found that the cold does not increase in a high ratio as
in the tropical regions of the ocean, the thermometer remaining fixed at
about 55 degrees F. between the depths of 1000 and 6000 feet. This might
have been anticipated, as Captain Smyth in his survey had shown that the
deepest part of the Straits of Gibraltar is only 1320 feet, so that a
submarine barrier exists there which must prevent the influx of any
under-current of the ocean cooled by polar ice.
Each of the four causes above mentioned, the wind, the tides,
evaporation, and the expansion and contraction of water by heat and
cold, may be conceived to operate independently of the others, and
although the influence of all the rest were annihilated. But there is
another cause, the rotation of the earth on its axis, which can only
come into play when the waters have already been set in motion by some
one or all of the forces above described, and when the direction of the
current so raised happens to be from south to north, or from north to
south.
The principle on which this cause operates is probably familiar to the
reader, as it has long been recognized in the case of the trade winds.
Without enlarging, therefore, on the theory, it will be sufficient to
offer an example of the mode of action alluded to. When a current flows
from the Cape of Good Hope towards the Gulf of Guinea, it consists of a
mass of water, which, on doubling the Cape, in lat. 35 degrees, has a
rotatory velocity of about 800 miles an hour; but when it reaches the
line, where it turns westward, it has arrived at a parallel where the
surface of the earth is whirled round at the rate of 1000 miles an hour,
or about 200 miles faster. If this great mass of water was transferred
suddenly from the higher to the lower latitude, the deficiency of its
rotatory motion, relatively to the land and water with which it would
come into juxtaposition, would be such as to cause an apparent motion of
the most rapid kind (of no less than 200 miles an hour) from east to
west.
In the case of such a sudden transfer, the eastern coast of America,
being carried round in an opposite direction, might strike against a
large body of water with tremendous violence, and a considerable part of
the continent might be submerged. This disturbance does not occur,
because the water of the stream, as it advances gradually into new zones
of the sea which are moving more rapidly, acquires by friction an
accelerated velocity. Yet as this motion is not imparted
instantaneously, the fluid is unable to keep up with the full speed of
the new surface over which it is successively brought. Hence, to borrow
the language of Herschel, when he speaks of the trade winds, "it lags or
hangs back, in a direction opposite to the earth's rotation, that is,
from east to west,"[390] and thus a current, which would have run simply
towards the north but for the rotation, may acquire a relative direction
towards the west.
We may next consider a case where the circumstances are the converse of
the above. The Gulf Stream flowing from about lat. 20 degrees is at first
impressed with a velocity of rotation of about 940 miles an hour, and
runs to the lat. 40 degrees, where the earth revolves only at the rate
of 766 miles, or 174 miles slower. In this case a relative motion of an
opposite kind may result; and the current may retain an excess of
rotatory velocity, tending continually to deflect it eastward. Polar
currents, therefore, or those flowing from high to low latitudes, are
driven towards the eastern shores of continents, while tropical currents
flowing towards the poles are directed against their western shores.
Thus it will be seen that currents depend, like the tides, on no
temporary or accidental circumstances, but on the laws which preside
over the motions of the heavenly bodies. But although the sum of their
influence in altering the surface of the earth may be very constant
throughout successive epochs, yet the points where these operations are
displayed in fullest energy shift perpetually. The height to which the
tides rise, and the violence and velocity of currents, depend in a great
measure on the actual configuration of the land, the contour of a long
line of continental or insular coast, the depth and breadth of channels,
the peculiar form of the bottom of seas--in a word, on a combination of
circumstances which are made to vary continually by many igneous and
aqueous causes, and, amongst the rest, by the tides and currents
themselves. Although these agents, therefore, of decay and reproduction
are local in reference to periods of short duration, such as those which
history embraces, they are nevertheless universal, if we extend our
views to a sufficient lapse of ages.
_Destroying and transporting power of currents._--After these
preliminary remarks on the nature and causes of currents, their velocity
and direction, we may next consider their action on the solid materials
of the earth. We shall find that their efforts are, in many respects,
strictly analogous to those of rivers. I have already treated in the
third chapter, of the manner in which currents sometimes combine with
ice, in carrying mud, pebbles, and large fragments of rock to great
distances. Their operations are more concealed from our view than those
of rivers, but extend over wider areas, and are therefore of more
geological importance.
_Waste of the British coasts._--_Shetland Islands_.--If we follow the
eastern and southern shores of the British islands, from our Ultima
Thule in Shetland to the Land's End in Cornwall, we shall find evidence
of a series of changes since the historical era, very illustrative of
the kind and degree of force exerted by tides and currents co-operating
with the waves of the sea. In this survey we shall have an opportunity
of tracing their joint power on islands, promontories, bays, and
estuaries; on bold, lofty cliffs, as well as on low shores; and on every
description of rock and soil, from granite to blown sand.
The northernmost group of the British islands, the Shetland, are
composed of a great variety of rocks, including granite, gneiss,
mica-slate, serpentine, greenstone, and many others, with some secondary
rocks, chiefly sandstone and conglomerate. These islands are exposed
continually to the uncontrolled violence of the Atlantic, for no land
intervenes between their western shores and America. The prevalence,
therefore, of strong westerly gales, causes the waves to be sometimes
driven with irresistible force upon the coast, while there is also a
current setting from the north. The spray of the sea aids the
decomposition of the rocks, and prepares them to be breached by the
mechanical force of the waves. Steep cliffs are hollowed out into deep
caves and lofty arches; and almost every promontory ends in a cluster of
rocks, imitating the forms of columns, pinnacles, and obelisks.
_Drifting of large masses of rock._--Modern observations show that the
reduction of continuous tracts to such insular masses is a process in
which nature is still actively engaged. "The isle of Stenness," says Dr.
Hibbert, "presents a scene of unequalled desolation. In stormy winters,
huge blocks of stones are overturned, or are removed from their native
beds, and hurried up a slight acclivity to a distance almost incredible.
In the winter of 1802, a tabular-shaped mass, eight feet two inches by
seven feet, and five feet one inch thick, was dislodged from its bed,
and removed to a distance of from eighty to ninety feet. I measured the
recent bed from which a block had been carried away the preceding winter
(A. D. 1818), and found it to be seventeen feet and a half by seven
feet, and the depth two feet eight inches. The removed mass had been
borne to a distance of thirty feet, when it was shivered into thirteen
or more lesser fragments, some of which, were carried still farther,
from 30 to 120 feet. A block, nine feet two inches by six feet and a
half, and four feet thick, was hurried up the acclivity to a distance of
150 feet."[391]
At Northmavine, also, angular blocks of stone have been removed in a
similar manner to considerable distances by the waves of the sea, some
of which are represented in the annexed figure.
_Effects of lightning._--In addition to numerous examples of masses
detached and driven by the waves, tides, and currents from their place,
some remarkable effects of lightning are recorded in these isles. At
Funzie, in Fetlar, about the middle of the last century, a rock of
mica-schist, 105 feet long, ten feet broad, and in some places four feet
thick, was in an instant torn by a flash of lightning from its bed, and
broken into three large and several smaller fragments. One of these,
twenty-six feet long, ten feet broad, and four feet thick, was simply
turned over. The second, which was twenty-eight feet long, seventeen
broad, and five feet in thickness, was hurled across a high point to the
distance of fifty yards. Another broken mass, about forty feet long, was
thrown still farther, but in the same direction, quite into the sea.
There were also many smaller fragments scattered up and down.[392]
[Illustration: Fig. 27.
Stony fragments drifted by the sea. Northmavine, Shetland.]
When we thus see electricity co-operating with the violent movements of
the ocean in heaping up piles of shattered rocks on dry land and beneath
the waters, we cannot but admit that a region which shall be the
theatre, for myriads of ages, of the action of such disturbing causes,
might present, at some future period, if upraised far above the bosom of
the deep, a scene of havoc and ruin that may compare with any now found
by the geologist on the surface of our continents.
In some of the Shetland Isles, as on the west of Meikle Roe, dikes, or
veins of soft granite, have mouldered away; while the matrix in which
they were inclosed, being of the same substance, but of a firmer
texture, has remained unaltered. Thus, long narrow ravines, sometimes
twenty feet wide, are laid open, and often give access to the waves.
After describing some huge cavernous apertures into which the sea flows
for 250 feet in Roeness, Dr. Hibbert, writing in 1822, enumerates other
ravages of the ocean. "A mass of rock, the average dimensions of which
may perhaps be rated at twelve or thirteen feet square, and four and a
half or five in thickness, was first moved from its bed, about fifty
years ago, to a distance of thirty feet, and has since been twice turned
over."
_Passage forced by the sea through porphyritic rocks._--"But the most
sublime scene is where a mural pile of porphyry, escaping the process
of disintegration that is devastating the coast, appears to have been
left as a sort of rampart against the inroads of the ocean;--the
Atlantic, when provoked by wintry gales, batters against it with all the
force of real artillery--the waves having, in their repeated assaults,
forced themselves an entrance. This breach, named the Grind of the Navir
(fig. 28), is widened every winter by the overwhelming surge that,
finding a passage through it, separates large stones from its sides, and
forces them to a distance of no less than 180 feet. In two or three
spots, the fragments which have been detached are brought together in
immense heaps, that appear as an accumulation of cubical masses, the
product of some quarry."[393]
[Illustration: Fig. 28.
Grind of the Navir--passage forced by the sea through rocks of hard
porphyry.]
It is evident from this example, that although the greater
indestructibility of some rocks may enable them to withstand, for a
longer time, the action of the elements, yet they cannot permanently
resist. There are localities in Shetland, in which rocks of almost every
variety of mineral composition are suffering disintegration; thus the
sea makes great inroads on the clay slate of Fitfel Head, on the
serpentine of the Vord Hill in Fetlar, and on the mica-schist of the Bay
of Triesta, on the east coast of the same island, which decomposes into
angular blocks. The quartz rock on the east of Walls, and the gneiss and
mica-schist of Garthness, suffer the same fate.
_Destruction of islands._--Such devastation cannot be incessantly
committed for thousands of years without dividing islands, until they
become at last mere clusters of rocks, the last shreds of masses once
continuous. To this state many appear to have been reduced, and
innumerable fantastic forms are assumed by rocks adjoining these islands
to which the name of Drongs is applied, as it is to those of similar
shape in Feroe.
[Illustration: Fig. 29.
Granitic rocks named the Drongs, between Papa Stour and Hillswick Ness.]
[Illustration: Fig. 30.
Granitic rocks to the south of Hillswick Ness, Shetland.]
The granite rocks (fig. 29), between Papa Stour and Hillswick Ness
afford an example. A still more singular cluster of rocks is seen to the
south of Hillswick Ness (fig. 30), which presents a variety of forms as
viewed from different points, and has often been likened to a small
fleet of vessels with spread sails.[394] We may imagine that in the
course of time Hillswick Ness itself may present a similar wreck, from
the unequal decomposition of the rocks whereof it is composed,
consisting of gneiss and mica-schist traversed in all directions by
veins of felspar-porphyry.
Midway between the groups of Shetland and Orkney is Fair Island, said to
be composed of sandstone with high perpendicular cliffs. The current
runs with such velocity, that during a calm, and when there is no swell,
the rocks on its shores are white with the foam of the sea driven
against them. The Orkneys, if carefully examined, would probably
illustrate our present topic as much as the Shetland group. The
northeast promontory of Sanda, one of these islands, has been cut off in
modern times by the sea, so that it became what is now called Start
Island, where a lighthouse was erected in 1807, since which time the new
strait has grown broader.
_East coast of Scotland._--To pass over to the main land of Scotland, we
find that in Inverness-shire there have been inroads of the sea at Fort
George, and others in Morayshire, which have swept away the old town of
Findhorn. On the coast of Kincardineshire, an illustration was afforded
at the close of the last century, of the effect of promontories in
protecting a line of low shore. The village of Mathers, two miles south
of Johnshaven, was built on an ancient shingle beach, protected by a
projecting ledge of limestone rock. This was quarried for lime to such
an extent that the sea broke through, and in 1795 carried away the whole
village in one night, and penetrated 150 yards inland, where it has
maintained its ground ever since, the new village having been built
farther inland on the new shore. In the bay of Montrose, we find the
North Esk and the South Esk rivers pouring annually into the sea large
quantities of sand and pebbles; yet they have formed no deltas, for the
waves, aided by the current, setting across their mouths, sweep away all
the materials. Considerable beds of shingle, brought down by the North
Esk, are seen along the beach.
Proceeding southwards, we learn that at Arbroath, in Forfarshire, which
stands on a rock of red sandstone, gardens and houses have been carried
away since the commencement of the present century by encroachments of
the sea. It had become necessary before 1828, to remove the lighthouses
at the mouth of the estuary of the Tay, in the same county, at Button
Ness, which were built on a tract of blown sand, the sea having
encroached for three-quarters of a mile.
_Force of waves and currents in estuaries._--The combined power which
waves and currents can exert in _estuaries_ (a term which I confine to
bays entered both by rivers and the tides of the sea), was remarkably
exhibited during the building of the Bell Rock Lighthouse, off the mouth
of the Tay. The Bell Rock is a sunken reef, consisting of red sandstone,
being from twelve to sixteen feet under the surface at high water, and
about twelve miles from the mainland. At the distance of 100 yards,
there is a depth, in all directions of two or three fathoms at low
water. In 1807, during the erection of the lighthouse, six large blocks
of granite, which had been landed on the reef, were removed by the force
of the sea, and thrown over a rising ledge to the distance of twelve or
fifteen paces; and an anchor, weighing about 22 cwt., was thrown up upon
the rock.[395] Mr. Stevenson informs us moreover, that drift stones,
measuring upwards of thirty cubic feet, or more than two tons' weight,
have, during storms, been often thrown upon the rock from the deep
water.[396]
_Submarine forests._--Among the proofs that the sea has encroached on
the land bordering the estuary of the Tay, Dr. Fleming has mentioned a
submarine forest which has been traced for several miles along the
northern shore of the county of Fife.[397] But subsequent surveys seem
to have shown that the bed of peat containing tree-roots, leaves, and
branches, now occurring at a lower level than the Tay, must have come
into its present position by a general sinking of the ground on which
the forest grew. The peat-bed alluded to is not confined, says Mr.
Buist, to the present channel of the Tay, but extends far beyond it, and
is covered by stratified clay from fifteen to twenty-five feet in
thickness, in the midst of which, in some places, is a bed full of
sea-shells.[398] Recent discoveries having established the fact that
upward and downward movements have affected our island since the general
coast-line had nearly acquired its present shape, we must hesitate
before we attribute any given change to a single cause, such as the
local encroachment of the sea upon low land.
On the coast of Fife, at St. Andrew's, a tract of land, said to have
intervened between the castle of Cardinal Beaton and the sea, has been
entirely swept away, as were the last remains of the Priory of Crail, in
the same county, in 1803. On both sides of the Frith of Forth, land has
been consumed; at North Berwick in particular, and at Newhaven, where an
arsenal and dock, built in the reign of James IV., in the fifteenth
century, has been overflowed.
_East coast of England._--If we now proceed to the English coast, we
find records of numerous lands having been destroyed in Northumberland,
as those near Bamborough and Holy Island, and at Tynemouth Castle, which
now overhangs the sea, although formerly separated from it by a strip of
land. At Hartlepool, and several other parts of the coast of Durham
composed of magnesian limestone, the sea has made considerable inroads.
_Coast of Yorkshire._--Almost the whole coast of Yorkshire, from the
mouth of the Tees to that of the Humber, is in a state of gradual
dilapidation. That part of the cliffs which consist of lias, the oolite
series, and chalk, decays slowly. They present abrupt and naked
precipices, often 300 feet in height; and it is only at a few points
that the grassy covering of the sloping talus marks a temporary
relaxation of the erosive action of the sea. The chalk cliffs are worn
into caves and needles in the projecting headland of Flamborough, where
they are decomposed by the salt spray, and slowly crumble away. But the
waste is most rapid between that promontory and Spurn Point, or the
coast of Holderness, as it is called, a tract consisting of beds of
clay, gravel, sand, and chalk rubble. The irregular intermixture of the
argillaceous beds causes many springs to be thrown out, and this
facilitates the undermining process, the waves beating against them, and
a strong current setting chiefly from the north. The wasteful action is
very conspicuous at Dimlington Height, the loftiest point in Holderness,
where the beacon stands on a cliff 146 feet above high water, the whole
being composed of clay, with pebbles scattered through it.[399] "For
many years," says Professor Phillips, "the rate at which the cliffs
recede from Bridlington to Spurn, a distance of thirty-six miles, has
been found by measurement to equal on an average two and a quarter yards
annually, which, upon thirty-six miles of coast, would amount to about
thirty acres a year. At this rate, the coast, the mean height of which
above the sea is about forty feet, has lost one mile in breadth since
the Norman Conquest, and more than two miles since the occupation of
York (Eboracum) by the Romans."[400] The extent of this denudation, as
estimated by the number of cubic feet of matter removed annually, will
be again spoken of in chapter 22.
In the old maps of Yorkshire, we find spots, now sand-banks in the sea,
marked as the ancient sites of the towns and villages of Auburn,
Hartburn, and Hyde. "Of Hyde," says Pennant, "only the tradition is
left; and near the village of Hornsea, a street called Hornsea Beck has
long since been swallowed."[401] Owthorne and its church have also been
in great part destroyed, and the village of Kilnsea; but these places
are now removed farther inland. The annual rate of encroachment at
Owthorne for several years preceding 1830, is stated to have averaged
about four yards. Not unreasonable fears are entertained that at some
future time the Spurn Point will become an island, and that the ocean,
entering into the estuary of the Humber, will cause great
devastation.[402] Pennant, after speaking of the silting up of some
ancient ports in that estuary, observes, "But, in return, the sea has
made most ample reprisals; the site, and even the very names of several
places, once towns of note upon the Humber, are now only recorded in
history; and Ravensper was at one time a rival to Hull (Madox, Ant.
Exch. i. 422), and a port so very considerable in 1332, that Edward
Baliol and the confederated English barons sailed from hence to invade
Scotland; and Henry IV., in 1399, made choice of this port to land at,
to effect the deposal of Richard II.; yet the whole of this has long
since been devoured by the merciless ocean; extensive sands, dry at low
water, are to be seen in their stead."[403]
Pennant describes Spurn Head as a promontory in the form of a sickle,
and says the land, for some miles to the north, was "perpetually preyed
on by the fury of the German Sea, which devours whole acres at a time,
and exposes on the shores considerable quantities of beautiful amber."
_Lincolnshire._--The maritime district of Lincolnshire consists chiefly
of lands that lie below the level of the sea, being protected by
embankments. Some of the fens were embanked and drained by the Romans;
but after their departure the sea returned, and large tracts were
covered with beds of silt, containing marine shells, now again converted
into productive lands. Many dreadful catastrophes are recorded by
incursions of the sea, whereby several parishes have been at different
times overwhelmed.
_Norfolk._--The decay of the cliffs of Norfolk and Suffolk is incessant.
At Hunstanton, on the north, the undermining of the lower arenaceous
beds at the foot of the cliff, causes masses of red and white chalk to
be precipitated from above. Between Hunstanton and Weybourne, low hills,
or dunes, of blown sand, are formed along the shore, from fifty to sixty
feet high. They are composed of dry sand, bound in a compact mass by the
long creeping roots of the plant called Marram (_Arundo arenaria_). Such
is the present set of the tides, that the harbors of Clay, Wells, and
other places are securely defended by these barriers; affording a clear
proof that it is not the strength of the material at particular points
that determines whether the sea shall be progressive or stationary, but
the general contour of the coast.
The waves constantly undermine the low chalk cliffs, covered with sand
and clay, between Weybourne and Sherringham, a certain portion of them
being annually removed. At the latter town I ascertained, in 1829, some
facts which throw light on the rate at which the sea gains upon the
land. It was computed, when the present inn was built, in 1805, that it
would require seventy years for the sea to reach the spot: the mean loss
of land being calculated, from previous observations, to be somewhat
less than one yard, annually. The distance between the house and the sea
was fifty yards; but no allowance was made for the slope of the ground
being _from_ the sea, in consequence of which the waste was naturally
accelerated every year, as the cliff grew lower, there being at each
succeeding period less matter to remove when portions of equal area fell
down. Between the years 1824 and 1829, no less than seventeen yards were
swept away, and only a small garden was then left between the building
and the sea. There was, in 1829, a depth of twenty feet (sufficient to
float a frigate) at one point in the harbor of that port, where, only
forty-eight years before, there stood a cliff fifty feet high, with
houses upon it! If once in half a century an equal amount of change were
produced suddenly by the momentary shock of an earthquake, history would
be filled with records of such wonderful revolutions of the earth's
surface; but, if the conversion of high land into deep sea be gradual,
it excites only local attention. The flagstaff of the Preventive Service
station, on the south side of this harbor, was thrice removed inland
between the years 1814 and 1829, in consequence of the advance of the
sea.
Farther to the south we find cliffs, composed, like those of Holderness
before mentioned, of alternating strata of blue clay, gravel, loam, and
fine sand. Although they sometimes exceed 300 feet in height, the havoc
made on the coast is most formidable. The whole site of ancient Cromer
now forms part of the German Ocean, the inhabitants having gradually
retreated inland to their present situation, from whence the sea still
threatens to dislodge them. In the winter of 1825, a fallen mass was
precipitated from near the lighthouse, which covered twelve acres,
extending far into the sea, the cliffs being 250 feet in height.[404]
The undermining by springs has sometimes caused large portions of the
upper part of the cliffs, with houses still standing upon them, to give
way, so that it is impossible, by erecting breakwaters at the base of
the cliffs, permanently to ward off the danger.
[Illustration: Fig. 31.
Tower of the buried Church of Eccles, Norfolk, A. D. 1839.
The inland slope of the hills of blown sand is shown in this view, with
the lighthouse of Hasborough in the distance.]
On the same coast, says Mr. R. C. Taylor, the ancient villages of
Shipden, Wimpwell, and Eccles have disappeared; several manors and large
portions of neighboring parishes having, piece after piece, been
swallowed up; nor has there been any intermission, from time immemorial,
in the ravages of the sea along a line of coast twenty miles in length,
in which these places stood.[405] Of Eccles, however, a monument still
remains in the rained tower of the old church, which is half buried in
the dunes of sand within a few paces (60?) of the sea-beach (fig. 31).
So early as 1605 the inhabitants petitioned James I. for a reduction of
taxes, as 300 acres of land, and all their houses, save fourteen, had
then been destroyed by the sea. Not one half that number of acres now
remains in the parish, and hills of blown sand now occupy the site of
the houses which were still extant in 1605. When I visited the spot in
1839, the sea was fast encroaching on the sand-hills, and had laid open
on the beach the foundations of a house fourteen yards square, the upper
part of which had evidently been pulled down before it had been buried
under sand. The body of the church has also been long buried, but the
tower still remains visible.
M. E. de Beaumont has suggested that sand-dunes in Holland and other
countries may serve as natural chronometers, by which the date of the
existing continents may be ascertained. The sands, he says, are
continually blown inland by the force of the winds, and by observing the
rate of their march we may calculate the period when the movement
commenced.[406] But the example just given will satisfy every geologist
that we cannot ascertain the starting-point of dunes, all coasts being
liable to waste, and the shores of the Low Countries in particular,
being not only exposed to inroads of the sea, but, as M. de Beaumont
himself has well shown, having even in historical times undergone a
change of level. The dunes may indeed, in some cases, be made use of as
chronometers, to enable us to assign a minimum of antiquity to existing
coast-lines; but this test must be applied with great caution, so
variable is the rate at which the sands may advance into the interior.
Hills of blown sand, between Eccles and Winterton, have barred up and
excluded the tide for many hundred years from the mouths of several
small estuaries; but there are records of nine breaches, from 20 to 120
yards wide, having been made through these, by which immense damage was
done to the low grounds in the interior. A few miles south of
Happisburgh, also, are hills of blown sand, which extend to Yarmouth.
These _dunes_ afford a temporary protection to the coast, and an inland
cliff, about a mile long, at Winterton, shows clearly that at that point
the sea must have penetrated formerly farther than at present.
_Silting up of estuaries_--At Yarmouth, the sea has not advanced upon
the sands in the slightest degree since the reign of Elizabeth. In the
time of the Saxons, a great estuary extended as far as Norwich, which
city, is represented; even in the thirteenth and fourteenth centuries,
as "situated on the banks of an arm of the sea." The sands whereon
Yarmouth is built, first became firm and habitable ground about the year
1008, from which time a line of dunes has gradually increased in height
and breadth, stretching across the whole entrance of the ancient
estuary, and obstructing the ingress of the tides so completely, that
they are only admitted by the narrow passage which the river keeps open,
and which has gradually shifted several miles to the south. The ordinary
tides at the river's mouth rise, at present, only to the height, of
three or four feet, the spring tides to about eight or nine.
By the exclusion of the sea, thousands of acres in the interior have
become cultivated lands; and, exclusive of smaller pools, upwards of
sixty freshwater lakes have been formed, varying in depth from fifteen
to thirty feet, and in extent from one acre to twelve hundred.[407] The
Yare, and other rivers, frequently communicate with these sheets of
water; and thus they are liable to be filled up gradually with
lacustrine and fluviatile deposits, and to be converted into land
covered with forests. Yet it must not be imagined, that the acquisition
of new land fit for cultivation in Norfolk and Suffolk indicates any
permanent growth of the eastern limits of our island to compensate its
reiterated losses. No _delta_ can form on such a shore.
Immediately off Yarmouth, and parallel to the shore, is a great range of
sand-banks, the shape of which varies slowly from year to year, and
often suddenly after great storms. Captain Hewitt, R. N., found in these
banks, in 1836, a broad channel sixty-five feet deep, where there was
only a depth of four feet during a prior survey in 1822. The sea had
excavated to the depth of sixty feet in the course of fourteen years, or
perhaps a shorter period. The new channel thus formed serves at present
(1838), for the entrance of ships into Yarmouth Roads; and the magnitude
of this change shows how easily a new set of the waves and currents
might endanger the submergence of the land gained within the ancient
estuary of the Yare.
That great banks should be thrown across the mouths of estuaries on our
eastern coast, where there is not a large body of river-water to
maintain an open channel, is perfectly intelligible, when we bear in
mind that the marine current, sweeping along the coast, is charged with
the materials of wasting cliffs, and ready to form a bar anywhere the
instant its course is interrupted or checked by any opposing stream. The
mouth of the Yare has been, within the last five centuries, diverted
about four miles to the south. In like manner it is evident that, at
some remote period, the river Alde entered the sea at Aldborough, until
its ancient outlet was barred up and at length transferred to a point no
less than ten miles distant to the southwest. In this case, ridges of
sand and shingle, like those of Lowestoff Ness, which will be described
by and by, have been thrown up between the river and the sea; and an
ancient sea-cliff is to be seen now inland.
It may be asked why the rivers on our east coast are always deflected
southwards, although the tidal current flows alternately from the south
and north? The cause is to be found in the superior force of what is
commonly called "the flood tide from the north," a tidal wave derived
from the Atlantic, a small part of which passes eastward up the English
Channel, and through the Straits of Dover and then northwards, while the
principal body of water, moving much more rapidly in a more open sea, on
the western side of Britain, first passes the Orkneys, and then turning,
flows down between Norway and Scotland, and sweeps with great velocity
along our eastern coast. It is well known that the highest tides on this
coast are occasioned by a powerful northwest wind, which raises the
eastern part of the Atlantic, and causes it to pour a greater volume of
water into the German Ocean. This circumstance of a violent _off-shore_
wind being attended with a rise of the waters, instead of a general
retreat of the sea, naturally excites the wonder of the inhabitants of
our coast. In many districts they look with confidence for a rich
harvest of that valuable manure, the sea-weed, when the north-westerly
gales prevail, and are rarely disappointed.
[Illustration: Fig. 32.
Map of Lowestoff Ness, Suffolk.[408]
_a_, _a_. The dotted lines express a series of sand and shingle, forming
the extremity of the triangular space called the Ness.
_b_, _b_, _b_. The dark line represents the inland cliff on which the
town of Lowestoff stands, between which and the sea is the Ness.]
_Coast of Suffolk._--The cliffs of Suffolk, to which we next proceed,
are somewhat less elevated than those of Norfolk, but composed of
similar alternations of clay, sand, and gravel. From Gorleston in
Suffolk, to within a few miles north of Lowestoff, the cliffs are slowly
undermined. Near the last-mentioned town, there is an inland cliff about
sixty feet high, the sloping talus of which is covered with turf and
heath. Between the cliff and the sea is a low flat tract of sand called
the Ness, nearly three miles long, and for the most part out of reach of
the highest tides. The point of the Ness projects from the base of the
original cliff to the distance of 660 yards. This accession of land,
says Mr. Taylor, has been effected at distinct and distant intervals, by
the influence of currents running between the land and a shoal about a
mile off Lowestoff, called the Holm Sand. The lines of growth in the
Ness are indicated by a series of concentric ridges or embankments
inclosing limited areas, and several of these ridges have been formed
within the observation of persons now living. A rampart of heavy
materials is first thrown up to an unusual altitude by some
extraordinary tide, attended with a violent gale. Subsequent tides
extend the base of this high bank of shingle, and the interstices are
then filled with sand blown from the beach. The Arundo and other marine
plants by degrees obtain a footing; and creeping along the ridge, give
solidity to the mass, and form in some cases a matted covering of turf.
Meanwhile another mound is forming externally, which by the like process
rises and gives protection to the first. If the sea forces its way
through one of the external and incomplete mounds, the breach is soon
repaired. After a while the marine plants within the areas inclosed by
these embankments are succeeded by a better species of herbage affording
good pasturage, and the sands become sufficiently firm to support
buildings.
_Destruction of Dunwich by the sea._--Of the gradual destruction of
Dunwich, once the most considerable seaport on this coast, we have many
authentic records. Gardner, in his history of that borough, published
in 1754, shows, by reference to documents, beginning with Doomsday Book,
that the cliffs at Dunwich, Southwold, Eastern, and Pakefield, have been
always subject to wear away. At Dunwich, in particular, two tracts of
land which had been taxed in the eleventh century, in the time of King
Edward the Confessor, are mentioned in the Conqueror's survey, made but
a few years afterwards, as having been devoured by the sea. The losses,
at a subsequent period, of a monastery,--at another of several
churches,--afterwards of the old port,--then of four hundred houses at
once,--of the church of St. Leonard, the high-road, town-hall, jail, and
many other buildings, are mentioned, with the dates when they perished.
It is stated that, in the sixteenth century, not one-quarter of the town
was left standing; yet the inhabitants retreating inland, the name was
preserved, as has been the case with many other ports when their ancient
site has been blotted out. There is, however, a church of considerable
antiquity still standing, the last of twelve mentioned in some records.
In 1740, the laying open of the churchyard of St. Nicholas and St.
Francis, in the sea-cliffs, is well described by Gardner, with the
coffins and skeletons exposed to view--some lying on the beach, and
rocked
"In cradle of the rude imperious surge."
Of these cemeteries no remains can now be seen. Ray also says, "that
ancient writings make mention of a wood a mile and a half to the east of
Dunwich, the site of which must at present be so far within the
sea."[409] This city, once so flourishing and populous, is now a small
village, with about twenty houses, and one hundred inhabitants.
There is an old tradition, "that the tailors sat in their shops at
Dunwich, and saw the ships in Yarmouth Bay;" but when we consider how
far the coast at Lowestoff Ness projects between these places, we cannot
give credit to the tale, which, nevertheless, proves how much the
inroads of the sea in times of old had prompted men of lively
imagination to indulge their taste for the marvellous.
Gardner's description of the cemeteries laid open by the waves reminds
us of the scene which has been so well depicted by Bewick,[410] and of
which numerous points on the same coast might have suggested the idea.
On the verge of a cliff, which the sea has undermined, are represented
the unshaken tower and western end of an abbey. The eastern aisle is
gone, and the pillars of the cloister are soon to follow. The waves have
almost isolated the promontory, and invaded the cemetery, where they
have made sport with the mortal relics, and thrown up a skull upon the
beach. In the foreground is seen a broken tombstone, erected, as its
legend tells, "to _perpetuate_ the memory"--of one whose name is
obliterated, as is that of the county for which he was "Custos
Rotulorum." A cormorant is perched on the monument, defiling it, as if
to remind some moralizer like Hamlet, of "the base uses" to which things
sacred may be turned. Had this excellent artist desired to satirize
certain popular theories of geology, he might have inscribed the stone
to the memory of some philosopher who taught "the permanency of existing
continents"--"the era of repose"--"the impotence of modern causes."
The incursions of the sea at Aldborough, were formerly very destructive,
and this borough is known to have been once situated a quarter of a mile
east of the present shore. The inhabitants continued to build farther
inland, till they arrived at the extremity of their property, and then
the town decayed greatly; but two sand-banks, thrown up at a short
distance, now afford a temporary safeguard to the coast. Between these
banks and the present shore, where the current now flows, the sea is
twenty-four feet deep on the spot where the town formerly stood.
_Essex._--Harwich is said to have owed its rise to the destruction of
Orwell, a town which stood on the spot now called "the west rocks," and
was overwhelmed by an inroad of the sea since the Conquest.
Apprehensions have been entertained that the isthmus on which Harwich
stands may at no remote period become an island, for the sea may be
expected to make a breach near Lower Dover Court, where Beacon Cliff is
composed of horizontal beds of London clay containing septaria. It had
wasted away considerably between the years 1829 and 1838, at both which
periods I examined this coast. In that short interval several gardens
and many houses had been swept into the sea, and in April, 1838, a whole
street was threatened with destruction. The advance of the sea is much
accelerated by the traffic carried on in septaria, which are shipped off
for cement as fast as they fall down upon the beach. These stones, if
allowed to remain in heaps on the shore, would break the force of the
waves and retard the conversion of the peninsula into an island, an
event which might be followed by the destruction of the town of Harwich.
Captain Washington, R. N., ascertained in 1847, that Beacon Cliff, above
mentioned, which is about fifty feet high, had given way at the rate of
forty feet in forty-seven years, between 1709 and 1756; eighty feet
between 1756 and 1804; and three hundred and fifty feet between the
latter period and 1841; showing a rapidly accelerated rate of
destruction.[411]
Among other losses it is recorded that, since the year 1807, a field
called the Vicar's Field, which belonged to the living of Harwich, has
been overwhelmed;[412] and in the year 1820 there was a considerable
space between the battery at Harwich, built in the beginning of the
present century, and the sea; part of the fortification had been swept
away in 1829, and the rest then overhung the water.
At Walton Naze, in the same county, the cliffs, composed of London clay,
capped by the shelly sands of the crag, reach the height of about 100
feet, and are annually undermined by the waves. The old churchyard of
Walton has been washed away, and the cliffs to the south are constantly
disappearing.
_Kent.--Isle of Sheppey._--On the coast bounding the estuary of the
Thames, there are numerous examples both of the gain and loss of land.
The Isle of Sheppey, which is now about six miles long by four in
breadth, is composed of London clay. The cliffs on the north, which are
from sixty to eighty feet high, decay rapidly, fifty acres having been
lost in twenty years, between 1810 and 1830. The church at Minster, now
near the coast, is said to have been in the middle of the island in
1780; and if the present rate of destruction should continue, we might
calculate the period, and that not a very remote one, when the whole
island will be annihilated. On the coast of the mainland, to the east of
Sheppey, is Herne Bay: a place still retaining the name of a bay,
although it is no longer appropriate, as the waves and currents have
swept away the ancient headlands. There was formerly a small promontory
in the line of the shoals where the present pier is built, by which the
larger bay was divided into two, called the Upper and Lower.[413]
[Illustration: Fig. 33.
View of Reculver Church, taken in the year 1781.
1. Isle of Sheppey. 2. Ancient chapel now destroyed. The cottage between
this chapel and the cliff was demolished by the sea, in 1782.]
Still farther east stands the church of Reculver, upon a cliff composed
of clay and sand, about twenty-five feet high. Reculver (Regulvium) was
an important military station in the time of the Romans, and appears,
from Leland's account, to have been, so late as Henry VIII.'s reign,
nearly one mile distant from the sea. In the "Gentleman's Magazine,"
there is a view of it, taken in 1781, which still represents a
considerable space as intervening between the north wall of the
churchyard and the cliff.[414] Sometime before the year 1780, the waves
had reached the site of the ancient Roman camp or fortification, the
walls of which had continued for several years after they were
undermined to overhang the sea, being firmly cemented into one mass.
They were eighty yards nearer the sea than the church, and they are
spoken of in the "Topographica Britannica," in the year 1780, as having
recently fallen down. In 1804, part of the churchyard with some
adjoining houses was washed away, and the ancient church, with its two
spires, was dismantled and abandoned as a place of worship, but kept in
repair as a landmark well known to mariners. I visited the spot in June,
1851, and saw human bones and part of a wooden coffin projecting from
the cliff, near the top. The whole building would probably have been
swept away long ere this, had not the force of the waves been checked by
an artificial causeway of stones and large wooden piles driven into the
sands on the beach to break the force of the waves.
[Illustration: Fig. 34.
Reculver Church, in 1834.]
_Isle of Thanet._--The isle of Thanet was, in the time of the Romans,
separated from the rest of Kent by a navigable channel, through which
the Roman fleets sailed on their way to and from London. Bede describes
this small estuary as being, in the beginning of the eighth century,
three furlongs in breadth; and it is supposed that it began to grow
shallow about the period of the Norman conquest. It was so far silted up
in the year 1485, that an act was then obtained to build a bridge across
it; and it has since become marsh land with small streams running
through it. On the coast, Bedlam Farm, belonging to the hospital of that
name, lost eight acres in the twenty years preceding 1830, the land
being composed of chalk from forty to fifty feet above the level of the
sea. It has been computed that the average waste of the cliff between
the North Foreland and the Reculvers, a distance of about eleven miles,
is not less than two feet per annum. The chalk cliffs on the south of
Thanet, between Ramsgate and Pegwell Bay, have on an average lost three
feet per annum for the last ten years (preceding 1830).
_Goodwin Sands._--The Goodwin Sands lie opposite this part of the
Kentish coast. They are about ten miles in length, and are in some parts
three, and in others seven, miles distant from the shore; and, for a
certain space, are laid bare at low water. That they are a remnant of
land, and not "a mere accumulation of sea sand," as Rennell
imagined,[415] may be presumed from the fact that, when the erection of
a lighthouse on this shoal was in contemplation by the Trinity Board in
the year 1817, it was found, by borings, that the bank consisted of
fifteen feet of sand, resting on blue clay; and, by subsequent borings,
the subjacent chalk has been reached. An obscure tradition has come down
to us, that the estates of Earl Goodwin, the father of Harold, who died
in the year 1053, were situated here, and some have conjectured that
they were overwhelmed by the flood mentioned in the Saxon chronicle,
_sub anno 1099_. The last remains of an island, consisting, like
Sheppey, of clay, may perhaps have been carried away about that time.
[Illustration: Fig. 35.
Shakspeare's Cliff in 1836, seen from the northeast.]
There are other records of waste in the county of Kent, as at Deal; and
at Dover, where Shakspeare's Cliff, composed entirely of chalk, has
suffered greatly, and continually diminishes in height, the slope of the
hill being towards the land. (See fig. 35.) There was an immense
landslip from this cliff in 1810, by which Dover was shaken as if by an
earthquake, and a still greater one in 1772.[416] We may suppose,
therefore, that the view from the top of the precipice in the year 1600,
when the tragedy of King Lear was written, was more "fearful and dizzy"
than it is now. The best antiquarian authorities are agreed, that Dover
Harbor was formerly an estuary, the sea flowing up a valley between the
chalk hills. The remains found in different excavations confirm the
description of the spot given by Caesar and Antoninus, and there is clear
historical evidence to prove that at an early period there was no
shingle at all at Dover.[417]
_Straits of Dover._--In proceeding from the northern parts of the German
Ocean towards the Straits of Dover, the water becomes gradually more
shallow, so that, in the distance of about two hundred leagues, we pass
from a depth of 120 to that of 58, 38, 18, and even less than 2 fathoms.
The shallowest part follows a line drawn between Romney Marsh and
Boulogne. From this point the English Channel again deepens
progressively as we proceed westward, so that the Straits of Dover may
be said to part two seas.[418]
Whether England was formerly united with France has often been a
favorite subject of speculation. So early as 1605 our countryman
Verstegan, in his "Antiquities of the English Nation," observed that
many preceding writers had maintained this opinion, but without
supporting it by any weighty reasons. He accordingly endeavors himself
to confirm it by various arguments, the principal of which are, first,
the proximity and identity of the composition of the opposite cliffs and
shores of Albion and Gallia, which, whether flat and sandy, or steep and
chalky, correspond exactly with each other; secondly the occurrence of a
submarine ridge, called "our Lady's Sand," extending from shore to shore
at no great depth, and which, from its composition, appears to be the
original basis of the isthmus; thirdly, the identity of the noxious
animals in France and England, which could neither have swum across, nor
have been introduced by man. Thus no one, he says, would have imported
wolves, therefore "these wicked beasts did of themselves pass over." He
supposes the ancient isthmus to have been about six English miles in
breadth, composed entirely of chalk and flint, and in some places of no
great height above the sea-level. The operation of the waves and tides,
he says, would have been more powerful when the straits were narrower,
and even now they are destroying cliffs composed of similar materials.
He suggests the possible co-operation of earthquakes; and when we
consider how many submarine forests skirt the southern and eastern
shores of England, and that there are raised beaches at many points
above the sea-level, containing fossil shells of recent species, it
seems reasonable to suppose that such upward and downward movements,
taking place perhaps as slowly as those now in progress in Sweden and
Greenland, may have greatly assisted the denuding force of "the ocean
stream," [Greek: Potamoio mega sthenos Ocheanoto].
_Folkstone._--At Folkstone, the sea undermines the chalk and subjacent
strata. About the year 1716 there was a remarkable sinking of a tract of
land near the sea, so that houses became visible from certain points at
sea, and from particular spots on the sea cliffs, from whence they could
not be seen previously. In the description of this subsidence in the
Phil. Trans. 1716, it is said, "that the land consisted of a solid stony
mass (chalk), resting on wet clay (gault), so that it slid forwards
towards the sea, just as a ship is launched on tallowed planks." It is
also stated that, within the memory of persons then living, the cliff
there had been washed away to the extent of ten rods.
Encroachments of the sea at Hythe are also on record; but between this
point and Rye there has been a gain of land within the times of history;
the rich level tract called Romney Marsh, or Dungeness, about ten miles
in width and five in breadth, and formed of silt, having received great
accession. It has been necessary, however, to protect it from the sea,
from the earliest periods, by embankments, the towns of Lydd and Romney
being the only parts of the marsh above the level of the highest
tides.[419] Mr. Redman has cited numerous old charts and trustworthy
authorities to prove that the average annual increase of the promontory
of shingle called Dungeness amounted for two centuries, previous to
1844, to nearly six yards. Its progress, however, has fluctuated during
that period; for between 1689 and 1794, a term of 105 years, the rate
was as much as 8-1/4 yards per annum.[420] It is ascertained that the
shingle is derived from the westward. Whether the pebbles are stopped by
the meeting of the tide from the north flowing through the Straits of
Dover, with that which comes up the Channel from the west, as was
formerly held, or by the check given to the tidal current by the waters
of the Rother, as some maintain, is still a disputed question.
Rye, situated to the south of Romney Marsh, was once destroyed by the
sea, but it is now two miles distant from it. The neighboring town of
Winchelsea was destroyed in the reign of Edward I., the mouth of the
Rother stopped up, and the river diverted into another channel. In its
old bed, an ancient vessel, apparently a Dutch merchantman, was found
about the year 1824. It was built entirely of oak, and much
blackened.[421] Large quantities of hazel-nuts, peat, and wood are found
in digging in Romney Marsh.
_South coast of England._--Westward of Hastings, or of St. Leonard's,
the shore line has been giving way as far as Pevensey Bay, where
formerly there existed a haven now entirely blocked up by shingle. The
degradation has equalled for a series of years seven feet per annum in
some places, and several martello towers had in consequence, before
1851, been removed by the Ordnance.[422] At the promontory of Beachy
Head a mass of chalk, three hundred feet in length, and from seventy to
eighty in breadth, fell in the year 1813 with a tremendous crash; and
similar slips have since been frequent.[423]
About a mile to the west of the town of Newhaven, the remains of an
ancient intrenchment are seen on the brow of Castle Hill. This
earth-work, supposed to be Roman, was evidently once of considerable
extent and of an oval form, but the greater part has been cut away by
the sea. The cliffs, which are undermined here, are high; more than one
hundred feet of chalk being covered by tertiary clay and sand, from
sixty to seventy feet in thickness. In a few centuries the last vestiges
of the plastic clay formation on the southern borders of the chalk of
the South Downs on this coast will probably be annihilated, and future
geologists will learn, from historical documents, the ancient
geographical boundaries of this group of strata in that direction. On
the opposite side of the estuary of the Ouse, on the east of Newhaven
harbor, a bed of shingle, composed of chalk flints derived from the
waste of the adjoining cliffs, had accumulated at Seaford for several
centuries. In the great storm of November, 1824, this bank was entirely
swept away, and the town of Seaford inundated. Another great beach of
shingle is now forming from fresh materials.
The whole coast of Sussex has been incessantly encroached upon by the
sea from time immemorial; and, although sudden inundations only, which
overwhelmed fertile or inhabited tracts, are noticed in history, the
records attest an extraordinary amount of loss. During a period of no
more than eighty years, there are notices of about _twenty_ inroads, in
which tracts of land of from twenty to _four hundred acres_ in extent
were overwhelmed at once, the value of the tithes being mentioned in the
Taxatio Ecclesiastica.[424] In the reign of Elizabeth, the town of
Brighton was situated on that tract where the chain pier now extends
into the sea. In the year 1665, twenty-two tenements had been destroyed
under the cliff. At that period there still remained under the cliff 113
tenements, the whole of which were overwhelmed in 1703 and 1705. No
traces of the ancient town are now perceptible, yet there is evidence
that the sea has merely resumed its ancient position at the base of the
cliffs, the site of the whole town having been merely a beach abandoned
by the ocean for ages.
_Hampshire.--Isle of Wight._--It would be endless to allude to all the
localities on the Sussex and Hampshire coasts where the land has given
way; but I may point out the relation which the geological structure of
the Isle of Wight bears to its present shape, as attesting that the
coast owes its outline to the continued action of the sea. Through the
middle of the island runs a high ridge of chalk strata, in a vertical
position, and in a direction east and west. This chalk forms the
projecting promontory of Culver Cliff on the east, and of the Needles on
the west; while Sandown Bay on the one side, and Compton Bay on the
other, have been hollowed out of the softer sands and argillaceous
strata, which are inferior, in geological position, to the chalk.
The same phenomena are repeated in the Isle of Purbeck, where the line
of vertical chalk forms the projecting promontory of Handfast Point; and
Swanage Bay marks the deep excavation made by the waves in the softer
strata, corresponding to those of Sandown Bay.
_Hurst Castle bank--progressive motion of sea beaches._--Although the
loose pebbles and grains of sand composing any given line of sea-beach
are carried sometimes one way, sometimes another, they have,
nevertheless, an ultimate motion in one particular direction.[425] Their
progress, for example, on the south coast of England, is from west to
east, which is owing partly to the action of the waves driven eastwards
by the prevailing wind, and partly to the current, or the motion of the
general body of water caused by the tides and winds. The force of the
waves gives motion to pebbles which the velocity of the currents alone
would be unable to carry forwards; but as the pebbles are finally
reduced to sand or mud, by continual attrition, they are brought within
the influence of a current; and this cause must determine the course
which the main body of matter derived from wasting cliffs will
eventually take.
It appears, from the observations of Mr. Palmer and others, that if a
pier or groin be erected anywhere on our southern or southeastern coast
to stop the progress of the beach, a heap of shingle soon collects on
the western side of such artificial barriers. The pebbles continue to
accumulate till they rise as high as the pier or groin, after which they
pour over in great numbers during heavy gales.[426]
The western entrance of the Channel, called the Solent, is crossed for
more than two-thirds of its width by the shingle-bank of Hurst Castle,
which is about two miles long, seventy yards broad, and twelve feet
high, presenting an inclined plane to the west. This singular bar
consists of a bed of rounded chalk flints, resting on a submarine
argillaceous base. The flints and a few other pebbles, intermixed, are
derived from the waste of Hordwell, and other cliffs to the westward,
where tertiary strata, capped with a covering of broken chalk flints,
from five to fifty feet thick, are rapidly undermined. In the great
storm of November, 1824, this bank of shingle was moved bodily forwards
for forty yards towards the northeast; and certain piles, which served
to mark the boundaries of two manors, were found after the storm on the
opposite side of the bar. At the same time many acres of pasture land
were covered by shingle, on the farm of Westover, near Lymington. But
the bar was soon restored in its old position by pebbles drifted from
the west; and it appears from ancient maps that it has preserved the
same general outline and position for centuries.[427]
Mr. Austen remarks that, as a general rule, it is only when high tides
concur with a gale of wind, that the sea reaches the base of cliffs so
as to undermine them and throw down earth and stone. But the waves are
perpetually employed in abrading and fashioning the materials already
strewed over the beach. Much of the gravel and shingle is always
travelling up and down, between high-water mark and a slight depth below
the level of the lowest tides, and occasionally the materials are swept
away and carried into deeper water. Owing to these movements every
portion of our southern coast may be seen at one time or other in the
condition of bare rock. Yet other beds of sand and shingle soon collect,
and, although composed of new materials, invariably exhibit on the same
spots precisely similar characters.[428]
The cliffs between Hurst Shingle Bar and Christchurch are undermined
continually, the sea having often encroached for a series of years at
the rate of a yard annually. Within the memory of persons now living, it
has been necessary thrice to remove the coast-road farther inland. The
tradition, therefore, is probably true, that the church of Hordwell was
once in the middle of that parish, although now (1830) very near the
sea. The promontory of Christchurch Head gives way slowly. It is the
only point between Lymington and Poole Harbor, in Dorsetshire, where any
hard stony masses occur in the cliffs. Five layers of large ferruginous
concretions, somewhat like the septaria of the London clay, have
occasioned a resistance at this point, to which we may ascribe this
headland. In the mean time, the waves have cut deeply into the soft
sands and loam of Poole Bay; and, after severe frosts, great landslips
take place, which by degrees become enlarged into narrow ravines, or
chines, as they are called, with vertical sides. One of these chines,
near Boscomb, has been deepened twenty feet within a few years. At the
head of each there is a spring, the waters of which have been chiefly
instrumental in producing these narrow excavations, which are sometimes
from 100 to 150 feet deep.
_Isle of Portland._--The peninsulas of Purbeck and Portland are
continually wasting away. In the latter, the soft argillaceous
substratum (Kimmeridge clay) hastens the dilapidation of the
superincumbent mass of limestone.
In 1655 the cliffs adjoining the principal quarries in Portland gave way
to the extent of one hundred yards, and fell into the sea; and in
December, 1734, a slide to the extent of 150 yards occurred on the east
side of the isle, by which several skeletons buried between slabs of
stone, were discovered. But a much more memorable occurrence of this
nature, in 1792, occasioned probably by the undermining of the cliffs,
is thus described in Hutchin's History of Dorsetshire:--"Early in the
morning the road was observed to crack: this continued increasing, and
before two o'clock the ground had sunk several feet, and was in one
continued motion, but attended with no other noise than what was
occasioned by the separation of the roots and brambles, and now and then
a falling rock. At night it seemed to stop a little, but soon moved
again; and, before morning, the ground from the top of the cliff to the
water-side had sunk in some places fifty feet perpendicular. The extent
of ground that moved was about _a mile and a quarter_ from north to
south, and 600 yards from east to west."
_Formation of the Chesil Bank._--Portland is connected with the mainland
by the Chesil Bank, a ridge of shingle about seventeen miles in length,
and, in most places, nearly a quarter of a mile in breadth. The pebbles
forming this immense barrier are chiefly siliceous, all loosely thrown
together, and rising to the height of from twenty to thirty feet above
the ordinary high-water mark; and at the southeastern end, which is
nearest the Isle of Portland, where the pebbles are largest, forty feet.
The fundamental rocks whereon the shingle rests are found at the depth
of a few yards only below the level of the sea. The formation of that
part of the bar which attaches Portland to the mainland may have been
due to an original shoal or reef, or to the set of the tides in the
narrow channel, by which the course of the pebbles, which are always
coming from the west, has been arrested. It is a singular fact that,
throughout the Chesil Bank, the pebbles increase gradually in size as we
proceed southeastward, or as we go farther from the quarter which
supplied them. Had the case been reversed, we should naturally have
attributed the circumstance to the constant wearing down of the pebbles
by friction, as they are rolled along a beach seventeen miles in length.
But the true explanation of the phenomenon is doubtless this: the tidal
current runs strongest from west to east, and its power is greater in
the more open channel or farther from the land. In other words its force
increases southwards, and as the direction of the bank is from northwest
to southeast, the size of the masses coming from the westward and thrown
ashore must always be largest where the motion of the water is most
violent. Colonel Reid states that all calcareous stones rolled along
from the west are soon ground into sand, and in this form they pass
round Portland Island.[429]
The storm of 1824 burst over the Chesil Bank with great fury, and the
village of Chesilton, built upon its southern extremity, was
overwhelmed, with many of the inhabitants. The same storm carried away
part of the Breakwater at Plymouth, and huge masses of rock, from two to
five tons in weight, were lifted from the bottom of the weather side,
and rolled fairly to the top of the pile. One block of limestone,
weighing seven tons, was washed round the western extremity of the
Breakwater, and carried 150 feet.[430] The propelling power is derived
in these cases from the breaking of the waves, which run fastest in
shallow water, and for a short space far exceed the most rapid currents
in swiftness. It was in the same month, and also during a spring-tide,
that a great flood is mentioned on the coasts of England, in the year
1099. Florence of Worcester says, "On the third day of the nones of Nov.
1099, the sea came out upon the shore and buried towns and men very
many, and oxen and sheep innumerable." We also read in the Saxon
Chronicle, for the year 1099, "This year eke on St. Martin's mass day,
the 11th of Novembre, sprung up so much of the sea flood, and so myckle
harm did, as no man minded that it ever afore did, and there was the ylk
day a new moon."
South of the Bill, or southern point of Portland, is a remarkable shoal
in the channel at the depth of seven fathoms, called "the Shambles,"
consisting entirely of rolled and broken shells of Purpura lapillus,
Mytilus edulis, and other species now living. This mass of light
materials is always in motion, varying in height from day to day, and
yet the shoal remains constant.
_Dorsetshire.--Devonshire._--At Lyme Regis, in Dorsetshire, the "Church
Cliffs," as they are called, consisting of lias about one hundred feet
in height, gradually fell away at the rate of one yard a year, from 1800
to 1829.[431]
[Illustration: Fig. 36.
Landslip, near Axmouth, Dec. 1839. (Rev. W. D. Conybeare.)
A. Tract of Downs still remaining at their original level.
B. New ravine.
C, D. Sunk and fractured strip united to A, before the convulsion.
D, E. Bendon undercliff as before, but more fissured, and thrust
forward about fifty feet, towards the sea.
F. Pyramidal crag, sunk from seventy to twenty feet in height.
G. New reef upheaved from the sea.
]
An extraordinary landslip occurred on the 24th of December, 1839, on the
coast between Lyme Regis and Axmouth, which has been described by the
Rev. W. D. Conybeare, to whose kindness I am indebted for the
accompanying section, fig. 36. The tract of downs ranging there along
the coast is capped by chalk (_h_), which rests on sandstone,
alternating with chert (_i_), beneath which is more than 100 feet of
loose sand (_k_), with concretions at the bottom, and belonging like _i_
to the green-sand formation; the whole of the above masses, _h_, _i_,
_k_, reposing on retentive beds of clay (_l_), belonging to the lias,
which shelves towards the sea. Numerous springs issuing from the loose
sand (_k_), have gradually removed portions of it, and thus undermined
the superstratum, so as to have caused subsidences at former times, and
to have produced a line of undercliff between D and E. In 1839 an
excessively wet season had saturated all the rocks with moisture, so as
to increase the weight of the incumbent mass, from which the support had
already been withdrawn by the action of springs. Thus the superstrata
were precipitated into hollows prepared for them, and the adjacent
masses of partially undermined rock, to which the movement was
communicated, were made to slide down on a slippery basis of watery sand
towards the sea. These causes gave rise to a convulsion, which began on
the morning of the 24th of December, with a crashing noise; and, on the
evening of the same day, fissures were seen opening in the ground, and
the walls of tenements rending and sinking, until a deep chasm or
ravine, B, was formed, extending nearly three-quarters of a mile in
length, with a depth of from 100 to 150 feet, and a breadth exceeding
240 feet. At the bottom of this deep gulf lie fragments of the original
surface thrown together in the wildest confusion. In consequence of
lateral movements, the tract intervening between the new fissure and the
sea, including the ancient undercliff, was fractured, and the whole line
of sea-cliff carried bodily forwards for many yards. "A remarkable
pyramidal crag, F, off Culverhole Point, which lately formed a
distinguishing landmark, has sunk from a height of about seventy to
twenty feet, and the main cliff, E, before more than fifty feet distant
from this insulated crag, is now brought almost close to it. This motion
of the sea-cliff has produced a farther effect, which may rank among the
most striking phenomena of this catastrophe. The lateral pressure of the
descending rocks has urged the neighboring strata, extending beneath the
shingle of the shore, by their state of unnatural condensation, to burst
upwards in a line parallel to the coast--thus an elevated ridge, G, more
than a mile in length, and rising more than forty feet, covered by a
confused assemblage of broken strata, and immense blocks of rock,
invested with sea-weed and corallines, and scattered over with shells
and star-fish, and other productions of the deep, forms an extended reef
in front of the present range of cliffs."[432]
A full account of this remarkable landslip, with a plan, sections, and
many fine illustrative drawings, was published by Messrs. Conybeare and
Buckland,[433] from one of which the annexed cut has been reduced, fig.
37.
[Illustration: Fig. 37.
View of the Axmouth landslip from Great Bindon, looking westward to the
Sidmouth hills, and estuary of the Exe. From an original drawing by Mrs.
Buckland.]
_Cornwall._--Near Penzance, in Cornwall, there is a projecting tongue of
land, called the "Green," formed of granitic sand, from which more than
thirty acres of pasture land have been gradually swept away, in the
course of the last two or three centuries.[434] It is also said that St.
Michael's Mount, now an insular rock, was formerly situated in a wood,
several miles from the sea; and its old Cornish name (Caraclowse in
Cowse) signifies, according to Carew, the Hoar Rock in the wood.[435]
Between the Mount and Newlyn there is seen under the sand, black
vegetable mould, full of hazel-nuts, and the branches, leaves, roots,
and trunks of forest-trees, all of indigenous species. This stratum has
been traced seaward as far as the ebb permits, and many proofs of a
submerged vegetable accumulation, with stumps of trees in the position
in which they grew, have been traced, says Sir Henry De la Beche, round
the shores of Devon, Cornwall, and Western Somerset. The facts not only
indicate a change in the relative level of the sea and land, since the
species of animals and plants were the same as those now living in this
district; but, what is very remarkable, there seems evidence of the
submergence having been effected, in part at least, since the country
was inhabited by man.[436]
A submarine forest occurring at the mouth of the Parret in
Somersetshire, on the south side of the Bristol Channel, was described
by Mr. L. Horner, in 1815, and its position attributed to subsidence. A
bed of peat is there seen below the level of the sea, and the trunks of
large trees, such as the oak and yew, having their roots still
diverging as they grew, and fixed in blue clay.[437]
_Tradition of loss of land in Cornwall._--The oldest historians mention
a tradition in Cornwall, of the submersion of the Lionnesse, a country
said to have stretched from the Land's End to the Scilly Islands. The
tract, if it existed, must have been thirty miles in length, and perhaps
ten in breadth. The land now remaining on either side is from two
hundred to three hundred feet high; the intervening sea about three
hundred feet deep. Although there is no authentic evidence for this
romantic tale, it probably originated in some former inroads of the
Atlantic, accompanying, perhaps, a subsidence of land on this
coast.[438]
_West coast of England._--Having now brought together an ample body of
proofs of the destructive operations of the waves, tides, and currents,
on our eastern and southern shores, it will be unnecessary to enter into
details of changes on the western coast, for they present merely a
repetition of the same phenomena, and in general on an inferior scale.
On the borders of the estuary of the Severn the flats of Somersetshire
and Gloucestershire have received enormous accessions, while, on the
other hand, the coast of Cheshire, between the rivers Mersey and Dee,
has lost, since the year 1764, many hundred yards, and some affirm more
than half a mile, by the advance of the sea upon the abrupt cliffs of
red clay and marls. Within the period above mentioned several
lighthouses have been successively abandoned.[439] There are traditions
in Pembrokeshire[440] and Cardiganshire[441] of far greater losses of
territory than that which the Lionnesse tale of Cornwall pretends to
commemorate. They are all important, as demonstrating that the earliest
inhabitants were familiar with the phenomenon of incursions of the sea.
_Loss of land on the coast of France._--The French coast, particularly
that part of Brittany, where the tides rise to an extraordinary height,
is the constant prey of the waves. In the ninth century many villages
and woods are reported to have been carried away, the coast undergoing
great change, whereby the hill of St. Michael was detached from the
mainland. The parish of Bourgneuf, and several others in that
neighborhood, were overflowed in the year 1500. In 1735, during a great
storm, the ruins of Palnel were seen uncovered in the sea.[442]