Chapter 6 (third part)

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ON THE ABSENCE OF ACTIVE VOLCANOES
IN THE AREAS OF SUBSIDENCE, AND ON
THEIR FREQUENT PRESENCE IN THE AREAS
OF ELEVATION.

Before making some concluding remarks
on the relations of the spaces
coloured blue and red, it will be
convenient to consider the position on
our map of the volcanoes historically
known to have been in action.  It is
impossible not to be struck, first with
the absence of volcanoes in the great areas of subsidence tinted pale
and dark blue,--namely, in the central parts of the Indian Ocean,
in the China Sea, in the sea between the barriers of Australia and
New Caledonia, in the Caroline, Marshall, Gilbert, and Low Archipelagoes;
and, secondly, with the coincidence of the principal volcanic chains
with the parts coloured red, which indicates the presence of
fringing-reefs; and, as we have just seen, the presence in most
cases of upraised organic remains of a modern date.  I may here remark
that the reefs were all coloured before the volcanoes were added to the map, or
indeed before I knew of the existence of several of them.

The volcano in Torres Strait, at the northern point of Australia, is that
which lies nearest to a large subsiding area, although situated 125 miles
within the outer margin of the actual barrier-reef.  The Great Comoro
Island, which probably contains a volcano, is only twenty miles distant
from the barrier-reef of Mohila; Ambil volcano, in the Philippines, is
distant only a little more than sixty miles from the atoll-formed Appoo
reef: and there are two other volcanoes in the map within ninety miles of
circles coloured blue.  These few cases, which thus offer partial
exceptions to the rule, of volcanoes being placed remote from the areas of
subsidence, lie either near single and isolated atolls, or near small
groups of encircled islands; and these by our theory can have, in few
instances, subsided to the same amount in depth or area, as groups of
atolls.  There is not one active volcano within several hundred miles of an
archipelago, or even a small group of atolls.  It is, therefore, a striking
fact that in the Friendly Archipelago, which owes its origin to the
elevation of a group of atolls, two volcanoes, and, perhaps, others are
known to be in action: on the other hand, on several of the encircled
islands in the Pacific, supposed by our theory to have subsided, there are
old craters and streams of lava, which show the effects of past and ancient
eruptions.  In these cases, it would appear as if the volcanoes had come
into action, and had become extinguished on the same spots, according as
the elevating or subsiding movements prevailed.

There are some other coasts on the map, where volcanoes in a state of
action concur with proofs of recent elevation, besides those coloured red
from being fringed by coral-reefs.  Thus I hope to show in a future volume,
that nearly the whole line of the west coast of South America, which forms
the greatest volcanic chain in the world, from near the equator for a space
of between 2,000 and 3,000 miles southward, has undergone an upward
movement during a late geological period.  The islands on the north-western
shores of the Pacific, which form the second greatest volcanic chain, are
very imperfectly known; but Luzon, in the Philippines, and the Loo Choo
Islands, have been recently elevated; and at Kamtschatka (At Sedanka, in
latitude 58 deg N. (Von Buch's "Descrip. des Isles Canaries," page 455).
In a forthcoming part, I shall give the evidence referred to with respect
to the elevation of New Zealand.) there are extensive tertiary beds of
modern date.  Evidence of the same nature, but not very satisfactory, may
be detected in Northern New Zealand where there are two volcanoes.  The
co-existence in other parts of the world of active volcanoes, with upraised
beds of a modern tertiary origin, will occur to every geologist.  (During
the subterranean disturbances which took place in Chile, in 1835, I have
shown ("Geolog. Trans." 2nd Ser., vol. v., page 606) that at the same
moment that a large district was upraised, volcanic matter burst forth at
widely separated points, through both new and old vents.)  Nevertheless,
until it could be shown that volcanoes were inactive, or did not exist in
subsiding areas, the conclusion that their distribution depended on the
nature of the subterranean movements in progress, would have been
hazardous.  But now, viewing the appended map, it may, I think, be
considered as almost established, that volcanoes are often (not necessarily
always) present in those areas where the subterranean motive power has
lately forced, or is now forcing outwards, the crust of the earth, but that
they are invariably absent in those, where the surface has lately subsided
or is still subsiding.  (We may infer from this rule, that in any old
deposit, which contains interstratified beds of erupted matter, there was
at the period, and in the area of its formation, a TENDENCY to an upward
movement in the earth's surface, and certainly no movement of subsidence.)

ON THE RELATIONS OF THE AREAS OF SUBSIDENCE AND ELEVATION.

The immense surfaces on the map, which, both by our theory and by the plain
evidence of upraised marine remains, have undergone a change of level
either downwards or upwards during a late period, is a most remarkable
fact.  The existence of continents shows that the areas have been immense
which at some period have been upraised; in South America we may feel sure,
and on the north-western shores of the Indian Ocean we may suspect, that
this rising is either now actually in progress, or has taken place quite
recently.  By our theory, we may conclude that the areas are likewise
immense which have lately subsided, or, judging from the earthquakes
occasionally felt and from other appearances, are now subsiding.  The
smallness of the scale of our map should not be overlooked: each of the
squares on it contains (not allowing for the curvature of the earth)
810,000 square miles.  Look at the space of ocean from near the southern
end of the Low Archipelago to the northern end of the Marshall Archipelago,
a length of 4,500 miles, in which, as far as is known, every island, except
Aurora which lies just without the Low Archipelago, is atoll-formed.  The
eastern and western boundaries of our map are continents, and they are
rising areas: the central spaces of the great Indian and Pacific Oceans,
are mostly subsiding; between them, north of Australia, lies the most
broken land on the globe, and there the rising parts are surrounded and
penetrated by areas of subsidence (I suspect that the Arru and Timor-laut
Islands present an included small area of subsidence, like that of the
China Sea, but I have not ventured to colour them from my imperfect
information, as given in the Appendix.), so that the prevailing movements
now in progress, seem to accord with the actual states of surface of the
great divisions of the world.

The blue spaces on the map are nearly all elongated; but it does not
necessarily follow from this (a caution, for which I am indebted to Mr.
Lyell), that the areas of subsidence were likewise elongated; for the
subsidence of a long, narrow space of the bed of the ocean, including in it
a transverse chain of mountains, surmounted by atolls, would only be marked
on the map by a transverse blue band.  But where a chain of atolls and
barrier-reefs lies in an elongated area, between spaces coloured red, which
therefore have remained stationary or have been upraised, this must have
resulted either from the area of subsidence having originally been
elongated (owing to some tendency in the earth's crust thus to subside), or
from the subsiding area having originally been of an irregular figure, or
as broad as long, and having since been narrowed by the elevation of
neighbouring districts.  Thus the areas, which subsided during the
formation of the great north and south lines of atolls in the Indian
Ocean,--of the east and west line of the Caroline atolls,--and of the
north-west and south-east line of the barrier-reefs of New Caledonia and
Louisiade, must have originally been elongated, or if not so, they must
have since been made elongated by elevations, which we know to belong to a
recent period.

I infer from Mr. Hopkins' researches ("Researches in Physical Geology,"
Transact. Cambridge Phil. Soc., volume vi, part i.), that for the formation
of a long chain of mountains, with few lateral spurs, an area elongated in
the same direction with the chain, must have been subjected to an elevatory
movement.  Mountain-chains, however, when already formed, although running
in very different directions, it seems (For instance in S. America from
latitude 34 deg, for very many degrees southward there are upraised beds
containing recent species of shells, on both the Atlantic and Pacific side
of the continent, and from the gradual ascent of the land, although with
very unequal slopes, on both sides towards the Cordillera, I think it can
hardly be doubted that the entire width has been upraised in mass within
the recent period.  In this case the two W.N.W. and E.S.E. mountain-lines,
namely the Sierra Ventana and the S. Tapalguen, and the great north and
south line of the Cordillera have been together raised.  In the West Indies
the N. and S. line of the Eastern Antilles, and the E. and W. line of
Jamaica, appear both to have been upraised within the latest geological
period.) may be raised together by a widely-acting force: so, perhaps,
mountain-chains may subside together.  Hence, we cannot tell, whether the
Caroline and Marshall Archipelagoes, two groups of atolls running in
different directions and meeting each other, have been formed by the
subsidence of two areas, or of one large area, including two distinct lines
of mountains.  We have, however, in the southern prolongation of the
Mariana Islands, probable evidence of a line of recent elevation having
intersected one of recent subsidence.  A view of the map will show that,
generally, there is a tendency to alternation in the parallel areas
undergoing opposite kinds of movement; as if the sinking of one area
balanced the rising of another.

The existence in many parts of the world of high table-land, proves that
large surfaces have been upraised in mass to considerable heights above the
level of the ocean; although the highest points in almost every country
consist of upturned strata, or erupted matter: and from the immense spaces
scattered with atolls, which indicate that land originally existed there,
although not one pinnacle now remains above the level of the sea, we may
conclude that wide areas have subsided to an amount, sufficient to bury not
only any formerly existing table-land, but even the heights formed by
fractured strata, and erupted matter.  The effects produced on the land by
the later elevatory movements, namely, successively rising cliffs, lines of
erosion, and beds of literal shells and pebbles, all requiring time for
their production, prove that these movements have been very slow; we can,
however, infer this with safety, only with respect to the few last hundred
feet of rise.  But with reference to the whole vast amount of subsidence,
necessary to have produced the many atolls widely scattered over immense
spaces, it has already been shown (and it is, perhaps, the most interesting
conclusion in this volume), that the movements must either have been
uniform and exceedingly slow, or have been effected by small steps,
separated from each other by long intervals of time, during which the
reef-constructing polypifers were able to bring up their solid frameworks
to the surface.  We have little means of judging whether many considerable
oscillations of level have generally occurred during the elevation of large
tracts; but we know, from clear geological evidence, that this has
frequently taken place; and we have seen on our map, that some of the same
islands have both subsided and been upraised.  I conclude, however, that
most of the large blue spaces, have subsided without many and great
elevatory oscillations, because only a few upraised atolls have been
observed: the supposition that such elevations have taken place, but that
the upraised parts have been worn down by the surf, and thus have escaped
observation, is overruled by the very considerable depth of the lagoons of
all the larger atolls; for this could not have been the case, if they had
suffered repeated elevations and abrasion.  From the comparative
observations made in these latter pages, we may finally conclude, that the
subterranean changes which have caused some large areas to rise, and others
to subside, have acted in a very similar manner.

RECAPITULATION.

In the three first chapters, the principal kinds of coral-reefs were
described in detail, and they were found to differ little, as far as
relates to the actual surface of the reef.  An atoll differs from an
encircling barrier-reef only in the absence of land within its central
expanse; and a barrier-reef differs from a fringing-reef, in being placed
at a much greater distance from the land with reference to the probable
inclination of its submarine foundation, and in the presence of a deep-water
lagoon-like space or moat within the reef.  In the fourth chapter the
growing powers of the reef-constructing polypifers were discussed; and it
was shown, that they cannot flourish beneath a very limited depth.  In
accordance with this limit, there is no difficulty respecting the
foundations on which fringing-reefs are based; whereas, with barrier-reefs
and atolls, there is a great apparent difficulty on this head; in
barrier-reefs from the improbability of the rock of the coast or of banks of
sediment extending, in every instance, so far seaward within the required
depth;--and in atolls, from the immensity of the spaces over which they are
interspersed, and the apparent necessity for believing that they are all
supported on mountain-summits, which although rising very near to the
surface-level of the sea, in no one instance emerge above it.  To escape
this latter most improbable admission, which implies the existence of
submarine chains of mountains of almost the same height, extending over
areas of many thousand square miles, there is but one alternative; namely,
the prolonged subsidence of the foundations, on which the atolls were
primarily based, together with the upward growth of the reef-constructing
corals.  On this view every difficulty vanishes; fringing reefs are thus
converted into barrier-reefs; and barrier-reefs, when encircling islands,
are thus converted into atolls, the instant the last pinnacle of land sinks
beneath the surface of the ocean.

Thus the ordinary forms and certain peculiarities in the structure of
atolls and barrier-reefs can be explained;--namely, the wall-like structure
on their inner sides, the basin or ring-like shape both of the marginal and
central reefs in the Maldiva atolls--the union of some atolls as if by a
ribbon--the apparent disseverment of others--and the occurrence, in atolls
as well as in barrier-reefs, of portions of reef, and of the whole of some
reefs, in a dead and submerged state, but retaining the outline of living
reefs.  Thus can be explained the existence of breaches through barrier-reefs
in front of valleys, though separated from them by a wide space of
deep water; thus, also, the ordinary outline of groups of atolls and the
relative forms of the separate atolls one to another; thus can be explained
the proximity of the two kinds of reefs formed during subsidence, and their
separation from the spaces where fringing-reefs abound.  On searching for
other evidence of the movements supposed by our theory, we find marks of
change in atolls and in barrier-reefs, and of subterranean disturbances
under them; but from the nature of things, it is scarcely possible to
detect any direct proofs of subsidence, although some appearances are
strongly in favour of it.  On the fringed coasts, however, the presence of
upraised marine bodies of a recent epoch, plainly show, that these coasts,
instead of having remained stationary, which is all that can be directly
inferred from our theory, have generally been elevated.

Finally, when the two great types of structure, namely barrier-reefs and
atolls on the one hand, and fringing-reefs on the other, were laid down in
colours on our map, a magnificent and harmonious picture of the movements,
which the crust of the earth has within a late period undergone, is
presented to us.  We there see vast areas rising, with volcanic matter
every now and then bursting forth through the vents or fissures with which
they are traversed.  We see other wide spaces slowly sinking without any
volcanic outburst, and we may feel sure, that this sinking must have been
immense in amount as well as in area, thus to have buried over the broad
face of the ocean every one of those mountains, above which atolls now
stand like monuments, marking the place of their former existence.
Reflecting how powerful an agent with respect to denudation, and
consequently to the nature and thickness of the deposits in accumulation,
the sea must ever be, when acting for prolonged periods on the land, during
either its slow emergence or subsidence; reflecting, also, on the final
effects of these movements in the interchange of land and ocean-water on
the climate of the earth, and on the distribution of organic beings, I may
be permitted to hope, that the conclusions derived from the study of
coral-formations, originally attempted merely to explain their peculiar
forms, may be thought worthy of the attention of geologists.

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Chapter 4 - Section 4.I

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CHAPTER IV.--ON THE DISTRIBUTION AND GROWTH OF CORAL-REEFS.

In this chapter I will give all the facts which I have collected, relating
to the distribution of coral-reefs,--to the conditions favourable to their
increase,--to the rate of their growth,--and to the depth at which they are
formed.

These subjects have an important bearing on the theory of the origin of the
different classes of coral-reefs.


SECTION 4.I.--ON THE DISTRIBUTION OF CORAL-REEFS, AND ON THE CONDITIONS
FAVOURABLE TO THEIR INCREASE.

With regard to the limits of latitude, over which coral-reefs extend, I
have nothing new to add.  The Bermuda Islands, in 32 deg 15' N., is the
point furthest removed from the equator, in which they appear to exist; and
it has been suggested that their extension so far northward in this
instance is owing to the warmth of the Gulf Stream.  In the Pacific, the
Loo Choo Islands, in latitude 27 deg N., have reefs on their shores, and
there is an atoll in 28 deg 30', situated N.W. of the Sandwich Archipelago.
In the Red Sea there are coral-reefs in latitude 30 deg.  In the southern
hemisphere coral-reefs do not extend so far from the equatorial sea.  In
the Southern Pacific there are only a few reefs beyond the line of the
tropics, but Houtmans Abrolhos, on the western shores of Australia in
latitude 29 deg S., are of coral formation.

The proximity of volcanic land, owing to the lime generally evolved from
it, has been thought to be favourable to the increase of coral-reefs.
There is, however, not much foundation for this view; for nowhere are
coral-reefs more extensive than on the shores of New Caledonia, and of
north-eastern Australia, which consist of primary formations; and in the
largest groups of atolls, namely the Maldiva, Chagos, Marshall, Gilbert,
and Low Archipelagoes, there is no volcanic or other kind of rock,
excepting that formed of coral.

The entire absence of coral-reefs in certain large areas within the
tropical seas, is a remarkable fact.  Thus no coral-reefs were observed,
during the surveying voyages of the "Beagle" and her tender on the west
coast of South America south of the equator, or round the Galapagos
Islands.  It appears, also, that there are none (I have been informed that
this is the case, by Lieutenant Ryder, R.N., and others who have had ample
opportunities for observation.) north of the equator; Mr. Lloyd, who
surveyed the Isthmus of Panama, remarked to me, that although he had seen
corals living in the Bay of Panama, yet he had never observed any reefs
formed by them.  I at first attributed this absence of reefs on the coasts
of Peru and of the Galapagos Islands (The mean temperature of the surface
sea from observations made by the direction of Captain Fitzroy on the
shores of the Galapagos Islands, between the 16th of September and the 20th
of October, 1835, was 68 deg Fahr.  The lowest temperature observed was
58.5 deg at the south-west end of Albemarle Island; and on the west coast
of this island, it was several times 62 deg and 63 deg.  The mean
temperature of the sea in the Low Archipelago of atolls, and near Tahiti,
from similar observations made on board the "Beagle", was (although further
from the equator) 77.5 deg, the lowest any day being 76.5 deg.  Therefore
we have here a difference of 9.5 deg in mean temperature, and 18 deg in
extremes; a difference doubtless quite sufficient to affect the
distribution of organic beings in the two areas.), to the coldness of the
currents from the south, but the Gulf of Panama is one of the hottest
pelagic districts in the world.  (Humboldt's "Personal Narrative," volume
vii., page 434.)  In the central parts of the Pacific there are islands
entirely free from reefs; in some few of these cases I have thought that
this was owing to recent volcanic action; but the existence of reefs round
the greater part of Hawaii, one of the Sandwich Islands, shows that recent
volcanic action does not necessarily prevent their growth.

In the last chapter I stated that the bottom of the sea round some islands
is thickly coated with living corals, which nevertheless do not form reefs,
either from insufficient growth, or from the species not being adapted to
contend with the breaking waves.

I have been assured by several people, that there are no coral-reefs on the
west coast of Africa (It might be concluded, from a paper by Captain Owen
("Geographical Journal", volume ii., page 89), that the reefs off Cape St.
Anne and the Sherboro' Islands were of coral, although the author states
that they are not purely coralline.  But I have been assured by Lieutenant
Holland, R.N., that these reefs are not of coral, or at least that they do
not at all resemble those in the West Indies.), or round the islands in the
Gulf of Guinea.  This perhaps may be attributed, in part, to the sediment
brought down by the many rivers debouching on that coast, and to the
extensive mud-banks, which line great part of it.  But the islands of St.
Helena, Ascension, the Cape Verdes, St. Paul's, and Fernando Noronha, are,
also, entirely without reefs, although they lie far out at sea, are
composed of the same ancient volcanic rocks, and have the same general
form, with those islands in the Pacific, the shores of which are surrounded
by gigantic walls of coral-rock.  With the exception of Bermuda, there is
not a single coral-reef in the central expanse of the Atlantic Ocean.  It
will, perhaps, be suggested that the quantity of carbonate of lime in
different parts of the sea, may regulate the presence of reefs.  But this
cannot be the case, for at Ascension, the waves charged to excess
precipitate a thick layer of calcareous matter on the tidal rocks; and at
St. Jago, in the Cape Verdes, carbonate of lime not only is abundant on the
shores, but it forms the chief part of some upraised post-tertiary strata.
The apparently capricious distribution, therefore, of coral-reefs, cannot
be explained by any of these obvious causes; but as the study of the
terrestrial and better known half of the world must convince every one that
no station capable of supporting life is lost,--nay more, that there is a
struggle for each station, between the different orders of nature,--we may
conclude that in those parts of the intertropical sea, in which there are
no coral-reefs, there are other organic bodies supplying the place of the
reef-building polypifers.  It has been shown in the chapter on Keeling
atoll that there are some species of large fish, and the whole tribe of
Holothuriae which prey on the tenderer parts of the corals.  On the other
hand, the polypifers in their turn must prey on some other organic beings;
the decrease of which from any cause would cause a proportionate
destruction of the living coral.  The relations, therefore, which determine
the formation of reefs on any shore, by the vigorous growth of the
efficient kinds of coral, must be very complex, and with our imperfect
knowledge quite inexplicable.  From these considerations, we may infer that
changes in the condition of the sea, not obvious to our senses, might
destroy all the coral-reefs in one area, and cause them to appear in
another: thus, the Pacific or Indian Ocean might become as barren of
coral-reefs as the Atlantic now is, without our being able to assign any
adequate cause for such a change.

It has been a question with some naturalists, which part of a reef is most
favourable to the growth of coral.  The great mounds of living Porites and
of Millepora round Keeling atoll occur exclusively on the extreme verge of
the reef, which is washed by a constant succession of breakers; and living
coral nowhere else forms solid masses.  At the Marshall islands the larger
kinds of coral (chiefly species of Astraea, a genus closely allied to
Porites) "which form rocks measuring several fathoms in thickness," prefer,
according to Chamisso (Kotzebue's "First Voyage" (English Translation),
volume iii., pages 142, 143, 331.), the most violent surf.  I have stated
that the outer margin of the Maldiva atolls consists of living corals (some
of which, if not all, are of the same species with those at Keeling atoll),
and here the surf is so tremendous, that even large ships have been thrown,
by a single heave of the sea, high and dry on the reef, all on board thus
escaping with their lives.

Ehrenberg (Ehrenberg, "Uber die Natur und Bildung der Corallen Banke im
rothen Meere," page 49.) remarks, that in the Red Sea the strongest corals
live on the outer reefs, and appear to love the surf; he adds, that the
more branched kinds abound a little way within, but that even these in
still more protected places, become smaller.  Many other facts having a
similar tendency might be adduced.  (In the West Indies, as I am informed
by Captain Bird Allen, R.N., it is the common belief of those, who are best
acquainted with the reefs, that the coral flourishes most, where freely
exposed to the swell of the open sea.)  It has, however, been doubted by
MM. Quoy and Gaimard, whether any kind of coral can even withstand, much
less flourish in, the breakers of an open sea ("Annales des Sciences
Naturelles," tome vi., pages 276, 278.--"La ou les ondes sont agitees, les
Lytophytes ne peuvent travailler, parce qu'elles detruiraient leurs
fragiles edifices," etc.): they affirm that the saxigenous lithophytes
flourish only where the water is tranquil, and the heat intense.  This
statement has passed from one geological work to another; nevertheless, the
protection of the whole reef undoubtedly is due to those kinds of coral,
which cannot exist in the situations thought by these naturalists to be
most favourable to them.  For should the outer and living margin perish, of
any one of the many low coral-islands, round which a line of great breakers
is incessantly foaming, the whole, it is scarcely possible to doubt, would
be washed away and destroyed, in less than half a century.  But the vital
energies of the corals conquer the mechanical power of the waves; and the
large fragments of reef torn up by every storm, are replaced by the slow
but steady growth of the innumerable polypifers, which form the living zone
on its outer edge.

From these facts, it is certain, that the strongest and most massive corals
flourish, where most exposed.  The less perfect state of the reef of most
atolls on the leeward and less exposed side, compared with its state to
windward; and the analogous case of the greater number of breaches on the
near sides of those atolls in the Maldiva Archipelago, which afford some
protection to each other, are obviously explained by this circumstance.  If
the question had been, under what conditions the greater number of species
of coral, not regarding their bulk and strength, were developed, I should
answer,--probably in the situations described by MM. Quoy and Gaimard,
where the water is tranquil and the heat intense.  The total number of
species of coral in the circumtropical seas must be very great: in the Red
Sea alone, 120 kinds, according to Ehrenberg (Ehrenberg, "Uber die Natur,"
etc., etc., page 46.), have been observed.

The same author has observed that the recoil of the sea from a steep shore
is injurious to the growth of coral, although waves breaking over a bank
are not so.  Ehrenberg also states, that where there is much sediment,
placed so as to be liable to be moved by the waves there is little or no
coral; and a collection of living specimens placed by him on a sandy shore
died in the course of a few days.  (Ibid., page 49.)  An experiment,
however, will presently be related in which some large masses of living
coral increased rapidly in size, after having been secured by stakes on a
sandbank.  That loose sediment should be injurious to the living
polypifers, appears, at first sight, probable; and accordingly, in sounding
off Keeling atoll, and (as will hereafter be shown) off Mauritius, the
arming of the lead invariably came up clean, where the coral was growing
vigorously.  This same circumstance has probably given rise to a strange
belief, which, according to Captain Owen (Captain Owen on the Geography of
the Maldiva Islands, "Geographical Journal", volume ii., page 88.), is
general amongst the inhabitants of the Maldiva atolls, namely that corals
have roots, and therefore that if merely broken down to the surface, they
grow up again; but, if rooted out, they are permanently destroyed.  By this
means the inhabitants keep their harbours clear; and thus the French
Governor of St. Mary's in Madagascar, "cleared out and made a beautiful
little port at that place."  For it is probable that sand would accumulate
in the hollows formed by tearing out the corals, but not on the broken and
projecting stumps, and therefore, in the former case, the fresh growth of
the coral might be thus prevented.

In the last chapter I remarked that fringing-reefs are almost universally
breached, where streams enter the sea.  (Lieutenant Wellstead and others
have remarked that this is the case in the Red Sea; Dr. Ruppell ("Reise in
Abyss." Band. i., page 142) says that there are pear-shaped harbours in the
upraised coral-coast, into which periodical streams enter.  From this
circumstance, I presume, we must infer that before the upheaval of the
strata now forming the coast-land, fresh water and sediment entered the sea
at these points; and the coral being thus prevented growing, the pear-shaped
harbours were produced.)  Most authors have attributed this fact to
the injurious effects of the fresh water, even where it enters the sea only
in small quantity, and during a part of the year.  No doubt brackish water
would prevent or retard the growth of coral; but I believe that the mud and
sand which is deposited, even by rivulets when flooded, is a much more
efficient check.  The reef on each side of the channel leading into Port
Louis at Mauritius, ends abruptly in a wall, at the foot of which I sounded
and found a bed of thick mud.  This steepness of the sides appears to be a
general character in such breaches.  Cook (Cook's "First Voyage," volume
ii., page 271 (Hawkesworth's edition).), speaking of one at Raiatea, says,
"like all the rest, it is very steep on both sides."  Now, if it were the
fresh water mingling with the salt which prevented the growth of coral, the
reef certainly would not terminate abruptly, but as the polypifers nearest
the impure stream would grow less vigorously than those farther off, so
would the reef gradually thin away.  On the other hand, the sediment
brought down from the land would only prevent the growth of the coral in
the line of its deposition, but would not check it on the side, so that the
reefs might increase till they overhung the bed of the channel.  The
breaches are much fewer in number, and front only the larger valleys in
reefs of the encircling barrier class.  They probably are kept open in the
same manner as those into the lagoon of an atoll, namely, by the force of
the currents and the drifting outwards of fine sediment.  Their position in
front of valleys, although often separated from the land by deep water
lagoon-channels, which it might be thought would entirely remove the
injurious effects both of the fresh water and the sediment, will receive a
simple explanation when we discuss the origin of barrier-reefs.

In the vegetable kingdom every different station has its peculiar group of
plants, and similar relations appear to prevail with corals.  We have
already described the great difference between the corals within the lagoon
of an atoll and those on its outer margin.  The corals, also, on the margin
of Keeling Island occurred in zones; thus the Porites and Millepora
complanata grow to a large size only where they are washed by a heavy sea,
and are killed by a short exposure to the air; whereas, three species of
Nullipora also live amidst the breakers, but are able to survive uncovered
for a part of each tide; at greater depths, a strong Madrepora and
Millepora alcicornis are the commonest kinds, the former appearing to be
confined to this part, beneath the zone of massive corals, minute
encrusting corallines and other organic bodies live.  If we compare the
external margin of the reef at Keeling atoll with that on the leeward side
of Mauritius, which are very differently circumstanced, we shall find a
corresponding difference in the appearance of the corals.  At the latter
place, the genus Madrepora is preponderant over every other kind, and
beneath the zone of massive corals there are large beds of Seriatopora.
There is also a marked difference, according to Captain Moresby (Captain
Moresby on the Northern Maldiva atolls, "Geographical Journal", volume v.,
page 401.), between the great branching corals of the Red Sea, and those on
the reefs of the Maldiva atolls.

These facts, which in themselves are deserving of notice, bear, perhaps,
not very remotely, on a remarkable circumstance which has been pointed out
to me by Captain Moresby, namely, that with very few exceptions, none of
the coral-knolls within the lagoons of Peros Banhos, Diego Garcia, and the
Great Chagos Bank (all situated in the Chagos group), rise to the surface
of the water; whereas all those, with equally few exceptions, within
Solomon and Egmont atolls in the same group, and likewise within the large
southern Maldiva atolls, reach the surface.  I make these statements, after
having examined the charts of each atoll.  In the lagoon of Peros Banhos,
which is nearly twenty miles across, there is only one single reef which
rises to the surface; in Diego Garcia there are seven, but several of these
lie close to the margin of the lagoon, and need scarcely have been
reckoned; in the Great Chagos Bank there is not one.  On the other hand, in
the lagoons of some of the great southern Maldiva atolls, although thickly
studded with reefs, every one without exception rises to the surface; and
on an average there are less than two submerged reefs in each atoll; in the
northern atolls, however, the submerged lagoon-reefs are not quite so rare.
The submerged reefs in the Chagos atolls generally have from one to seven
fathoms water on them, but some have from seven to ten.  Most of them are
small with very steep sides (Some of these statements were not communicated
to me verbally by Captain Moresby, but are taken from the MS. account
before alluded to, of the Chagos Group.); at Peros Banhos they rise from a
depth of about thirty fathoms, and some of them in the Great Chagos Bank
from above forty fathoms; they are covered, Captain Moresby informs me,
with living and healthy coral, two and three feet high, consisting of
several species.  Why then have not these lagoon-reefs reached the surface,
like the innumerable ones in the atolls above named?  If we attempt to
assign any difference in their external conditions, as the cause of this
diversity, we are at once baffled.  The lagoon of Diego Garcia is not deep,
and is almost wholly surrounded by its reef; Peros Banhos is very deep,
much larger, with many wide passages communicating with the open sea.  On
the other hand, of those atolls, in which all or nearly all the lagoon-reefs
have reached the surface, some are small, others large, some shallow,
others deep, some well-enclosed, and others open.

Captain Moresby informs me that he has seen a French chart of Diego Garcia
made eighty years before his survey, and apparently very accurate; and from
it he infers, that during this interval there has not been the smallest
change in the depth on any of the knolls within the lagoon.  It is also
known that during the last fifty-one years, the eastern channel into the
lagoon has neither become narrower, nor decreased in depth; and as there
are numerous small knolls of living coral within it, some change might have
been anticipated.  Moreover, as the whole reef round the lagoon of this
atoll has been converted into land--an unparalleled case, I believe, in an
atoll of such large size,--and as the strip of land is for considerable
spaces more than half a mile wide--also a very unusual circumstance,--we
have the best possible evidence, that Diego Garcia has remained at its
present level for a very long period.  With this fact, and with the
knowledge that no sensible change has taken place during eighty years in
the coral-knolls, and considering that every single reef has reached the
surface in other atolls, which do not present the smallest appearance of
being older than Diego Garcia and Peros Banhos, and which are placed under
the same external conditions with them, one is led to conclude that these
submerged reefs, although covered with luxuriant coral, have no tendency to
grow upwards, and that they would remain at their present levels for an
almost indefinite period.

From the number of these knolls, from their position, size, and form, many
of them being only one or two hundred yards across, with a rounded outline,
and precipitous sides,--it is indisputable that they have been formed by
the growth of coral; and this makes the case much more remarkable.  In
Peros Banhos and in the Great Chagos Bank, some of these almost columnar
masses are 200 feet high, and their summits lie only from two to eight
fathoms beneath the surface; therefore, a small proportional amount more of
growth would cause them to attain the surface, like those numerous knolls,
which rise from an equally great depth within the Maldiva atolls.  We can
hardly suppose that time has been wanting for the upward growth of the
coral, whilst in Diego Garcia, the broad annular strip of land, formed by
the continued accumulation of detritus, shows how long this atoll has
remained at its present level.  We must look to some other cause than the
rate of growth; and I suspect it will be found in the reefs being formed of
different species of corals, adapted to live at different depths.

The Great Chagos Bank is situated in the centre of the Chagos Group, and
the Pitt and Speaker Banks at its two extreme points.  These banks resemble
atolls, except in their external rim being about eight fathoms submerged,
and in being formed of dead rock, with very little living coral on it: a
portion nine miles long of the annular reef of Peros Banhos atoll is in the
same condition.  These facts, as will hereafter be shown, render it very
probable that the whole group at some former period subsided seven or eight
fathoms; and that the coral perished on the outer margin of those atolls
which are now submerged, but that it continued alive, and grew up to the
surface on those which are now perfect.  If these atolls did subside, and
if from the suddenness of the movement or from any other cause, those
corals which are better adapted to live at a certain depth than at the
surface, once got possession of the knolls, supplanting the former
occupants, they would exert little or no tendency to grow upwards.  To
illustrate this, I may observe, that if the corals of the upper zone on the
outer edge of Keeling atoll were to perish, it is improbable that those of
the lower zone would grow to the surface, and thus become exposed to
conditions for which they do not appear to be adapted.  The conjecture,
that the corals on the submerged knolls within the Chagos atolls have
analogous habits with those of the lower zone outside Keeling atoll,
receives some support from a remark by Captain Moresby, namely, that they
have a different appearance from those on the reefs in the Maldiva atolls,
which, as we have seen, all rise to the surface: he compares the kind of
difference to that of the vegetation under different climates.  I have
entered at considerable length into this case, although unable to throw
much light on it, in order to show that an equal tendency to upward growth
ought not to be attributed to all coral-reefs,--to those situated at
different depths,--to those forming the ring of an atoll or those on the
knolls within a lagoon,--to those in one area and those in another.  The
inference, therefore, that one reef could not grow up to the surface within
a given time, because another, not known to be covered with the same
species of corals, and not known to be placed under conditions exactly the
same, has not within the same time reached the surface, is unsound.

Critical introduction by John W. Judd

THE STRUCTURE AND DISTRIBUTION OF CORAL REEFS.


CRITICAL INTRODUCTION.

A scientific discovery is the outcome of an interesting process of
evolution in the mind of its author.  When we are able to detect the germs
of thought in which such a discovery has originated, and to trace the
successive stages of the reasoning by which the crude idea has developed
into an epoch-making book, we have the materials for reconstructing an
important chapter of scientific history.  Such a contribution to the story
of the "making of science" may be furnished in respect to Darwin's famous
theory of coral-reefs, and the clearly reasoned treatise in which it was
first fully set forth.

The subject of corals and coral-reefs is one concerning which much popular
misconception has always prevailed.  The misleading comparison of coral-rock
with the combs of bees and the nests of wasps is perhaps responsible
for much of this misunderstanding; one writer has indeed described a
coral-reef as being "built by fishes by means of their teeth."  Scarcely
less misleading, however, are the references we so frequently meet with,
both in prose and verse, to the "skill," "industry," and "perseverance" of
the "coral-insect" in "building" his "home."  As well might we praise men
for their cleverness in making their own skeletons, and laud their assiduity
in filling churchyards with the same.  The polyps and other organisms, whose
remains accumulate to form a coral-reef, simply live and perform their
natural functions, and then die, leaving behind them, in the natural course
of events, the hard calcareous portions of their structures to add to the
growing reef.

While the forms of coral-reefs and coral-islands are sometimes very
remarkable and worthy of attentive study, there is no ground, it need
scarcely be added, for the suggestion that they afford proofs of design on
the part of the living builders, or that, in the words of Flinders, they
constitute breastworks, defending the workshops from whence "infant
colonies might be safely sent forth."

It was not till the beginning of the present century that travellers like
Beechey, Chamisso, Quoy and Gaimard, Moresby, Nelson, and others, began to
collect accurate details concerning the forms and structure of coral-masses,
and to make such observations on the habits of reef-forming polyps,
as might serve as a basis for safe reasoning concerning the origin of
coral-reefs and islands.  In the second volume of Lyell's "Principles of
Geology," published in 1832, the final chapter gives an admirable summary
of all that was then known on the subject.  At that time, the ring-form of
the atolls was almost universally regarded as a proof that they had grown
up on submerged volcanic craters; and Lyell gave his powerful support to
that theory.

Charles Darwin was never tired of acknowledging his indebtedness to Lyell.
In dedicating to his friend the second edition of his "Naturalist's Voyage
Round the World," Darwin writes that he does so "with grateful pleasure, as
an acknowledgment that the chief part of whatever scientific merit this
journal and the other works of the author may possess, has been derived
from studying the well-known and admirable 'Principles of Geology.'"

The second volume of Lyell's "Principles" appeared after Darwin had left
England; but it was doubtless sent on to him without delay by his faithful
friend and correspondent, Professor Henslow.  It appears to have reached
Darwin at a most opportune moment, while, in fact, he was studying the
striking evidences of slow and long-continued, but often interrupted
movement on the west coast of South America.  Darwin's acute mind could not
fail to detect the weakness of the then prevalent theory concerning the
origin of the ring-shaped atolls--and the difficulty which he found in
accepting the volcanic theory, as an explanation of the phenomena of
coral-reefs, is well set forth in his book.

In an interesting fragment of autobiography, Darwin has given us a very
clear account of the way in which the leading idea of the theory of
coral-reefs originated in his mind; he writes, "No other work of mine was
begun in so deductive a spirit as this, for the whole theory was thought
out on the west coast of South America, before I had seen a true
coral-reef.  I had therefore only to verify and extend my views by a
careful examination of living reefs.  But it should be observed that I had
during the two previous years been incessantly attending to the effects on
the shores of South America of the intermittent elevation of the land,
together with the denudation and deposition of sediment.  This necessarily
led me to reflect much on the effects of subsidence, and it was easy to
replace in imagination the continued deposition of sediment by the upward
growth of corals.  To do this was to form my theory of the formation of
barrier-reefs and atolls."

On her homeward voyage, the "Beagle" visited Tahiti, Australia, and some of
the coral-islands in the Indian Ocean, and Darwin had an opportunity of
testing and verifying the conclusion at which he had arrived by studying
the statements of other observers.

I well recollect a remarkable conversation I had with Darwin, shortly after
the death of Lyell.  With characteristic modesty, he told me that he never
fully realised the importance of his theory of coral-reefs till he had an
opportunity of discussing it with Lyell, shortly after the return of the
"Beagle".  Lyell, on receiving from the lips of its author a sketch of the
new theory, was so overcome with delight that he danced about and threw
himself into the wildest contortions, as was his manner when excessively
pleased.  He wrote shortly afterwards to Darwin as follows:--"I could think
of nothing for days after your lesson on coral-reefs, but of the tops of
submerged continents.  It is all true, but do not flatter yourself that you
will be believed till you are growing bald like me, with hard work and
vexation at the incredulity of the world."  On May 24th, 1837, Lyell wrote
to Sir John Herschel as follows:--"I am very full of Darwin's new theory of
coral-islands, and have urged Whewell to make him read it at our next
meeting.  I must give up my volcanic crater forever, though it cost me a
pang at first, for it accounted for so much."  Dr. Whewell was president of
the Geological Society at the time, and on May 31st, 1837, Darwin read a
paper entitled "On Certain Areas of Elevation and Subsidence in the Pacific
and Indian oceans, as deduced from the Study of Coral Formations," an
abstract of which appeared in the second volume of the Society's
proceedings.

It was about this time that Darwin, having settled himself in lodgings at
Great Marlborough Street, commenced the writing of his book on "Coral-Reefs."
Many delays from ill-health and the interruption of other work,
caused the progress to be slow, and his journal speaks of "recommencing"
the subject in February 1839, shortly after his marriage, and again in
October of the same year.  In July 1841, he states that he began once more
"after more than thirteen month's interval," and the last proof-sheet of
the book was not corrected till May 6th, 1842.  Darwin writes in his
autobiography, "This book, though a small one, cost me twenty months of
hard work, as I had to read every work on the islands of the Pacific, and
to consult many charts."  The task of elaborating and writing out his books
was, with Darwin, always a very slow and laborious one; but it is clear
that in accomplishing the work now under consideration, there was a long
and constant struggle with the lethargy and weakness resulting from the sad
condition of his health at that time.

Lyell's anticipation that the theory of coral-reefs would be slow in
meeting with general acceptance was certainly not justified by the actual
facts.  On the contrary the new book was at once received with general
assent among both geologists and zoologists, and even attracted a
considerable amount of attention from the general public.

It was not long before the coral-reef theory of Darwin found an able
exponent and sturdy champion in the person of the great American
naturalist, Professor James D. Dana.  Two years after the return of the
"Beagle" to England, the ships of the United States Exploring Expedition
set sail upon their four years' cruise, under the command of Captain
Wilkes, and Dana was a member of the scientific staff.  When, in 1839, the
expedition arrived at Sydney, a newspaper paragraph was found which gave
the American naturalist the first intimation of Darwin's new theory of the
origin of atolls and barrier-reefs.  Writing in 1872, Dana describes the
effect produced on his mind by reading this passage:--"The paragraph threw
a flood of light over the subject, and called forth feelings of peculiar
satisfaction, and of gratefulness to Mr. Darwin, which still come up afresh
whenever the subject of coral islands is mentioned.  The Gambier Islands in
the Paumotus, which gave him the key to the theory, I had not seen; but on
reaching the Feejees, six months later, in 1840, I found there similar
facts on a still grander scale and of a more diversified character, so that
I was afterward enabled to speak of his theory as established with more
positiveness than he himself, in his philosophic caution, had been ready to
adopt.  His work on coral-reefs appeared in 1842, when my report on the
subject was already in manuscript.  It showed that the conclusions on other
points, which we had independently reached, were for the most part the
same.  The principal points of difference relate to the reason for the
absence of corals from some coasts, and the evidence therefrom as to
changes of level, and the distribution of the oceanic regions of elevation
and subsidence--topics which a wide range of travel over the Pacific
brought directly and constantly to my attention."

Among the Reports of the United States Exploring Expedition, two important
works from the pen of Professor Dana made their appearance;--one on
"Zoophytes," which treats at length on "Corals and Coral-Animals," and the
other on "Coral-Reefs and Islands."  In 1872, Dana prepared a work of a
more popular character in which some of the chief results of his studies
are described; it bore the title of "Corals and Coral-Islands."  Of this
work, new and enlarged editions appeared in 1874 and 1890 in America, while
two editions were published in this country in 1872 and 1875.  In all these
works their author, while maintaining an independent judgment on certain
matters of detail, warmly defends the views of Darwin on all points
essential to the theory.

Another able exponent and illustrator of the theory of coral-reefs was
found in Professor J.B. Jukes, who accompanied H.M.S. "Fly", as naturalist,
during the survey of the Great Barrier-Reef--in the years 1842 to 1846.
Jukes, who was a man of great acuteness as well as independence of mind,
concludes his account of the great Australian reefs with the following
words:--"After seeing much of the Great Barrier-Reefs, and reflecting much
upon them, and trying if it were possible by any means to evade the
conclusions to which Mr. Darwin has come, I cannot help adding that his
hypothesis is perfectly satisfactory to my mind, and rises beyond a mere
hypothesis into the true theory of coral-reefs."

As the result of the clear exposition of the subject by Darwin, Lyell,
Dana, and Jukes, the theory of coral-reefs had, by the middle of the
present century, commanded the almost universal assent of both biologists
and geologists.  In 1859 Baron von Richthofen brought forward new facts in
its support, by showing that the existence of the thick masses of dolomitic
limestone in the Tyrol could be best accounted for if they were regarded as
of coralline origin and as being formed during a period of long continued
subsidence.  The same views were maintained by Professor Mojsisovics in his
"Dolomit-riffe von Sudtirol und Venetien," which appeared in 1879.

The first serious note of dissent to the generally accepted theory was
heard in 1863, when a distinguished German naturalist, Dr. Karl Semper,
declared that his study of the Pelew Islands showed that uninterrupted
subsidence could not have been going on in that region.  Dr. Semper's
objections were very carefully considered by Mr. Darwin, and a reply to
them appeared in the second and revised edition of his "Coral-Reefs," which
was published in 1874.  With characteristic frankness and freedom from
prejudice, Darwin admitted that the facts brought forward by Dr. Semper
proved that in certain specified cases, subsidence could not have played
the chief part in originating the peculiar forms of the coral-islands.  But
while making this admission, he firmly maintained that exceptional cases,
like those described in the Pelew Islands, were not sufficient to
invalidate the theory of subsidence as applied to the widely spread atolls,
encircling reefs, and barrier-reefs of the Pacific and Indian Oceans.  It
is worthy of note that to the end of his life Darwin maintained a friendly
correspondence with Semper concerning the points on which they were at
issue.

After the appearance of Semper's work, Dr. J.J. Rein published an account
of the Bermudas, in which he opposed the interpretation of the structure of
the islands given by Nelson and other authors, and maintained that the
facts observed in them are opposed to the views of Darwin.  Although, so
far as I am aware, Darwin had no opportunity of studying and considering
these particular objections, it may be mentioned that two American
geologists have since carefully re-examined the district--Professor W.N.
Rice in 1884 and Professor A. Heilprin in 1889--and they have independently
arrived at the conclusion that Dr. Rein's objections cannot be maintained.

The most serious opposition to Darwin's coral-reef theory, however, was
that which developed itself after the return of H.M.S. "Challenger" from
her famous voyage.  Mr. John Murray, one of the staff of naturalists on
board that vessel, propounded a new theory of coral-reefs, and maintained
that the view that they were formed by subsidence was one that was no
longer tenable; these objections have been supported by Professor Alexander
Agassiz in the United States, and by Dr. A. Geikie, and Dr. H.B. Guppy in
this country.

Although Mr. Darwin did not live to bring out a third edition of his
"Coral-Reefs," I know from several conversations with him that he had given
the most patient and thoughtful consideration to Mr. Murray's paper on the
subject.  He admitted to me that had he known, when he wrote his work, of
the abundant deposition of the remains of calcareous organisms on the sea
floor, he might have regarded this cause as sufficient in a few cases to
raise the summits of submerged volcanoes or other mountains to a level at
which reef-forming corals can commence to flourish.  But he did not think
that the admission that under certain favourable conditions, atolls might
be thus formed without subsidence, necessitated an abandonment of his
theory in the case of the innumerable examples of the kind which stud the
Indian and Pacific Oceans.

A letter written by Darwin to Professor Alexander Agassiz in May 1881 shows
exactly the attitude which careful consideration of the subject led him to
maintain towards the theory propounded by Mr. Murray:--"You will have
seen," he writes, "Mr. Murray's views on the formation of atolls and
barrier-reefs.  Before publishing my book, I thought long over the same
view, but only as far as ordinary marine organisms are concerned, for at
that time little was known of the multitude of minute oceanic organisms.  I
rejected this view, as from the few dredgings made in the "Beagle", in the
south temperate regions, I concluded that shells, the smaller corals, etc.,
decayed and were dissolved when not protected by the deposition of
sediment, and sediment could not accumulate in the open ocean.  Certainly,
shells, etc., were in several cases completely rotten, and crumbled into
mud between my fingers; but you will know whether this is in any degree
common.  I have expressly said that a bank at the proper depth would give
rise to an atoll, which could not be distinguished from one formed during
subsidence.  I can, however, hardly believe in the existence of as many
banks (there having been no subsidence) as there are atolls in the great
oceans, within a reasonable depth, on which minute oceanic organisms could
have accumulated to the depth of many hundred feet."

Darwin's concluding words in the same letter written within a year of his
death, are a striking proof of the candour and openness of mind which he
preserved so well to the end, in this as in other controversies.

"If I am wrong, the sooner I am knocked on the head and annihilated so much
the better.  It still seems to me a marvellous thing that there should not
have been much, and long-continued, subsidence in the beds of the great
oceans.  I wish some doubly rich millionaire would take it into his head to
have borings made in some of the Pacific and Indian atolls, and bring home
cores for slicing from a depth of 500 or 600 feet."

It is noteworthy that the objections to Darwin's theory have for the most
part proceeded from zoologists, while those who have fully appreciated the
geological aspect of the question, have been the staunchest supporters of
the theory of subsidence.  The desirability of such boring operations in
atolls has been insisted upon by several geologists, and it may be hoped
that before many years have passed away, Darwin's hopes may be realised,
either with or without the intervention of the "doubly rich millionaire."

Three years after the death of Darwin, the veteran Professor Dana
re-entered the lists and contributed a powerful defence of the theory of
subsidence in the form of a reply to an essay written by the ablest
exponent of the anti-Darwinian views on this subject, Dr. A. Geikie.  While
pointing out that the Darwinian position had been to a great extent
misunderstood by its opponents, he showed that the rival theory presented
even greater difficulties than those which it professed to remove.

During the last five years, the whole question of the origin of coral-reefs
and islands has been re-opened, and a controversy has arisen, into which,
unfortunately, acrimonious elements have been very unnecessarily
introduced.  Those who desire it, will find clear and impartial statements
of the varied and often mutually destructive views put forward by different
authors, in three works which have made their appearance within the last
year,--"The Bermuda Islands," by Professor Angelo Heilprin; "Corals and
Coral-Islands," new edition by Professor J.D. Dana; and the third edition
of Darwin's "Coral-Reefs," with Notes and Appendix by Professor T.G.
Bonney.

Most readers will, I think, rise from the perusal of these works with the
conviction that, while on certain points of detail it is clear that,
through the want of knowledge concerning the action of marine organisms in
the open ocean, Darwin was betrayed into some grave errors, yet the main
foundations of his argument have not been seriously impaired by the new
facts observed in the deep-sea researches, or by the severe criticism to
which his theory has been subjected during the last ten years.  On the
other hand, I think it will appear that much misapprehension has been
exhibited by some of Darwin's critics, as to what his views and arguments
really were; so that the reprint and wide circulation of the book in its
original form is greatly to be desired, and cannot but be attended with
advantage to all those who will have the fairness to acquaint themselves
with Darwin's views at first hand, before attempting to reply to them.

JOHN W. JUDD.